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Article

Zircon U–Pb Age and Geochemistry of Ore-Hosting Rocks from the Liuhe Orefield of the Jiapigou Gold Ore Belt, NE China: Magmatism and Tectonic Implications

by
Jian Zhang
1,2,
Yanchen Yang
1,*,
Piyi Guo
3 and
Wukeyila Wutiepu
4
1
College of Earth Sciences, Jilin University, Changchun 130061, China
2
Team 607, Jilin Nonferrous Metal Geological Exploration Bureau, Jilin 132000, China
3
Team 608, Jilin Nonferrous Metal Geological Exploration Bureau, Changchun 130000, China
4
Xinjiang Research Centre for Mineral Resources, Xinjiang Institute of Ecology and Geography, Chinese Academy of Sciences, Urumqi 830011, China
*
Author to whom correspondence should be addressed.
Minerals 2022, 12(9), 1121; https://doi.org/10.3390/min12091121
Submission received: 17 August 2022 / Revised: 28 August 2022 / Accepted: 1 September 2022 / Published: 2 September 2022
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Abstract

:
Liuhe gold orefield is being newly explored in the southeast part of the Jiapigou gold ore belt, and occurs in the Neoarchean basement composed of trondhjemite–tonalite–granodiorite (TTG). Zircon U–Pb data suggest that the ore-hosting magma emplacement in the Liuhe orefield mainly took place in two epochs: late Neoarchean to early Paleoproterozoic (ca. 2500 Ma) and early Jurassic of the Mesozoic era (ca. 170 Ma). The TTG rocks show higher A12O3 (12.58 to 15.71%) and Na2O/K2O ratios (1.16 to 2.9), and lower MgO (0.93 to 2.73%) and Mg# values, with positive Eu anomaly and low Y and Yb content, and high Sr/Y (22.3–79.6), and the plot in the adakite field in the Sr/Y-Y discriminant diagram belongs to the modern island-arc adakite rocks. Samples in this study are plotted in the pre-plate collision area in the R1-R2 discrimination diagram, and fall into the VAG and VAG + Syn-COLG field in the Rb-Y + Nb and Nb-Y diagram, respectively, indicating that the magmatism is related to plate subduction. The ore-bearing TTGs of the late Neoarchean to early Paleoproterozoic deposits were derived from the partial melting of mafic lower crustal caused by the underplating of basaltic magma on the island-arc or active continental margin before plate collision. The magmatism of the Dajiagou deposit occurred in active continental margin setting associated with the westward subduction of the paleo-Pacific plate beneath Eurasian Plate during the early Jurassic of Mesozoic period.

1. Introduction

As the oldest and largest craton in China, the North China Craton (NCC) has been the subject of extensive research and attention owing to its complex evolution and abundant mineral resources [1,2,3,4,5,6,7,8]. The gold deposits are distributed along the margin of the NCC and generally occur in the Precambrian basement rocks or Phanerozoic felsic plutons [3,9,10,11]. From Jiaodong, many gold concentration areas lie along the margin of the NCC in a counterclockwise direction, including the Eastern Liaoning, Jiapigou, Chifeng–Chaoyang, Eastern Hebei, Zhan–Xuan, Daqingshan, Xiaoqinling–Xiongershan, and Western Qinling areas. The gold reserves in the NCC account for over 70% of all reserves in China [9,12]. As the gold mining area with the longest mining history in China, the northern margin of the NCC is rich in gold resources, with more than 900 t of Au. The most famous is the Jiapigou gold mining area, which has a mining history of nearly 200 years and has produced 150 t of gold, includes dozens of gold deposits such as the Erdaogou, Xiaobeigou, Banmiaozi, and Bajiazi deposits [4,13,14]. It is regarded as one of the most important gold-producing districts in China [4,15].
The Jiapigou gold ore belt is located in the eastern part of the northern margin of the NCC, with the Siberian plate and the Yangtze Craton to the north and south, respectively, and the Pacific plate to the east (Figure 1a,b) [16]. The entire gold belt is located in the NW Jiapigou fault between the NE Liangjiang fault and the Huifahe fault [5]. It lies in the Neoarchean basement and is mainly composed of gray gneisses, including Neoarchean–Paleoproterozoic trondhjemite–tonalite–granodiorite (TTG). However, it was extensively reworked by the closure of the Paleo-Asian Ocean between the NCC and the Siberian plate and the subduction of the Pacific plate beneath the East Asian continent in the Mesozoic. The Jiapigou fault suffered from ductile shear in the early stage and brittle deformation in the late stage; the ore bodies lie in the ductile–brittle shear zone and are obviously controlled by structure [14,17,18,19,20,21]. Although the Jiapigou gold ore belt contains several large gold ore fields, such as the Jiapigou, Banmiaozi, and Haigou gold ore fields, the shallow resources have been exhausted by the long mining history. The Liuhe gold ore field is a newly prospected ore field located southeast of the Jiapigou gold ore belt. It includes the large Dajiagou deposit, and the small-scale Zhemagou, Gaoligou, and Binghugou deposits. According to the traditional Archean gold metallogenic theory, the large gold deposits generally occur in the granite-greenstone belt, such as Canada, Australia, and South Africa, while there are a few reports of large gold deposits in high-grade metamorphic zones. The ore morphology, ore type and other characteristics of the deposit in the Liuhe orefield are not very different from those of gold deposit in the Jiapigou granite-greenstone belt, which makes it necessary to further discuss the relationship between high-intensity metamorphic zone and gold mineralization. Since the discovery of the Liuhe gold deposit in the 1990s, it has been a hot spot for geologists; however, because of the late exploration and development in this area, the lack of research on deposit geology and genesis has seriously limited understanding of the metallogenic regularity in this area and restrained future exploration. In this paper, we report new geological, petrological, zircon U–Pb and whole-rock geochemical data for the Djiagou, Daxigou, Binghugou, Gaoligou, and Zhemagou deposits, combined with the latest data of the Liuhe ore field and Jiapigou gold ore belt, and the petrogenesis of ore-bearing rocks, the metallogenic geodynamic setting, genesis, and metallogenic model of these deposits are expounded in detail.

2. Regional Geology

The Liuhe area is located in the northern end of the Longgang continental nucleus in the eastern part of the northern NCC, and on the platform marginal active belt at the junction of the NCC and Jihei fold belt. It belongs to the same tectonic unit as the Jiapigou gold ore field, which is the southeast extension of the Jiapigou gold belt [25,26] (Figure 1c). The Liuhe area is an Archean high-grade metamorphic terrain, dominated by Archean rock units. Owing to the influence of the regional metamorphism and tectonic movement, the rock metamorphism and deformation are extremely intense [27]. The exposed rocks are mainly gray gneiss (TTG), including Wutai potassium and sodium granites, the supercrust rocks and Fuping felsic gneiss are mostly “floating” in the gray gneiss, while the metamorphic intermediate–basic intrusive rocks mostly occur as dikes (Figure 2) [28,29]. The magmatic activities in the Liuhe area were relatively frequent and can be traced back to the Archean. The Archean–Proterozoic magmatic rocks have undergone multiple metamorphism and deformation and mostly became gray gneisses [13,24]. With the intensification of crustal activity and diapirism, Caledonian granodiorite intruded in a large area along the margin of the platform. Under the influence of the Indosinian movement, the intermediate–basic to acidic magma of the Wudaoliuhe sequence emplaced and was represented by the EW trending Wudaoliuhe granite [30]. In the Yanshanian period, quartz porphyry, granite porphyry, and rhyolitic porphyry sporadically distributed in the area. Mesozoic intermediate–basic, acidic, and alkaline dikes distributed along the NE-trending tectono-magmatic activity zone between the Toudaoliuhe–Wudaoliuhe sequence, among which cryptoexplosive breccia bodies were found in Jiancaogou and Binghugou in Sandaoliuhe [31]. In the Himalayan period, basalt was ejected near the upper and lower walls of the NE-trending structure of the Erdaosonghua River. Magmatic rocks from the Archean to the Mesozoic Jurassic were developed in the study area, including Neoarchean granitic gneiss, Proterozoic intrusive rocks, and Mesozoic intrusive rocks and volcanic rocks. The Neoarchean granitic gneisses are gneissic and contain a large number of supracrustal xenoliths. The Proterozoic intrusive rocks are the products of Archaean craton activation, and are mainly weakly gneissic granitic gneiss. The Paleozoic magmatism was not developed. Mesozoic intrusive rocks are mainly granitic complexes, which occur as irregular intrusives or composite complexes. Archean granites are widely outcropped in the study area, mainly including TTG series and monzogranitic and potassium granitic gneiss. The TTG assemblage is trondhjemite–tonalite–granodiorite, which is largely outcropped on the west side of the Jiapigou ductile shear zone. Monzogranitic and potassium granitic gneiss are widely exposed in the east of the study area, mainly distributed along the ductile shear zone in a zonal pattern. Due to the influence of regional metamorphism and the transformation of tectonic deformation, the contact relationship between them is not clear or covered up, and the intrusion of light metagranite into potassic granitic gneiss can be seen in some areas. In general, Archean granites evolved from sodic to potassic.
The Liuhe area is located in the active belt along the margin of the NCC, with developed fault structures. The main structure is the NW-trending ductile–brittle shear zone, which is the southeast extension of the NW-trending ore-controlling structure of the Jiapigou gold ore field, and they are distributed parallel to each other in the outer contact zone of the west side of the Mesozoic Wudaoliuhe monzogranite [32]. The early stage has the characteristics of a ductile shear zone, and the late stage has the characteristics of a brittle fracture structure. In the ductile–brittle shear zone, dikes, porphyry, and cryptoexplosive breccia in different periods can be seen, indicating that the ductile–brittle shear zone has the characteristics of multiple structural superposition and multi-stage dike intrusion and is also the main ore-controlling structure in the Liuhe area [33]. The ductile shear zone cuts through the basement rock–gray gneiss (TTG), proving that the latest formation time of the shear zone was late Archean–Early Proterozoic.

3. Samples and Analytical Methods

3.1. Samples and Petrography

Among the 6 samples collected in this study, 5 were Neoarchean TTG rocks and 1 was Mesozoic intrusive rock. Detailed descriptions of the rock samples and their lithofacies are given below and shown in Table 1.
Monzogranite (sample DJG–N1): light fleshy red in color, of a medium grain and massive structure. It was composed of fleshy red potash feldspar (35–40%), gray plagioclase (30%), quartz (25%) and so on; the plagioclase was partially altered into kaolin and sericite, the quartz particle size was 0.2–3 mm, and most were anhedral granular crystals filled in feldspar minerals; a small amount of pyrite and other metal minerals were seen locally (Figure 3a).
Diorite (sample DJG–N2): the rock was gray-black, of a fine-grained, massive, vein-like structure. Among them, the size of the plagioclase was 0.1–0.3 mm, the content was 40–50%; sericite alteration occurred mostly, hornblende was altered into chlorite, and the content was 30%; pyrite was a cubic crystal with a particle size of 0.0n mm, some crystals reached 0.5 mm, and the content was ±1–10%. When the rocks were subjected to strong tectonic forces and alteration, discoloration occurred and diorite mylonites were found (Figure 3b,c,f).
Monzogranitic breccia (sample BHG–N1): the rock was reddish-brown and brecciform in structure. The breccia was monzogranite with a subangular shape, the cementation was mainly crystal and rock powder of monzogranitic rocks, and the cementation was mainly pore type; contact cementation was also seen locally (Figure 3d,h).
Trondhjemite (sample ZMG–N1): the rocks were mainly grayish white, partially light fleshy red, medium granular texture, massive structure. Main mineral composition: plagioclase was columnar, particle size 0.4–2.0 mm, partially altered into sericite, common polysynthetic twinning, content 50%; quartz was anhedral granular, particle size 0.1–2.0 mm, content 35%; biotite was flake, particle size 0.2–2.5 mm, content 10%, mostly altered into chlorite and magnetite; potash feldspathization was seen locally in the rocks (Figure 3e,i).
Monzogranite (sample GLG–N1): gray-red, medium granular texture, gneissic structure, particle size 3–4 mm. The main mineral components included potassium feldspar, which was columnar, partially altered into kaolin, content 35%; plagioclase was irregular tabular, and there was polysynthetic twinning, some of them were altered into kaolin and sericite, and the content was 25%; quartz was anhedral granular, content of 25%; biotite was flake and varied in size among felsic minerals, with a content of 10% (Figure 3g).
Monzogranite (sample DXG–N1): the rock was light fleshy red, medium-coarse granular texture, massive structure. Orthoclase was anhedral crystal, with a content of about 35%; plagioclase was irregular granular, common sericite, local visible residual polysynthetic twinning, content was about 30%; potassium feldspar was irregular anhedral crystal, content was about 5%; quartz was anhedral granular, content was about 25%; a small amount of biotite and other minerals were detected.

3.2. Whole-Rock Major and Trace Element Analysis

Major elements, trace elements, and rare earth elements (REEs) were analyzed and tested in the ALS Chemex, Guangzhou, China. The major elements were tested by X–ray fluorescence spectrometry (XRF), and the FeO was analyzed by the volumetric method of hydrofluoric acid–sulfuric acid solution and potassium dichromate titration. The analysis accuracy was better than 2%. Trace and rare earth elements were determined using inductively coupled plasma mass spectrometry (ICP-MS). The analysis process was as follows: weigh the 0.0500 g sample in the Teflon high-pressure inner tank, add 1 mL HF and 0.5 mL HNO3, cover the Teflon lid, seal it in the steel sleeve, and place it in the oven at 190 °C for 48 h. After cooling, remove the inner tank and evaporate on the electric heating plate until nearly dry. Add 0.5 mL HNO3 and steam until nearly dry, repeat twice; add 5 mL (1+ 1) HNO3, reseal in the steel jacket, and maintain at 130 °C for 3 h. After cooling, move the sample into a clean plastic bottle with a constant volume of 50 mL. The computer test analysis accuracy was better than 5%.

3.3. Zircon U–Pb Isotopic Analyses

The zircon U–Pb (LA–ICP–MS) method was used to date the main rocks in the samples from the study area. The zircon samples were selected by traditional gravity and magnetic separation methods in the laboratory of the Hebei Institute of Regional Geology and Mineral Resources Survey, Langfang, China. Laser ablation (LA)–ICP–MS zircon U–Pb geochronology from 14 samples was carried out at the MLR Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Jilin University, Changchun, China. A Coherent COMPEx Pro ArF excimer laser was used for laser ablation. The mass spectrometry was performed with an Agilent 7500 A quadrupole plasma mass spectrometer [34]. The standard zircon 91500 (1062 Ma) was used as the external standard for isotope ratio correction [35], the standard zircon GJ–1 was used as the blind sample for monitoring, the international standard sample NIST610 was used as the external standard for element content, and Si was used as the internal standard element for calculation. Isotope ratio and element content were calculated using GLITTER software [36]. Isoplot calculates Concordia ages and images were given using Isoplot/Ex (3.0) [37]. Common Pb correction was calculated using the program presented by Anderson (2002) [38].

4. Analytical Results

4.1. Major and Trace Element Geochemistry

Among the 22 samples analyzed, except DJG–N2–Q1 to DJG–N2–Q4 from the Dajiagou deposit, which are altered fine-grained diorite, 18 samples, including trondhjemite and monzogranite, are Neoarchean metamorphic plutonic rocks, i.e., TTG rocks. The whole-rock geochemical data and relevant parameters of the samples are listed in Table 2, and the detailed characteristics are described as below:
(1) TTG
The chemical analyses of the 18 Neoarchean samples show high SiO2 (60.51–72.38%) and Na2O ((2.95–4.62%), low K2O (1.72–3.32%), MgO (0.93–2.37%), TiO2 (0.22–0.55%), and TFe2O3 (2.30–5.53%), and variable CaO (1.72–7.07%) and Al2O3 (11.42–16.66%), with K2O/Na2O ratios of 0.37–0.94, and Mg# values of 0.34–0.54 (Table 2). Rare earth elements (REEs) for the TTG samples showed a wide range of ΣREE values (55.02–283.11 ppm), light rare earth element (LREE) values from 51.01 to 277.79 ppm, rare earth element (HREE) values from 4.01 to 10.01 ppm, LREE/HREE ratios from 10.73 to 52.22, and (La/Yb)N values from 16.85 to 97.34. The chondrite–normalized REE patterns showed relative enrichment in LREEs, depletion in HREEs, and slightly positive Eu anomalies (Figure 4a). Plotting the data for these TTG samples on primitive mantle normalized spider diagrams indicated that they were enriched in large ion lithophile elements (LILEs; e.g., Rb, Ba, Th, and K) and depleted in high field strength elements (HFSEs; e.g., Ti, Nb, and Ti). Sr was mostly negative anomalies of varying degrees, and a few samples had no or very slightly positive Sr anomalies, indicating the existence of crystallization differentiation of plagioclase and biotite and local enrichment of plagioclase during the magmatic evolution (Figure 4b).
(2) Fine-grained diorite
The four fine-grained samples showed low SiO2 (40.91–44.17%) and Na2O (0.27–0.38%) contents, and intermediate K2O (1.81–3.28%), Al2O3 (10.29–11.72%), CaO (7.24–8.66%), and TFe2O3 (15.60–16.94%) contents, and had relatively high K2O/Na2O ratios of 4.89–9.37 and Mg# value (0.60–0.62) (Table 2). The analysis results of trace and rare earth elements indicated that the diorite had a relatively high content of REEs (93.98–120.70 ppm), relatively enriched LREEs, depleted HREEs (∑LREE/∑HREE = 4.84–5.95, (La/Yb)N = 5.78–7.00), and the fractionation between the LREEs and HREEs was not obvious; δEu was 0.88–1.00, there was no Eu anomaly (Figure 4a). The diorite was relatively enriched in Rb (61.0–115.3 ppm), Ba (175–550 ppm), K (14,000–25,800 ppm) and other large ion lithophile elements and depleted in HFSEs such as Nb (10.0–14.0 ppm), Ta (0.81–1.10 ppm), and P (740–1000 ppm) (Figure 4b). In addition, the diorite rocks had lower Sr/Y values (5.81–9.01) and (La/Yb)N values (5.8–7.0) and higher Y values (21.1–23.4 ppm), which were obviously different from the geochemical characteristics of the adakite rocks, but similar to the typical arc calc–alkaline rocks [41].

4.2. Zircon U–Pb Geochronology

Sample (BHG–N1) is a monzogranitic breccia collected from the Binghugou deposit. The zircons are mainly prismatic and euhedral shapes, with the aspect ratio mostly in the range of 1:1–2:1, and typical oscillatory zones are common (Figure 5a). Th/U ratios are less than 1, except for one result (=1.43), which was consistent with the characteristics of typical magmatic zircons [42]. Fifteen analyses from this sample yielded 207Pb/206Pb ages from 2476 to 2551 Ma (Table 3), defining a weighted mean age of 2498.2 ± 7.5 Ma (mean squared weighted deviation (MSWD) = 0.103) (Figure 6a).
Sample (DJG–N1) is monzogranite collected from the Dajiagou deposit. Most zircons exhibited oscillatory or planar zoning under CL, and the grain size in the range of 100–150 μm with the aspect ratio of 1:1–2:1 (Figure 5b). The Th/U ratios of zircon are mostly 0.44–0.82, characteristic of magmatic zircon. The 207Pb/206Pb age of 14 zircon grains ranges from 2513 to 2550 Ma (Table 3), with the weighted mean age of 2544.7 ± 8.8 Ma (MSWD = 0.09) (Figure 6b).
Sample (DJG–N2) is diorite collected from the Dajiagou deposit. The shape of zircon is mainly stubby prismatic. The zircons are translucent with a grain size of 80–130 μm, and the aspect ratio of 1:1–2:1. Most zircons had typical magmatic oscillation zoning (Figure 5c), and Th/U ratios at 0.14–0.88, indicating that the zircons were magmatic zircons. Thirteen zircon grains yielded concordant 206Pb/238U age of 151 ± 2 to 182 ± 3 Ma (Table 3), with a weighted mean of 169.7 ± 5.1 Ma (MSWD = 0.118) (Figure 6c).
Sample (DXG–N1) is monzogranite collected from the Daxigou deposit. The zircons were mainly prismatic in shape and a few are irregular. The grain size ranges from 100 to 130 μm and the aspect ratio is 1:1–1:2. Most of the zircons are dark, with internal oscillation zoning (Figure 5d). The Th/U ratios (0.10–1.09) exhibit the characteristics of magmatic zircons. The 207Pb/206Pb ages of the 16 zircon grains range from 2492 to 2507 Ma (Table 3) and yielded a weighted mean age of 2501.7 ± 8.3 Ma (MSWD = 0.076) (Figure 6d).
Sample (GLG–N1) is monzogranite collected from the Gaoligou deposit. Most zircon grains are euhedral and elongate with lengths of 90–150 μm and aspect ratio of 1:1 to 1:2. The zircons are mostly translucent with clear magmatic oscillation zoning in the CL images, indicating a magmatic origin (Figure 5e). The 12 analyses show 207Pb/206Pb ages from 2445 to 2467 Ma (Table 3) and yielded a weighted mean age of 2458.0 ± 11.0 Ma (MSWD = 0.11) (Figure 6e).
Sample (ZMG–N1) is trondhjemite collected from the Zhemagou deposit. The zircon grains are subhedral to euhedral, with lengths of 80–130 μm and aspect ratio of 1–2. Most zircons have typical oscillation zoning (Figure 5f) and the Th/U ratios are between 0.35 and 1.01, indicating magmatic origin. The 207Pb/206Pb ages of 15 analytical spots on the zircon grains range from 2489 to 2511 Ma (Table 3), with a weighted mean age of 2500.4 ± 8.3 Ma (MSWD = 0.180) (Figure 6f).

5. Discussion

5.1. Timing of Magmatism in the Liuhe Gold Ore Field

There are some controversies about the timing of gold deposits in the Jiapigou gold belt, with interpreted ages ranging from the Neoarchaean–Palaeoproterozoic, 2475–2469 Ma [17,43], through the Indo-Chinese epoch of the Mesozoic, 204 Ma [44], to the Yanshannian epoch of the Mesozoic, 170–160 Ma [45,46,47,48]. Other scholars have proposed a multi-stage mineralization, 3000–2800 Ma, 2700–2500 Ga, 2000–1800 Ma, 500–300 Ma, 230–130 Ma [49,50,51]. Huang (2012) [52] suggested that the gold mineralization of the Jiapigou gold belt first took place during the Palaeoproterozoic Era (~2426.0 Ma). The Yanshanian gold mineralization event (~166.2 Ma) may also have a major effect on the ore bodies of the Jiapigou gold belt, and this led to new gold mineralization as well as redistribution of the Palaeoproterozoic ore bodies.
The zircon U–Pb dating provides constraints on the formation ages of ore-hosting TTGs. The zircon 207Pb/206Pb ages of ore-hosting TTGs from the GLG, DXG, ZMG, and BHG deposits were 2458.0 ± 11.0, 2501.7 ± 8.3, 2500.4 ± 8.3, and 2498.2 ± 7.5 Ma, respectively. The age of these ore-hosting granites may indicate a large-scale magmatic event in the Liuhe orefield in late Neoarchean to early Paleoproterozoic. The zircon 206Pb/238U age obtained for the ore-hosting fine-grained diorite of the DJG deposit is 169.7 ± 5.1 Ma, indicating that magmatism took place in the early Jurassic. Based on the above data, we propose that emplacement of ore-hosting magma in the Liuhe orefield mainly took place in two epochs: late Neoarchean to early Paleoproterozoic and early Jurassic of Mesozoic.

5.2. Petrogenesis of Archean TTG Series

In the samples collected in this study, except for the diorite in the Dajiagou deposit, all the trondhjemite and monzogranite (monzogranite breccia) belonged to Archean TTG gneisses with relatively clear petrological characteristics, and most of them are of gneissic and/or streaked structure. The mineral composition was quartz + plagioclase (oligoclase) + potassium feldspar + biotite + amphibole. In the TAS classification diagram (Figure 7a), 4 of the 18 samples fell into the diorite field, 10 into the granodiorite, and 4 into the granite. This indicates that most of the TTG rocks belong to the granodiorite [53]. The major elements show a linear distribution in the Harker diagram (Figure 8); SiO2 has negative correlations with MgO, TiO2, Fe2O3, CaO, and P2O5, reflecting the characteristics of typical magmatic evolution, while K2O, Na2O, and Al2O3 have no significant correlations with SiO2, showing the characteristics of Archean TTG rocks. According to the molar ratios of Al2O3/(CaO + Na2O + K2O) and Al2O3/(Na2O + K2O), most samples are peraluminous, with a few samples being metaluminous in the A/CNK vs. A/NK diagram (Figure 7b) [54]. In the K2O vs. SiO2 diagram (Figure 7c), except for a few samples, most fell into the high-K calc–alkaline series and calc–alkaline series, indicating that they were calc–alkaline series rocks [55]. In the Nb vs. 10,000 × Ga/Al diagram, all samples were plotted within the fields of I- and S-type granites (Figure 7d), indicating that the TTG rocks have an affinity to those of the I-type suite [56]. The trondhjemite and monzogranite have similar REE distribution patterns, both of which show that the fractionation degree of light and heavy REEs increases gradually, indicating that they belong to a homologous magmatic evolution process and the magmatic differentiation degree gradually increases [57,58].
Adakite is a petrological term introduced to refer to a special type of island-arc andesite, dacite, rhyolite (dacite is the most common), or tonodiorite and trondhjemite in the Cenozoic island-arc environment associated with the young subducted oceanic lithosphere [59,60]. The geochemical characteristics of the adakites are SiO2 ≥ 56% and Al2O3 ≥ 15%, and MgO is usually less than 3% (rarely more than 6%). They are rich in Na+, with Na2O and K2O contents in the range of ±4 and ±1–2%, generally Na2O > K2O. The contents of Y and Yb are relatively low, at <18 and <1.9 ppm, respectively. It shows positive Eu and Sr anomalies, with the Sr > 400 ppm. Adakite is formed by the partial melting of slab during subduction at a small angle and is used as a marker to identify subduction. The TTG rocks in the study area exhibited the following characteristics: SiO2 content varied from 62.99 to 70.67%, with higher A12O3 (12.58 to 15.71%) and Na2O/K2O ratios (1.16 to 2.9), and lower MgO (0.93 to 2.73%) and Mg# value. Trace elements showed a positive Eu anomaly and low Y and Yb content, and the Sr/Y ratios were high (22.3–79.6). The TTGs fall into the adakite field according to the Sr/Y–Y discriminant diagram (Figure 9a) [61], indicating that they belong to the modern island-arc adakite rocks [52].
At the same time, the Neoarchean TTG in the study area had high SiO2, while Mg#, Cr and Ni were low, indicating that the parent magma of the Neoarchean TTG did not interact with the mantle peridotite; the magma was mainly derived from the dehydration and partial melting of garnet amphibolite, and the contribution of mantle components was not obvious [65]. Because the temperature of the Archean mantle was much higher than that of the present, the softening and melting of the Archean oceanic crust occurred once subduction took place, making the subduction of the Archean ocean plate quite different from that of the modern ocean plate, and low angle gentle subduction occurred in the majority of cases [61]. The thin or undeveloped mantle wedge above the gently subducted oceanic crust resulted in a small contribution of mantle components to Archean TTG rocks, generally showing low Mg# values. The major rock formations of the Archean are composed of greenstone belt and TTG gneiss. The widespread occurrence of olivine komatiites in greenstone belts around the world indicates that the temperature of the Archean mantle and the melting degree of mantle magma were much higher than today. Therefore, the average composition of the Archean oceanic crust was also more basic than that of the present, and it can be inferred that the magma produced by the melting of mantle or oceanic crust caused by Archean plate subduction was also more basic than that of island-arc volcanic rocks currently. The partial melting of mafic rocks in the lower crust caused by basaltic magma underplating is the main mechanism for the formation of granitic rocks in the modern island arcs and active continental margins. The TTG rocks in the study area contained amphibolite inclusions with different basic degrees, which were metamorphosed by the products of basaltic magma underplating the subduction background. Based on the above analysis, we suggest that the TTG series in the study area may have derived from the partial melting of mafic lower crustal caused by the underplating of basaltic magma on the island-arc or active continental margin, and its formation is similar to the current generation mechanism of granitic magma under the same tectonic setting.

5.3. Tectonic Setting of the Magmatism in the Liuhe Area

The Neoarchean TTG rock series from the Liuhe area is a series of intermediate-acidic metaluminous–peraluminous calc–alkaline rocks, and their geochemical characteristics are close to those of the island-arc or continental margin-arc setting in the Phanerozoic [54]; most of the samples fell into the adakite area in the Sr/Y–Y discrimination diagram [66]. From the perspective of structural geology, adakite can be used as a magmatic marker to identify the subduction zone [67]. Relevant studies have pointed out that the NCC is different from the ancient continental crust and has the characteristics of island arc [68] and thus inferred that tectonism similar to modern plate subduction had occurred in the Mesoarchean. Although the oldest rocks found in the NCC were quartzite and felsic gneiss, the island-arc attribute of the initial continental crust does not exclude the early continental crust having a horizontal accretion mode, that is, the vast cratonic continental block formed by a series of island-arc collisions and aggregations [69]. Geng et al. (2012) [70] also noted that the formation of TTG intrusive rocks in the NCC was about 100 Ma earlier than regional metamorphism, which can be explained by the collision process after subduction. The emplacement age of TTG rock was 2515–2551 Ma in this study, which was basically consistent with the previous results, indicating that there was intense and extensive magmatism in the Liuhe area at the end of the Neoarchean [71,72]. According to the R1–R2 discrimination diagram (Figure 9b), the collected samples were mainly plotted in the area of pre-plate collision [58,61]. Nearly all the rocks fell in the VAG field in the Rb–Y + Nb diagram (Figure 9c), [and the VAG + Syn–COLG field in the Nb–Y diagram (Figure 9c) [62]. All samples were far from within-plate granite (WPG) and ocean-ridge granite (ORG) areas, indicating that the magmatism was related to plate subduction. The above features suggested a subduction-related arc signature, and it is widely accepted that the TTG rocks were derived from subducted oceanic crust [73]. Therefore, the Neoarchean ore-bearing TTG series in the Liuhe area was likely formed in an island-arc or active continental margin setting before plate collision.
The formation of metamorphic plutonic intrusive rocks indicated that the Liuhe area had experienced the formation, thickening, collision–subduction, and melting of the ancient continental crust in the Neoarchean–Paleoproterozoic, reflecting the continuous growth and maturation of the Archean crust. The source of partial melting gradually moved upward from the early upper mantle to the lower crust and upper crust and represented an important process of continental crust horizontal accretion in the late Neoarchean [74]. In the Precambrian crustal evolution of the North China plate, ca. 2.6 Ga was the period in which various geological processes occurred intensively, and ca. 2.5 Ga was the main activity period of TTG magma.
Under the subduction of the Pacific plate in the Mesozoic, the eastern part of China was characterized by intense volcanic eruption, magmatic intrusion, and tectonic movement. Because of the northwest migration, subduction, and collision of the Pacific plate, the North China plate has undergone a remarkable counterclockwise rotation. The tectonic stress in this area is manifested as the sinistral translation of the NE-trending Dunmi fault and its secondary Liangjiang fault, leading to large-scale regional folding of the existing Jiapigou fault in the process of sinistral torsion. A series of tensional NNE–NE-trending faults are derived at the turning end of the fold, while the NS-trending faults are in a compressive state; therefore, there is no NS-trending ore body. Indosinian magmatic activity occurred in the Liuhe area in the early Mesozoic, and the magmatic rocks represented by Wudaokuohe granite body intruded into place. In the Yanshanian, hypabyssal, and ultra-hypabyssal rhyolites, quartz porphyry, granite porphyry, and other magmatic emplacement occurred. The ore-controlling structure of the Jiapigou gold belt, the NW-trending ductile–brittle shear zone, has extended to the Liuhe area in the southeast direction, and the Dajiagou gold deposit is now located in the southeast extension of the ore-controlling structure. At the same time, the subduction of the Pacific plate also formed NE-trending faults, which cut the ductile–brittle shear zone and ore body formed in the earlier period, causing certain damage to the ore body. Therefore, there are relatively few Archean deposits in the Liuhe orefield and even the entire Jiapigou gold belt.

5.4. Archean Gold Transport in the Liuhe Gold Orefield

Considering the theories of Precambrian gold mineralization at home and abroad and the comprehensive research results of the geological characteristics of various gold deposits in the study area [5,48,75,76,77], we suggest the following scenario for the initial Au enrichment of the Liuhe gold orefield. The metamorphic supracrusts of the late Mesoarchean in this area belong to the basic volcanic formation, accompanied by a small amount of ferrosilicon quartzite sedimentary formation, and it is well known that the Archean basic volcanic formations have gold-bearing properties [3,6,78,79,80,81]. The upwelling of mantle under the original Longgang old landmass led to thinning and rifting of the upper crust, and the greenstone belt was formed by the eruption accumulation and clastic deposition of a large number of tholeiite and felsic volcanic rocks [64,82,83]. The subcontinental lithospheric mantle (SCLM) was metasomatized multiple times by Au-enriched melts and fluids before subducting beneath the NCC [84]. Fluids derived from dehydration during the oceanic crust subduction additionally metasomatized the cratonic SCLM with incompatible and fluid-mobile elements, including Au and Pb [85], and the entry of a large amount of subduction fluids not only triggered partial melting of the SCLM, but also provided an effective medium to remove the incompatible elements from the modified SCLM [86,87,88,89]. The resulting Au-enriched melt then underplated the cratonic mafic lower continental crust (LCC). With the intensifying of continent–continent collision and arc–continent collision, TTG granitic magma continued its upwelling, emplacement, and anatexis. From the late Neoarchean to early Paleoproterozoic, the intensification of metamorphism and deformation caused the schistosity and mylonization of the metamorphic supracrusts and felsic gneiss, forming a large-scale ductile shear zone in the Liuhe area and even the entire Jiapigou gold ore belt [44,90,91]. With the intensification of tectonic activity and uplift of terrane, the ductile shear zone was transformed into a ductile–brittle shear zone, resulting in the dynamic metamorphism of the initial tectonic cataclasite [92]. A large amount of granite magma rose along the multi-stage large-scale ductile shear zone system, differentiated a large amount of magmatic fluid, mixed with the fluid enriched in ore-forming materials, and activated the Au in the gold-bearing metamorphic rocks, then migrated to the shear zone through the water–rock interaction [93,94]. Under these conditions, shallow water and metamorphic hydrothermal fluids circulated and migrated along the tectonic belt owing to the development of rock fissures and the increase in porosity, causing the rocks in the tectonic belt to undergo the intergranular dialysis, which triggered further activation and migration of gold [43,63]. By using the secondary structure of the ductile shear zone as the ore hosting, the ore-forming materials were enriched and precipitated, and eventually formed gold ore bodies (Figure 10).

6. Conclusions

  • The zircon ages of ore-hosting TTGs and fine-grained diorite indicated that the large-scale ore-hosting magma emplacement in the Liuhe orefield mainly took place in two epochs: late Neoarchean to early Paleoproterozoic and early Jurassic of Mesozoic.
  • The Neoarchean TTGs in the Liuhe area comprise a series of intermediate-acidic metaluminous–peraluminous calc–alkaline rocks, which belong to the modern island-arc adakite rocks.
  • The Ca. 2.5 Ga was the main activity period of TTG magma in the Liuhe area, the ore-hosting TTGs were derived from the partial melting of mafic lower crustal caused by the underplating of basaltic magma on the island-arc or active continental margin before plate collision.
  • The magmatism of the Dajiagou deposit occurred in an active continental margin setting associated with the westward subduction of the paleo-Pacific plate beneath the Eurasian plate during the early Jurassic of Mesozoic period.

Author Contributions

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

Funding

This research received no external funding.

Data Availability Statement

The data provided in this study can be obtained from the figures and the tables in the article.

Acknowledgments

The authors are most grateful to the staff of the ALS Chemex, Guangzhou, China, as well as the laboratory of Hebei Institute of Regional Geology and Mineral Resources Survey, Langfang, China and the MLR Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Jilin University, Changchun, China, during the zircon U–Pb dating and geochemical analyses. The authors deeply appreciate the kind and critical constructive comments and suggestions from the editor-in-chief and two anonymous reviewers, which greatly improved the quality of our manuscript.

Conflicts of Interest

The authors declare no conflict of interest.

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Minerals 12 01121 g001 550
Figure 1. (a) General map showing the location of NE China, modified after Safonova and Santosh (2014) [22]; (b) tectonic sketch map of NE China (modified after Wu et al., 2011) [23]; (c) regional geological map of the Jiapigou gold ore belt, NE China. Showing the distribution of the major gold deposits (modified after Zeng et al., 2017) [24].
Figure 1. (a) General map showing the location of NE China, modified after Safonova and Santosh (2014) [22]; (b) tectonic sketch map of NE China (modified after Wu et al., 2011) [23]; (c) regional geological map of the Jiapigou gold ore belt, NE China. Showing the distribution of the major gold deposits (modified after Zeng et al., 2017) [24].
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Figure 2. Simplified geological map of the Liuhe gold orefield, NE China.
Figure 2. Simplified geological map of the Liuhe gold orefield, NE China.
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Minerals 12 01121 g003 550
Figure 3. Representative outcrop and photomicrographs (cross-polarized light) for representative igneous rocks in the Liuhe gold Orefield, NE China: (a) spatial relationship between monzogranite and ductile shear zones; (b) auriferous quartz veins in the ductile shear zones; (c) spatial relationship between ductile shear zones and altered fine-grained diorite; (d) monzogranitic breccia (BHG-N1); (e) trondhjemite (ZMG-N1); (f) pyrite in diorite (DJG-N2); (g) photomicrograph of monzogranite (GLG-N1); (h) photomicrograph of monzogranitic breccia (BHG-N1); (i) photomicrograph of trondhjemite (ZMG-N1). Pl: plagioclase; Kfs: Kfeldspar; Qz: quartz; Bi: biotite; Ser: Sericite Py: pyrite.
Figure 3. Representative outcrop and photomicrographs (cross-polarized light) for representative igneous rocks in the Liuhe gold Orefield, NE China: (a) spatial relationship between monzogranite and ductile shear zones; (b) auriferous quartz veins in the ductile shear zones; (c) spatial relationship between ductile shear zones and altered fine-grained diorite; (d) monzogranitic breccia (BHG-N1); (e) trondhjemite (ZMG-N1); (f) pyrite in diorite (DJG-N2); (g) photomicrograph of monzogranite (GLG-N1); (h) photomicrograph of monzogranitic breccia (BHG-N1); (i) photomicrograph of trondhjemite (ZMG-N1). Pl: plagioclase; Kfs: Kfeldspar; Qz: quartz; Bi: biotite; Ser: Sericite Py: pyrite.
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Figure 4. Chondrite-normalized REE pattern (a) and primitive mantle (PM) normalized spider diagram (b) for the TTG gneisses and diorites in the Liuhe deposits. Primitive mantle and chondrite values are from McDonough and Sun (1995) [40] and Sun and McDonough (1989) [39], respectively.
Figure 4. Chondrite-normalized REE pattern (a) and primitive mantle (PM) normalized spider diagram (b) for the TTG gneisses and diorites in the Liuhe deposits. Primitive mantle and chondrite values are from McDonough and Sun (1995) [40] and Sun and McDonough (1989) [39], respectively.
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Figure 5. Cathodoluminescence (CL) images of represented analyzed zircons from the TTG gneisses and diorite samples in the Liuhe orefield.
Figure 5. Cathodoluminescence (CL) images of represented analyzed zircons from the TTG gneisses and diorite samples in the Liuhe orefield.
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Figure 6. Concordant diagrams showing U–Pb data and mean age of zircons from the Liuhe orefield, NE China.
Figure 6. Concordant diagrams showing U–Pb data and mean age of zircons from the Liuhe orefield, NE China.
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Figure 7. (a) The chemical classification and nomenclature of plutonic rocks using the total alkalis versus silica (TAS) diagram [53]; (b) A/NK vs. A/CNK [54]; (c) K2O vs. SiO2 [55]; (d) diagrams of Nb vs. 10,000 × Ga/Al of A-type granites from I- and S-type granites [56].
Figure 7. (a) The chemical classification and nomenclature of plutonic rocks using the total alkalis versus silica (TAS) diagram [53]; (b) A/NK vs. A/CNK [54]; (c) K2O vs. SiO2 [55]; (d) diagrams of Nb vs. 10,000 × Ga/Al of A-type granites from I- and S-type granites [56].
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Figure 8. Harker variation diagrams for the TTG gneisses in the Liuhe deposits.
Figure 8. Harker variation diagrams for the TTG gneisses in the Liuhe deposits.
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Figure 9. (a) Sr/Y-Y diagrams for the dioritic gneisses adapted from Martin (1999) [61]; (b) R1 vs. R2 diagram (after Batchelor et al., 1985; Qu et al., 2004) [62,63], R1 = 4Si − 11(Na + K) − 2(Fe + Ti) (mol), R2 = 6Ca + 2 Mg + Al (mol); Discrimination diagrams for granitic rocks after Pearce et al. (1984) [64], (c) Rb-Y + Nb diagram and (d) Nb-Y diagram. VAG: volcanic-arc granites; syn-COLG: syn-collisional granites; WPG: within plate granites; ORG: ocean-ridge granites.
Figure 9. (a) Sr/Y-Y diagrams for the dioritic gneisses adapted from Martin (1999) [61]; (b) R1 vs. R2 diagram (after Batchelor et al., 1985; Qu et al., 2004) [62,63], R1 = 4Si − 11(Na + K) − 2(Fe + Ti) (mol), R2 = 6Ca + 2 Mg + Al (mol); Discrimination diagrams for granitic rocks after Pearce et al. (1984) [64], (c) Rb-Y + Nb diagram and (d) Nb-Y diagram. VAG: volcanic-arc granites; syn-COLG: syn-collisional granites; WPG: within plate granites; ORG: ocean-ridge granites.
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Figure 10. Gold mineral transport model within Neoarchean TTG in the Liuhe orefield (after [95]). UCC-upper continental crust; LCC-lower continental crust; SCLM-subcontinental lithospheric mantle.
Figure 10. Gold mineral transport model within Neoarchean TTG in the Liuhe orefield (after [95]). UCC-upper continental crust; LCC-lower continental crust; SCLM-subcontinental lithospheric mantle.
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Table
Table 1. Simplified locations and petrological characteristics for the samples from the Liuhe orefield, NE China.
Table 1. Simplified locations and petrological characteristics for the samples from the Liuhe orefield, NE China.
Sample No.LithologyLocationTexture/StructureMineral Assemblage
BHG-N1Monzogranitic brecciaBinghugou gold depositbrecciform structureKfs(35%) + Pl(30%) + Qz(25%) + Bi(5%)
DJG-N1MonzograniteDajiagou gold depositmedium-grain texture, massive structureKfs(35%) + Pl(30%) + Qz(25%) + Bi(5%)
DJG-N2DioriteDajiagou gold depositfine-grained texture, massive, veined structurePl(50%) + Hb(35%) + Kfs(10%) + Qz(5%)
DXG-N1MonzograniteDaxigou gold depositmedium-grain texture, massive structureKfs (40%) + Pl(30%) + Qz(25%)
GLG-N1MonzograniteGaoligou gold depositmedium-grain texture, gneissic structureKfs(35%) + Pl(25%) + Qz(25%) + Bi(10%)
ZMG-N1TrondhjemiteZhemagou gold depositmedium-grain texture, massive structurePl(50%) + Qz(35%)+ Bi(10%)
Note. Kfs: K-feldspar; Pl: plagioclase; Qz: quartz; Bi: biotite; Hb: hornblende.
Table
Table 2. Whole-rock major (wt.%) and trace element (ppm) compositions of TTG gneisses and diorites from the deposits in the Liuhe orefield.
Table 2. Whole-rock major (wt.%) and trace element (ppm) compositions of TTG gneisses and diorites from the deposits in the Liuhe orefield.
SampleGLG-N1-Q1GLG-N1-Q2GLG-N1-Q3GLG-N1-Q4DJ-N1-Q1DJ-N1-Q2DJ-N1-Q3DJ-N2-Q1DJ-N2-Q2DJ-N2-Q3DJ-N2-Q4
SiO265.2967.2761.6667.0865.8863.9263.7042.5343.9244.1740.91
Al2O316.2815.4616.6616.0715.2615.9115.1311.7210.2910.8910.87
Fe2O3T4.204.915.413.684.674.745.0915.8815.8815.6016.94
CaO3.583.374.453.586.117.075.467.248.668.387.47
MgO2.041.282.731.772.142.572.0612.7012.5511.7513.55
K2O1.871.881.911.721.741.792.353.281.812.771.86
Na2O4.554.154.524.624.303.313.360.350.270.360.38
MnO0.060.050.100.050.120.120.100.200.220.280.22
TiO20.440.460.380.400.500.470.552.191.862.032.68
P2O50.180.150.260.160.080.110.090.200.180.160.23
LOI1.530.781.691.310.691.041.481.171.891.141.81
Rb117.574.4110.0104.580.686.7107.0115.370.9113.561.0
Sr337350358335221238298210133131193
Ba26278825024810183142550175258309
V326736279195136369337357448
Cr7041696725222327410409108701020
Nb15.88.612.214.44.74.74.212.712.110.014.0
Ta0.820.590.500.690.200.300.290.830.950.811.10
Zr3362022052919598105163153135174
Hf8.34.94.87.22.22.42.64.24.53.95.2
Th2.9212.102.602.582.184.707.782.452.241.992.58
U1.450.670.741.420.300.320.640.450.420.270.39
Pb11.215.211.512.82670106.5140.082.696.129.943.6
Co11.311.013.311.121.917.621.188.880.869.6114.0
Zn80839564312118188256252173298
Sn1.01.61.01.11.21.21.11.92.11.41.4
Ni34.311.938.335.296.5103.5121.5440.0461.0375.0535.0
Li11.36.410.410.112.37.88.663.223.921.470.4
Mo1.641.731.011.512.232.541.970.850.810.851.11
La26.138.532.825.515.520.623.418.016.314.419.2
Ce47.870.965.646.129.238.245.142.835.732.643.5
Pr5.037.647.534.833.374.345.205.975.104.515.99
Nd17.326.027.216.612.916.019.326.123.320.126.1
Sm2.484.034.512.072.452.973.466.265.935.076.24
Eu0.931.111.110.960.841.150.811.862.011.581.81
Gd1.742.843.381.692.192.482.666.006.235.106.20
Tb0.220.330.390.210.320.340.360.870.970.770.90
Dy1.101.752.161.071.621.901.974.715.314.695.02
Ho0.220.310.420.220.300.350.350.850.960.860.87
Er0.670.801.170.590.760.870.972.222.352.102.44
Tm0.100.120.170.090.100.110.140.300.320.280.31
Yb0.740.731.130.610.620.630.831.791.851.681.85
Lu0.120.100.180.100.080.090.130.240.280.240.27
Y6.28.011.45.88.49.89.923.322.821.123.4
ΣREE104.6155.2147.8100.670.390.0104.7118.0106.694.0120.7
ΣLREE99.6148.2138.896.164.383.397.3101.088.378.3102.8
ΣHREE4.97.09.04.66.06.87.417.018.315.717.9
LREE:HREE20.321.215.421.010.712.313.15.94.85.05.8
(La:Sm)N6.66.04.67.74.04.44.31.81.71.81.9
(La:Yb)N23.835.619.628.216.922.019.06.85.95.87.0
Mg#0.490.340.500.490.480.520.450.620.610.600.62
δEu1.31.00.81.51.11.30.80.91.00.90.9
δCe0.90.91.00.90.90.90.91.00.91.01.0
SampleDXG-N1-Q1DXG-N1-Q2DXG-N1-Q3DXG-N1-Q4BHG-N1-Q1BHG-N1-Q2BHG-N1-Q3BHG-N1-Q4ZMG-N1-Q1ZMG-N1-Q2ZMG-N1-Q3
SiO265.9060.5162.2362.0472.1770.3670.7872.3863.3365.3063.42
Al2O314.3613.4811.4213.8014.5814.1614.8814.2214.8814.9415.38
Fe2O3T4.305.454.435.012.303.552.482.395.034.315.53
CaO1.774.095.323.472.101.932.211.723.172.882.95
MgO1.622.382.562.110.981.261.200.932.131.622.15
K2O2.932.782.662.232.802.392.371.913.323.162.66
Na2O3.543.173.223.323.752.953.903.383.523.483.45
MnO0.040.060.080.050.020.030.020.020.050.050.06
TiO20.490.500.330.460.350.290.420.220.450.390.53
P2O50.100.110.090.100.090.110.090.070.170.160.27
LOI 10000.891.940.530.241.251.201.271.110.670.100.06
Rb108.0167.0139.0166.879.7112.580.9104.081.588.6103.5
Sr184116145125348459354414398421489
Ba32623520825483013606711180106512801205
V8989548034463328726563
Cr8089518640574042988087
Nb5.35.73.35.23.62.74.32.16.16.09.5
Ta0.490.500.310.390.230.200.200.050.400.400.64
Zr25123615722613918689138167173106
Hf7.06.64.36.24.25.22.63.84.94.83.1
Th13.801.300.432.6121.615.808.477.631.191.372.05
U0.530.510.330.450.320.330.190.250.410.400.41
Pb14.27.699.410.618.622.816.921.411.914.614.0
Co18.013.89.013.36.57.47.66.015.410.713.6
Zn5766626336424433715975
Sn0.60.60.60.61.11.11.11.01.00.91.0
Ni32.637.427.338.518.315.723.812.229.521.629.4
Li24.910.65.211.09.09.010.88.522.412.627.8
Mo0.991.911.071.430.980.830.860.991.571.231.32
La82.321.913.825.546.539.838.332.730.527.035.3
Ce136.537.123.342.966.261.452.146.952.445.864.9
Pr13.403.912.544.436.746.185.434.656.025.197.79
Nd39.813.68.814.320.620.116.814.820.818.628.1
Sm4.281.921.672.012.743.012.472.203.022.884.28
Eu1.511.050.901.011.331.391.291.421.211.271.40
Gd2.381.781.431.531.902.211.711.582.212.213.63
Tb0.240.200.190.180.240.290.230.210.290.290.47
Dy1.181.090.990.971.161.511.131.071.601.602.46
Ho0.210.220.190.180.200.270.200.190.300.330.48
Er0.550.630.530.510.530.660.490.490.860.981.33
Tm0.080.090.080.080.070.100.070.070.130.150.20
Yb0.570.610.510.570.420.630.420.410.910.931.25
Lu0.110.110.090.100.070.100.070.070.160.150.19
Y5.25.25.34.95.17.24.95.28.68.413.0
ΣREE283.184.255.094.3148.7137.7120.7106.8120.4107.4151.8
ΣLREE277.879.551.090.2144.1131.9116.4102.7114.0100.7141.8
ΣHREE5.34.74.04.14.65.84.34.16.56.610.0
LREE:HREE52.216.812.721.931.422.926.925.117.615.214.2
(La:Sm)N12.17.25.28.010.78.39.89.36.45.95.2
(La:Yb)N97.324.218.230.274.642.661.553.822.619.619.0
Mg#0.430.470.540.460.460.420.490.440.460.430.44
δEu1.31.71.71.71.71.61.82.21.41.51.1
δCe0.90.90.90.90.80.80.80.80.90.90.9
Note: LOI = loss on ignition. Mg# = 100 × molar Mg2+/(Mg2+ + Fe2+). TFeO = FeO + 0.8998 × Fe2O3. A/CNK = molar Al2O3/(CaO + Na2O + K2O); letter N in footnote means normalization to chondrite, and the value referred to Sun and Mcdonough (1989) [39].
Table
Table 3. Results of LA-ICPMS U–Pb dating for the single-grain zircon from the TTG gneisses and diorite samples in the Liuhe orefield.
Table 3. Results of LA-ICPMS U–Pb dating for the single-grain zircon from the TTG gneisses and diorite samples in the Liuhe orefield.
AnalysisContent (ppm)Isotopic RatiosIsotopic Ages (Ma)
No.PbThUTh/U207Pb/206Pb1σ207Pb/235U1σ206Pb/238U1σ206Pb/238U1σ207Pb/235U1σ207Pb/206Pb1σ
BHG-N1-0189458314040.420.16420.002511.15600.19810.49200.0058257925253617250015
BHG-N1-023644484700.950.16450.002911.03710.19410.48480.0065254828252616250314
BHG-N1-033884864950.980.16450.002310.94760.17120.48300.0052254123251915250213
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MDPI and ACS Style

Zhang, J.; Yang, Y.; Guo, P.; Wutiepu, W. Zircon U–Pb Age and Geochemistry of Ore-Hosting Rocks from the Liuhe Orefield of the Jiapigou Gold Ore Belt, NE China: Magmatism and Tectonic Implications. Minerals 2022, 12, 1121. https://doi.org/10.3390/min12091121

AMA Style

Zhang J, Yang Y, Guo P, Wutiepu W. Zircon U–Pb Age and Geochemistry of Ore-Hosting Rocks from the Liuhe Orefield of the Jiapigou Gold Ore Belt, NE China: Magmatism and Tectonic Implications. Minerals. 2022; 12(9):1121. https://doi.org/10.3390/min12091121

Chicago/Turabian Style

Zhang, Jian, Yanchen Yang, Piyi Guo, and Wukeyila Wutiepu. 2022. "Zircon U–Pb Age and Geochemistry of Ore-Hosting Rocks from the Liuhe Orefield of the Jiapigou Gold Ore Belt, NE China: Magmatism and Tectonic Implications" Minerals 12, no. 9: 1121. https://doi.org/10.3390/min12091121

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