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Article

Petrogenesis and Tectonic Setting of Early Cretaceous A-Type Granite from the Southern Great Xing’an Range, Northeastern China: Geochronological, Geochemical, and Hf Isotopic Evidence

by
Xiangjin Ran
1,
Xi Wang
1,2,* and
Zhenming Sun
3
1
College of Earth Sciences, Jilin University, Changchun 130061, China
2
Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of Natural Resources of China, Changchun 130026, China
3
Changchun Institute of Technology, Changchun 130012, China
*
Author to whom correspondence should be addressed.
Minerals 2023, 13(12), 1523; https://0-doi-org.brum.beds.ac.uk/10.3390/min13121523
Submission received: 26 September 2023 / Revised: 17 November 2023 / Accepted: 4 December 2023 / Published: 6 December 2023
(This article belongs to the Section Mineral Geochemistry and Geochronology)
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Abstract

:
The southern Great Xing’an Range is located in the eastern Central Asian Orogenic Belt, where voluminous igneous rocks developed during the Late Mesozoic period. The east slope of the southern Great Xing’an Range has been the topic of numerous debates on the level of influence of the Mongol-Okhotsk and the Paleo-Pacific regimes in the Late Mesozoic period. Therefore, this area is a suitable region in which to study the temporal changes in magma sources and tectono-magmatic evolution. In this paper, whole-rock geochemical data, zircon U-Pb geochronology, and zircon Hf isotope studies were carried out on the granitoids in the east slope area of the southern Great Xing’an Range. LA-ICP-MS zircon U-Pb dating revealed the ages of four granitoid samples: 135.0 ± 0.6 Ma, 130.7 ± 1.4 Ma, 130.4 ± 1.0 Ma, and 127.6 ± 0.8 Ma, respectively. The Hf isotope values 176Hf/177Hf = 0.282751–0.283015, εHf (t) = +2.0~+11.5, and T2DM = 583~1442 Ma suggest that the magma was generated by partial melting of Meso- and Neoproterozoic accreted and thickened low crust. The whole-rock geochemical data implied that these granitoids are A-type granite and their formation is closely linked to the subduction of the Paleo-Pacific Ocean plate. These geochemical, isotopic, and geochronological data suggest that the Early Cretaceous magmatism in the east slope area of the southern Great Xing’an Range formed in an extensional back-arc tectonic setting associated with the slab roll-back of the Paleo-Pacific plate subduction.

1. Introduction

A-type granite, first defined by Loiselle and Wones [1], is characterized as alkaline, anhydrous, and anorogenic and has always been one of the most important research topics in the field of granite. Many scholars have proposed multiple petrogeochemical indexes and classification schemes to characterize the diversity of A-type granite, which is mainly reflected in petrogenesis and tectonic settings [2,3,4,5,6,7]. A-type granite has changed significantly since its original conception due to more extensive research [8,9]. Currently, the rock types include not only alkali feldspar granite and alkaline granite, but also metaluminous and peraluminous granite [10]. The formation of A-type granite involves different processes, different tectonic settings, and different source areas, so it is of great geological significance to study A-type granite. Furthermore, Eby [10] subdivided A-type granite into two chemical subgroups, A1 and A2, based on trace element abundances and ratios. The A1-type (Y/Nb < 1.2) represents magma sources originated from the intraplate or rift-zone setting; the A2-type (Y/Nb > 1.2) represents magma derived from post-orogenic or post-collisional environment magmatism.
The eastern part of the Central Asian Orogenic Belt (CAOB) in northeastern (NE) China (Figure 1a) consists of four major micro-continental blocks, including the Erguna, Xing’an, Songnen, and Jiamusi blocks, from north to south (Figure 1b) [11,12]. The southern Great Xing’an Range (GXR), located in the eastern part of the CAOB, is an important geotectonic unit in NE China bound by the Hegenshan–Heihe Fault to the north and the Solonker–Xra Moron suture to the south and bordered by the Songliao Basin to the east. (Figure 1b) [13,14]. There are voluminous Hercynian, Indosinian, and Yanshanian granitic plutons distributed as NNE and NE directions in this region (Figure 1c,d). This area is an ideal location for investigating temporal changes in magma source regions and tectono-magmatic evolution processes. Numerous studies have been carried out on geochronology, petrogenesis, tectonic settings, and the tectonic evolution of the late Mesozoic period [15,16,17,18,19,20,21,22,23]. However, some controversy surrounds the Late Mesozoic tectonic setting in this region as numerous scholars consider the post-orogenic extension following the subduction of the Mongol-Okhotsk Ocean [24,25,26,27], and others believe that the Early Cretaceous magmatic activity was closely related to the subduction of the Paleo-Pacific Ocean Plate [17,18,19,28,29,30,31,32,33]. This controversial and invoked viewpoint is indicative of the complex tectonic evolution of this area during the Late Mesozoic period. The controversy is the result of a lack of understanding of the effect of the region scope of the Mongol-Okhotsk and the Paleo-Pacific regimes in the different periods. The study area, which is located on the border of the GXR and the Songliao Basin, is key to the highly contested effects of the region scope of the two regimes in the Late Mesozoic period, particularly the Early Cretaceous period. Zhu [34] and Tian et al. [35] considered that the Paleo-Pacific regimes’ effect scope can reach the western part of the GXR based on the features of the gravity lineament in NE China. Additionally, Han et al. [22] suggested that the effect scope of the Paleo-Pacific regimes extending to the GXR was unreasonable because the study area is too far from the Pacific trench (>1300 km). Therefore, this study investigates the spatiotemporal variation in the east slope area of the southern GXR (Figure 1d) and provides high-precision zircon U–Pb, whole-rock major and trace element compositions, and Hf isotopes of intrusive rocks. These data, together with previously published data, allow us to explain the emplacement age, petrogenesis, and sources and further explore the tectonic setting of the GXR.

2. Regional Geology and Sample Description

2.1. Regional Geology

The southern GXR is located in eastern Inner Mongolia, NE China. It is bounded by the Hegenshan–Heihe Fault in the north and the Solonker-Xra Moron Suture in the south, and it is adjacent to the Songliao Basin in the east (Figure 1b). Its history includes the closure of the Paleo-Asian Ocean between the Siberian Craton in the north and the North China Craton in the south during the Paleozoic period [37] and the superposition of the Mongol-Okhotsk Ocean and Paleo-Pacific Ocean tectonic systems during the Mesozoic period [15,38]. Stratigraphy and widespread Permian and Mesozoic volcano sedimentary succession constitute the major body of the southern GXR. The Lower Permian Shoushangou Formation (P1s) is mainly composed of thick-bedded limestone with chert nodules; the Middle Permian Dashizhai Formation (P2d), consists of intermediate-to-acidic lava, rhyolite, and volcaniclastics; the Middle Permian Zhesi Formation (P2zs) is composed of silty mudstone and tuffaceous silty sandstone; and the Upper Permian Linxi Formation (P3l) consists of sandy conglomerate. The Middle Jurassic Xinmin Formation (J2x) is composed of sandy conglomerate and tuff. The Upper Jurassic Manketouebo Formation (J3m) is composed of rhyolitic tuff, while the Upper Jurassic Manitu Formation (J3mn) is composed of andesite clastic rocks. The Lower Cretaceous Baiyingaolao Formation (K1b) is composed of rhyolite, and the Lower Cretaceous Meiletu Formation (K1m) comprises a suite of basaltic andesite, andesite, and trachyte (Figure 1d) [22,39,40]. In this region, intrusive rocks are mainly composed of voluminous Paleozoic (Hercynian) and Mesozoic (Indosinian and Yanshanian) granitoids, and the Early Yanshanian granites are distributed in the NNE and NE directions [41,42,43,44] (Figure 1c). Recently obtained geochronological data indicate multiple episodes of granitic magmatism in this region, with the majority formed in the Cretaceous, Jurassic to Triassic, Devonian to Cambrian, and lesser Neoproterozoic periods [15]. Most of the W, Sn, Mo, Ag, Pb, Zn, and Cu deposits in the region are associated with Indosinian and Yanshanian granites [45,46,47].

2.2. Sample Descriptions

Since the distribution of granite in the study area is relatively dispersed, we selected four relatively large-scale rock masses and typical granitoids for sampling (Figure 1d) and numbered them D5092 (44°34′18″ E, 119°46′00″ N), PM103 (44°32′22″ E, 120°13′22″ N), PM104 (44°32′44″ E, 120°11′23″ N), and PM105 (44°45′31″ E, 120°04′37″ N), respectively. The sampling locations are listed in Figure 1d. More petrography for granitoids is detailed below.
Sample D5092 (Figure 2a) is flesh pink, with a massive structure and a porphyritic texture (Figure 2e); the phenocrysts are mainly composed of plagioclase (35%~45%), K-feldspar (20%–25%), quartz (20%–25%), and minor biotite (<5%). The porphyroclasts are 2.5–7.5mm in size. The matrix with grain size varies from 0.2 to 0.9 mm of plagioclase (20%–25%), K-feldspar (30%–40%), quartz (20%–30%), biotite (5%–10%), and minor accessory minerals (including zircon and apatite).
Sample PM103 (Figure 2b,f) is gray and consists of K-feldspar (20%–25%), plagioclase (15%–20%), quartz (5%–10%), and biotite(5%±) porphyroclasts ranging in size from 0.5 to 1.5 mm in size and a fine-grained matrix of K-feldspar (10%–15%), plagioclase (10%–15%), quartz (15%–20%), and biotite (<5%) with accessory minerals, including sphene, zircon, and apatite.
Sample PM104 is flesh red, with a massive structure (Figure 2c) and a porphyritic texture (Figure 2g); it contains porphyroclasts and fine-grained groundmass with graphic texture. The principal minerals include K-feldspar (25%–35%), plagioclase (30%–40%), quartz (25%–30%), biotite (<5%), and hornblende (<5%).
Sample PM105 is flesh pink, and its phenocrysts are mainly composed of K-feldspar (10%–15%), plagioclase (15%–20%), and biotite (5%–10%), and the matrix (60%–70%) is microcrystalline quartz, K-feldspar, and plagioclase partly replaced by kaolinization. There is graphic intergrowth of quartz and K-feldspar in the matrix. The accessory minerals are magnetite and zircons (Figure 2d,h).

3. Analytical Methods

3.1. Zircon U-Pb Dating and the Hf Isotope

Four samples of zircon were selected from rock samples using standard gravimetric and magnetic separation techniques at the Langfang Geological Service Limited Corporation, Langfang (Hebei, China). Separated grains were mounted in epoxy resin disks and polished until they were approximately sectioned in half. The microstructures of the zircon grains were examined using cathodoluminescence (CL) and back-scattered electron (BSE) imaging prior to analysis. The testing was conducted at the LA-ICP-MS facility at the Isotopic Laboratory, Tianjin Institute of Geology and Mineral Resources of China Geological Survey. Laser sampling was performed using a Neptune multiple-collector inductively coupled plasma mass spectrometer (Thermo Fisher Ltd., Waltham, MA, USA) with a NEW WAVE 193 nm-FX ArF Excimer laser-ablation system (ESI Ltd., High Wycombe, UK). Data analysis was conducted with a beam diameter of 30 μm, an 8-Hz repetition rate, and energy density of 11 J/cm2. GJ-1 was used as an external standard for U-Pb dating analyses (published TIMS ages of 206Pb/238U = 600.7 ± 1.1 Ma, 207Pb/235U = 602.0 ± 1.0 Ma, and 207Pb/206Pb = 607.7 ± 4.3 Ma; Jackson et al. [48]). Every eight analyses were followed by two analyses of the standard zircon GJ-1, and common Pb was corrected as described by Andersen [49]. NIST SRM 610 glass was used as an external standard to calculate the U, Th, and Pb concentrations of zircons. 207Pb/206Pb, 206Pb/238U, 207Pb/235U, and 208Pb/232Th ratios were calculated using ICP-MS Data Cal 8.4 [50], Weighted mean 206Pb/238U ages and concordia plots were calculated using Isoplot v. 3.0 [51]. Age data and concordia plots were reported at 1 error, whereas the uncertainties for weighted mean ages are given at a 95% confidence level.
In situ zircon Hf isotopic analyses were undertaken with a beam diameter of 50 μm and a repetition rate of 11 Hz on the same zircon zones or on the same spots where U–Pb age analyses were conducted using the same equipment as was used for Zircon U-Pb. The GJ-1 and 91500 zircon standards yielded176Hf/177Hf ratios of 0.282008 ± 24 (2σ, n = 17) and 0.282297 ± 18 (2σ, n = 16), respectively [52]. Geng et al. [52] described the details of the instrumental conditions and analytical procedures for Lu–Hf isotope analyses. The εHf(t) were calculated based on the decay constant for 176Lu of 1.865 × 10−11year−1 [53] and present day chondritic ratios of 176Hf/177Hf = 0.282785 and 176Lu/177Hf = 0.0336 [54]. The TDM and T2DM were calculated for each sample as described by references [55] and [56].

3.2. Major and Trace Element Analyses

Whole-rock major and trace elements of granitoid samples were analyzed at the Laboratory of Tianjin Geological Mineral Testing Center, Tianjin, China. All samples (a total of 4, 3, 3, and 3 major and trace element composition analyses were conducted from samples D5092, PM103, PM104, and PM105, respectively) were chosen with relatively homogeneous and weak alterations, and then crushed to pass through a 200 mesh. Major and trace element contents were determined using X-ray fluorescence spectroscopy (XRF) and inductively coupled plasma–mass spectrometry (ICP–MS), and the presence of FeO in major was determined using the potassium chromate volumetric analysis method. The precision and accuracy for major element analyses were >5%, and for trace elements, both precision and accuracy were greater than 10% [57].

4. Results

4.1. Major and Trace Elements Composition

The major and trace element compositions of 13 granitoid samples are shown in Table 1.
The samples (D5092, PM103, PM104, and PM105) are characterized by high SiO2 (69.54 wt.%~75.60 wt.%, mean = 73.68 wt.%), relatively rich in K2O (4.10 wt.%~5.04 wt.%, mean = 4.56 wt.%, Na2O = 4.00 wt.%~4.36 wt.%, mean = 4.16 wt.%). Samples lie in the subalkaline granite field in the (K2O + Na2O) vs. SiO2 discrimination diagram (Figure 3a). Poor in CaO (0.16 wt.%~0.61 wt.%, mean = 0.42 wt.%), rich in Al2O3 (Al2O3 = 12.75 wt.%~14.39 wt.%, mean = 13.33 wt.%), FeOT content (1.55 wt.%~2.78 wt.%), and poor in MgO (MgO = 0.09 wt.%~1.05 wt.%, mean = 0.28 wt.%), FeOT/MgO ratios are within the range of 1.77~24.24, and with A/CNK values of 0.98~1.19 and A/NK values of 1.07~1.28, belong to metaluminous/peraluminous and high-K calc-alkaline series (Figure 3b,c). The LREEs are relatively enriched, while the HREEs are variably depleted (Figure 4a), with chondrite-normalized (La/Yb)N values of 2.48 to 11.07, and significantly developed negative Eu anomalies (δEu = 0.06–0.46). In addition, when normalized to the primitive mantle, they are relatively enriched in Rb, Th, U, and K, and significantly depleted in Ba, Nb, Ta, Sr, P, and Ti (Figure 4b).

4.2. Zircon U-Pb Dating

The zircon grains collected from the study samples have clear oscillatory zoning in CL images (Figure 5), and their Th/U ratios range from 0.10 to 5.19 (most ratios > 0.4) (Table 2), demonstrating their magmatic origin [56,63]. The analytical results are listed in Table 2. Additionally, 23 spot analyses of zircons from the porphyritic monzogranite sample (D5092) yielded a weighted mean 206Pb/238U age of 135.0 ± 0.6 Ma (N = 23, MSWD = 0.59; Figure 5a). For the granite porphyry sample (PM103), 15 points (except for one discordance age) form a coherent cluster with a weighted mean 206Pb/238U age of 130.7 ± 1.4 Ma (N = 15, MSWD = 3.5;Figure 5b). For the granite porphyry sample PM104, one zircon analysis was excluded from the age calculation due to discordance (280 ± 3 Ma). The remaining 14 spots form a coherent cluster and give a mean 206Pb/238U age of 130.4 ± 1.0 Ma (MSWD = 1.3) (Figure 5c). For the sample PM105 of granite porphyry, all 19 spot analyses resulted in 206Pb/238U ages ranging from 124 ± 1 to 130 ± 2 Ma, with a weighted mean 206Pb/238U age of 127.6 ± 0.8 Ma (MSWD = 1.4) (Figure 5d).

4.3. Zircon Hf Isotopes

Four samples were selected for zircon Hf isotope analysis on the same domains that were subjected to zircon U-Pb dating, and the results are listed in Table 3 and shown in Figure 6.
The zircon samples from D5092 showed zircon εHf(t) values from +4.7 to +11.5 and TDM2 ages from 583 to 1207 Ma. Sample PM103 shows relatively homogeneous Hf isotopic compositions, with initial 176Hf/177Hf ratios of 0.282817–0.282976 and εHf(t) values between + 4.5 and +10.1, with an average value of + 6.5 and two-stage model ages (TDM2) of 713–1218 Ma. Sample PM104 provided εHf(t) values ranging from +3.9 to +8.3 and TDM2 ages from 896 to 1276 Ma. Sample PM105 had εHf(t) values ranging from +2.0 to +9.5 and TDM2 ages from 761 to 1442 Ma.
In the diagram of εHf (t) vs. age, all εHf (t) values of the zircons plotted between the Chondrite Uniform Reservoir (CHUR) evolutionary line and the depleted mantle field were located in the field of the Phanerozoic igneous rocks in Eastern CAOB (Figure 6a) and consisted of the Early Cretaceous magmatic rocks in the southern GXR (Figure 6b) [18,19,65,66,67,68].

5. Discussion

5.1. Emplacement Ages of Granitoids

The zircon grains are euhedral–subhedral and display striped absorption and fine-scale oscillatory growth zoning. The representative zircon grains are shown in the CL images (Figure 5). We believe these zircons are of igneous origin [69,70] with relatively high Th/U ratios, which is consistent with magmatic origin. Therefore, the zircon U-Pb age represents the emplacement age of rocks. In the sample PM104, one of the zircon U-Pb ages is 280 ± 3 Ma, considering the late Permian tectono-magmatic event in the adjacent area, such as the Zhalantun area [71], the Nenjiang area [72], and the Heihe area [72,73]. Therefore, the 280 ± 3 Ma zircon should be the captured zircon; we deleted the data for this point accordingly. The weighted averages of the four samples of granitoids (D5092, PM103, PM104, and PM105) are 135.0 ± 0.6 Ma, 130.7 ± 1.4 Ma, 130.4 ± 1.0 Ma, and 127.6 ± 0.8 Ma, respectively (Figure 5). In summation, the emplacement age of the research rocks occurred in the Early Cretaceous period.

5.2. Petrogenesis of the Granitoids

In recent years, the genetic classification scheme of MISA (M, I, S, and A types) granite based on the nature of the magma source region has been widely accepted [74,75]. The mineral assemblage of the granitoids is mainly K-feldspar, plagioclase, quartz, and biotite, with a lesser amount of accessory mineral such as titanite, zircon, apatite magnetite, and zircons. A-type granite substantiates previously recognized geochemical features with high SiO2, Na2O + K2O, Fe/Mg, Ga/A1, Zr, Nb, Ga, Y, and Ce, and low CaO and Sr. This research focuses on rocks consistent with A-type granite with geochemical features (Table 1 and Figure 4). The major elements of these rocks are high SiO2, high (Na2O + K2O), high FeOT, and low MgO and CaO (Table 1). The trace elements of these rocks display consistent trace elements of primitive mantle-normalized patterns with positive Nb, Ga, Y, and Ce and negative anomalies of Ba, Nb, Ta, Sr, P, and Ti (Figure 4b). The ΣREEs contents of the rocks vary from 59.41 ppm to 344.05 ppm and are characterized by significant fractionation between LREE and HREE, with LREE/HREE values of 3.50–10.22 and (LaN/YbN) ratios of 2.48-11.07, and they have remarkable negative Eu anomalies with δEu = 0.06–0.46 and exhibit right-inclined “V”-shaped patterns with LREE enrichment (Figure 4a). In addition, in the diagrams of the 10,000 Ga/Al-(Na2O + K2O), 10,000 Ga/Al-FeOT/MgO, 10,000 Ga/Al-Nb, and 10,000 Ga/Al-Zr, all samples are plotted in the A-type field (Figure 7). Furthermore, A-type granite is generally considered to originate from relatively high-temperature magma [1,76], while I-type and S-type granite are derived from low-temperature magma [77]. The zircon saturation temperatures of granitoids in the study area are 799~868 °C (mean = 825 °C), 784~892 °C (mean = 845 °C), 809~831 °C (mean = 820 °C), and 812~891 °C (mean = 844 °C), respectively (Table 1), which are, obviously, higher than the crystallization temperatures of I-type granite (764 °C) [5]. A high differentiation index (DI) (most of them are greater than 93, except for samples PM103-1 and PM103-3) (Table 1) also reflects the characteristics of A-type granite.

5.3. Magma Source of the Granitoids

There are four possible interpretations for the source of A-type granites: (1) differentiation or partial melting of mantle-derived mafic magma [78,79,80,81,82]; (2) mixing melting of crust–mantle material [83]; (3) partial melting of the felsic rocks in the upper crust [84,85,86]; and (4) magmatic mixing of the mantle-derived basic magmas and crust-derived acidic magmas [64,87].
The major elements of the 13 granitoid samples contain high SiO2 (mean = 73.68 wt.%), which is much higher than the SiO2 (45.40 wt.%) content of the primitive mantle [88], and low MgO (mean = 0.28 wt.%), which is much lower than the MgO (36.77 wt.%) content of the primitive mantle [88]. These results indicate that these rocks are unreasonable if they originate from differentiation or partial melting of the primitive mantle. When normalized to the primitive mantle, these rocks are rich in trace elements of Th, U, and Rb, and negative in Nb, Ta, Ti, Sr, and P, implying that the composition is formed from the partial melting of the crust material [89].
The Nb/Ta ratios for these granitoids vary between 7.17 and 14.83 (mean = 10.87), which is significantly lower than the mantle values (17.5 ± 2) and is close to the crust values (~11) [82,83]. Figure 3b,c showed that the granitoids belong to the high-K calc-alkaline series and metaluminous/peraluminous series. The Zr /Hf values range from 23.83 to 33.78 (mean = 28.57), which is much lower than the mantle-derived magmas (36.27 ± 2.0) [90,91]; these results excluded the involvement of mantle-derived materials [92].
The initial 176Hf/177Hf ratios for four granitoid samples varied from 0.282751 to 0.283015 and the calculated εHf (t) for the corresponding zircon U-Pb age showed positive values ranging between 2.0 and 11.5 (Table 3), implying that the magma originated from the depleted mantle or was derived from newly underplated lower crusts [93,94]. Furthermore, the Hf two-stage ages (T2DM) of zircon can more accurately reflect the time of crust–mantle differentiation, and the T2DM ages of these rocks ranged from 583 Ma to 1442 Ma, suggesting that the magmas were generated by partial melting of the juvenile crust accreted during the Mesoproterozoic–Neoproterozoic period.

5.4. Tectonic Setting

The Mongol-Okhotsk Ocean and Paleo-Pacific Ocean tectonic regimes developed coevally during the Middle–Late Jurassic in the GXR, NE China [95]. The westward subduction of the Paleo-Pacific plate led to changes in the tectonic regimes from the compressional setting to an extensional setting during the Late Jurassic to Early Cretaceous period [43,96]. And widespread development of Early Cretaceous magmatism in NE China, including the GXR, eastern Jilin–Heilongjiang province, and Songliao Basin, is mainly related to the subduction of the Paleo-Pacific Plate [17,97]. The zircon U-Pb age of four samples in the study area ranges from 127.6 Ma to 135.0 Ma (Early Cretaceous), suggesting that these rocks may be the product of the subduction of the Paleo-Pacific Plate. The Ta+Yb-Rb diagram (Figure 8a) and Y-Nb diagram (Figure 8b) show that all samples were plotted at the joint of volcanic arc granite (VAG), within-plate granite (WPG), and syn-collision granite (Syn-COLG), implying that these are indicators of post-collision extensional settings [98,99]. In the R1-10,000 Ga/Al diagram, all samples were plotted in PA-type granite [100] (Figure 9a) and in the classification diagram of A1-type and A2-type granite. The granite samples fell in the A2-type granite zone [4] (Figure 9b), indicating that these granitoids occurred in an extensional tectonic setting. This conclusion is supported by the determination of synchronous I-type granite [101,102], A-type granite [72], metamorphic core complexes [103], and the formation of sedimentary basins [104] in the study area or an adjacent area. Hence, the study area was in an extensional setting during the Late Cretaceous period.
Many scholars have reported that the emplacement of massive Early Cretaceous A- type granite in NE China is associated with the Paleo-Pacific plate subduction instead of the post-Mongol-Okhotsk Ocean tectonic regime [15,29,105,106,107]. Furthermore, Early Cretaceous granite in the GXR is distributed in the NNE and NE directions, which is consistent with the subduction zone of the Paleo-Pacific plate but differs from the suture zone of the Mongol-Okhotsk Ocean [41,42,43,44]. Considering the exposure of calc-alkaline rock assemblages in the Early Cretaceous period in NE China [15] and the alkaline components of the volcanic rocks have increased polarity from the continental margin (east) to the continental (west) [20], we suggest that the studied A-type granitoids were formed in a back-arc extensional setting related to the slab rollback during the subduction of the Paleo-Pacific plate. The rollback of the Paleo-Pacific plate led to the asthenosphere mantle upwelling and the development of back-arc extension. The upwelling of the asthenosphere weakened the continental lithosphere of NE China, resulting in a widespread back-arc extension setting [108], and formed the low-pressure, high-temperature A-type granitoids. In summary, the study area was determined to be an extensional setting during the Early Cretaceous period, which is associated with the slab roll-back during the subduction of the Paleo-Pacific plate.

6. Conclusions

The whole-rock major and trace element compositions of the granitoids from the east slope of the Southern Great Xing’an Range indicate that these rocks are A-type granite. The emplacement age of these A-type granite rocks was identified as having occurred in the Early Cretaceous period (127.6 Ma–135.0 Ma). The Hf isotopes implied that the magma sources of granitoids caused the possible partial melting of the Mesoproterozoic–Neoproterozoic accreted lower crust. The study area was in an extensional back-arc setting during the Early Cretaceous period, which is associated with the slab roll-back of the Paleo-Pacific plate subduction.

Author Contributions

Conceptualization, X.R. and X.W.; Data curation, Z.S.; Funding acquisition, X.R. and X.W.; Investigation, X.R. and X.W.; Methodology, X.W.; Resources, Z.S.; Software, X.R.; Validation, X.W.; Visualization, X.R.; Writing—original draft, X.R.; Writing—review and editing, X.W. All authors have read and agreed to the published version of the manuscript.

Funding

This work was financially supported by the Jilin Province Science and Technology Department Program (No. 20220203197SF) and the China Geological Survey Program (No. 12120115031701).

Data Availability Statement

The data is available within the article.

Acknowledgments

We sincerely thank two anonymous reviewers for their constructive suggestions that helped us to improve the manuscript. We also thank the staff of the Langfang Geological Service Limited Corporation, Langfang, Hebei, China and the Tianjin Geological Mineral Testing Center, Tianjin, China, for their advice and assistance during the zircon selection and target making, and the in situ zircon U-Pb dating and zircon Hf isotopic analysis. We also appreciate the geologists from the Inner Mongolia Chifeng Geology and Mineral Resources Exploration Development Institute for their support of our fieldwork.

Conflicts of Interest

The authors declare no conflict of interest.

References

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Minerals 13 01523 g001
Figure 1. (a) Schematic map of the Central Asian Orogenic Belt, showing the major tectonic entities and the location of Figure 1b; (b) geotectonic division map of NE China (modified after [15]); (c) geological map showing distribution of magmatic rocks [36]; (d) geological map and sample locations of the study area in the southern GXR.
Figure 1. (a) Schematic map of the Central Asian Orogenic Belt, showing the major tectonic entities and the location of Figure 1b; (b) geotectonic division map of NE China (modified after [15]); (c) geological map showing distribution of magmatic rocks [36]; (d) geological map and sample locations of the study area in the southern GXR.
Minerals 13 01523 g001
Minerals 13 01523 g002
Figure 2. Representative field photographs showing the massive structure (a–d) and micrographic porphyritic textures (e–h) of granitoids from the study area.
Figure 2. Representative field photographs showing the massive structure (a–d) and micrographic porphyritic textures (e–h) of granitoids from the study area.
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Minerals 13 01523 g003
Figure 3. (a) Na2O + K2O vs. SiO2 (after [58]), (b) SiO2 vs. K2O (after [59]), and (c) A/NK versus A/CNK diagrams (after [60]) diagrams of granitoids from the southern GXR.
Figure 3. (a) Na2O + K2O vs. SiO2 (after [58]), (b) SiO2 vs. K2O (after [59]), and (c) A/NK versus A/CNK diagrams (after [60]) diagrams of granitoids from the southern GXR.
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Minerals 13 01523 g004
Figure 4. Chondrite-normalized REE (a) and primitive-mantle-normalized multi-element (b) diagrams for samples of the granitoids in study area (normalizing values are from ([61]); blue lines represent the study samples, and shaded fields represent A-type granite (data from Zhang et al. [62]).
Figure 4. Chondrite-normalized REE (a) and primitive-mantle-normalized multi-element (b) diagrams for samples of the granitoids in study area (normalizing values are from ([61]); blue lines represent the study samples, and shaded fields represent A-type granite (data from Zhang et al. [62]).
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Minerals 13 01523 g005
Figure 5. Representative cathodoluminescence (CL) images of zircons from the granitoid rocks and Zircon U-Pb Concordia diagrams of the granitoid samples. (a) D5092; (b) PM103; (c) PM104; (d) PM105.
Figure 5. Representative cathodoluminescence (CL) images of zircons from the granitoid rocks and Zircon U-Pb Concordia diagrams of the granitoid samples. (a) D5092; (b) PM103; (c) PM104; (d) PM105.
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Minerals 13 01523 g006
Figure 6. Correlations between εHf(t) and ages of zircons from the intrusions. CAOB = Central Asian Orogenic Belt; YFTB = Yanshan Fold and Thrust Belt. (a) Modified after [19,64] and (b) modified after [18,65].
Figure 6. Correlations between εHf(t) and ages of zircons from the intrusions. CAOB = Central Asian Orogenic Belt; YFTB = Yanshan Fold and Thrust Belt. (a) Modified after [19,64] and (b) modified after [18,65].
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Minerals 13 01523 g007
Figure 7. Discrimination diagrams of granite genetic type in the study area: (a) (K2O + Na2O) vs. 10,000 Ga/Al; (b) FeO/MgO vs. 10,000 Ga/Al; (c) Nb vs. 10,000 Ga/Al; and (d) Zr vs. 10,000 Ga/Al (after [2]).
Figure 7. Discrimination diagrams of granite genetic type in the study area: (a) (K2O + Na2O) vs. 10,000 Ga/Al; (b) FeO/MgO vs. 10,000 Ga/Al; (c) Nb vs. 10,000 Ga/Al; and (d) Zr vs. 10,000 Ga/Al (after [2]).
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Minerals 13 01523 g008
Figure 8. (a) Ta + Yb vs. Rb diagram; (b) Y vs. Nb diagram [71]. Abbreviations: VAG—volcanic arc granite; ORG—ocean ridge granite; WPG—within-plate granite; Syn-COLG—syn-collision granite.
Figure 8. (a) Ta + Yb vs. Rb diagram; (b) Y vs. Nb diagram [71]. Abbreviations: VAG—volcanic arc granite; ORG—ocean ridge granite; WPG—within-plate granite; Syn-COLG—syn-collision granite.
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Minerals 13 01523 g009
Figure 9. (a) R1-10,000 Ga/Al diagram (after [101]) and (b) Nb-Y-Ce diagram (after [4]) of the granitoids from study area.
Figure 9. (a) R1-10,000 Ga/Al diagram (after [101]) and (b) Nb-Y-Ce diagram (after [4]) of the granitoids from study area.
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Table 1. Whole-rock geochemical data of granitoids in southern Great Xing’an Range (Major elements: wt. %; Trace elements: ppm).
Table 1. Whole-rock geochemical data of granitoids in southern Great Xing’an Range (Major elements: wt. %; Trace elements: ppm).
Sample No.D5092-1D5092-2D5092-3D5092-4PM103-1PM103-2PM103-3PM104-1PM104-2PM104-4PM105-2PM105-3PM105-4
Major element (wt.%)
SiO274.4374.3074.1374.4972.5773.5069.5474.6874.3775.6075.0874.4970.63
Al2O312.9212.8712.8813.1213.9013.7314.2013.2013.2013.1212.7512.9514.39
CaO0.560.610.590.490.550.440.490.260.340.160.310.490.16
K2O4.494.504.544.614.224.104.145.035.004.214.804.575.04
Na2O4.114.194.354.134.024.334.004.054.204.104.054.144.36
Fe2O31.461.181.311.351.880.931.641.271.421.442.111.291.11
FeO0.980.780.950.771.090.720.390.410.640.640.570.981.18
MgO0.170.190.190.190.450.571.050.090.100.180.100.190.19
MnO0.080.060.070.080.210.030.030.060.070.040.060.080.07
P2O50.050.040.040.050.110.140.050.010.030.020.020.040.03
TiO20.230.200.200.210.710.330.730.160.150.110.110.210.23
LOI0.260.650.530.540.670.760.360.390.511.020.500.451.40
Total100.12100.21100.0599.90100.6499.6799.7799.69100.08101.39100.75100.0999.85
FeOT2.291.842.131.982.781.551.871.551.911.932.472.142.18
A/NK1.111.091.071.111.241.191.281.091.071.161.081.101.14
A/CNK1.021.000.981.041.141.111.191.051.021.131.031.021.11
K2O+Na2O8.608.698.898.748.248.428.149.099.208.318.858.719.41
Na2O/K2O0.920.930.960.900.951.060.970.800.840.980.850.910.86
Trace element (ppm)
Li4.4811.317.998.2156.3728.9226.259.6010.448.775.2710.1615.00
Be3.393.854.194.172.984.033.183.594.723.493.463.571.02
V7.005.624.904.03102.6224.8879.033.156.165.141.142.465.18
Cr21.3614.2210.8217.8166.8820.2654.5210.1519.0838.8027.7816.0435.40
Co0.890.870.810.8220.183.2312.300.360.990.720.971.100.74
Ni5.343.042.214.205.008.104.003.095.192.144.702.931.88
Ga18.2119.2418.0719.0625.6219.7830.4319.3118.3024.1020.8721.5020.30
Rb271.98253.39260.72273.29232.06120.83223.20227.73207.12128.00307.94308.89123.00
Sr31.5473.6461.0570.20165.6980.8082.0720.6014.8643.9036.2484.9122.50
Zr235.13207.61226.63253.28248.08143.17310.72253.43234.18180.90211.55212.61454.70
Nb9.0110.9211.3110.9716.489.5230.0616.1214.8011.5110.0011.8311.75
Ba188.93237.77175.97229.90805.42438.03448.0350.4472.68241.40223.13308.8185.50
La33.8539.6331.9038.5549.2025.3873.3233.2925.9617.4038.3150.968.80
Ce56.3174.5260.2063.53106.7955.61151.3858.8946.2334.7094.19113.0122.00
Pr9.049.968.729.9211.756.9617.127.836.755.5110.5513.092.67
Nd35.5339.0634.5538.8845.3925.8960.5529.6625.4121.9040.6750.299.98
Sm7.067.597.057.478.645.5010.585.534.924.828.249.382.41
Eu0.260.440.350.390.520.620.430.100.130.220.320.560.34
Gd5.636.345.976.327.094.459.124.554.163.826.977.592.20
Tb0.991.121.081.111.220.841.450.800.720.671.311.290.51
Dy5.896.496.596.666.705.038.024.474.093.978.167.223.87
Ho1.141.281.321.331.260.901.420.840.820.811.661.380.81
Er3.413.773.883.933.782.894.542.602.402.575.074.142.47
Tm0.530.600.620.620.600.460.710.430.410.410.800.670.39
Yb3.473.904.024.053.712.934.752.742.592.705.324.432.55
Lu0.520.600.620.620.560.400.670.410.390.420.800.680.41
Y29.9635.1137.9537.7738.1027.5141.2722.4121.1116.2847.7539.0319.74
Hf8.347.378.328.937.345.949.398.868.327.598.347.3813.50
Ta0.811.101.251.151.111.332.531.241.181.160.901.171.06
Th13.7416.6115.7916.0517.0417.7922.6313.1211.2515.7019.0219.3613.00
U2.062.922.762.898.504.295.704.192.027.013.402.993.16
DI95939595909390969595949494
TZr(°C)868799812821892784860831820809812812891
ΣREE163.62195.30166.88183.39247.20137.88344.05152.14124.9899.91222.38264.7159.41
LREE142.04171.21142.77158.74222.29119.96313.37135.31109.4084.55192.28237.2946.20
HREE21.5824.1024.1124.6524.9117.9130.6816.8415.5815.3730.1027.4213.20
LREE/HREE6.587.105.926.448.926.7010.228.047.025.506.398.663.50
LaN/YbN7.007.285.696.829.526.2111.078.727.194.635.178.252.48
δEu0.130.190.170.180.210.380.130.060.090.160.130.200.46
10,000 Ga/Al2.662.822.652.743.482.724.052.762.623.473.093.142.67
Table 2. LA-MC-ICP-MS zircon U-Pb data of granitoids in southern Great Xing’an Range.
Table 2. LA-MC-ICP-MS zircon U-Pb data of granitoids in southern Great Xing’an Range.
No.Pb
(ppm)		Th
(ppm)		U
(ppm)		Th/UIsotopic RatiosAges (Ma)
207Pb/206Pb207Pb/235U206Pb/238U207Pb/206Pb207Pb/235U206Pb/238U
Ratio1σRatio1σRatio1σAge1σAge1σAge1σ
Sample D5092
13811470.550.04910.00290.14260.00820.02110.000215413713581341
28463990.120.04820.00210.14000.00600.02110.000210710113361341
392814320.650.04870.00160.14050.00470.02090.00021357913341331
4101544530.340.04900.00180.14370.00530.02130.00021488613651361
5106644841.370.04850.00100.14260.00310.02130.00021245013531361
6136246071.030.04810.00090.14230.00280.02140.00021054513531372
78583700.160.04820.00130.14300.00390.02150.00021096313641371
881313820.340.04850.00120.14380.00380.02150.00021236013641371
92217982.210.04900.00470.14450.01380.02140.0003146224137131372
1012735220.140.04860.00130.14290.00400.02130.00021316413641361
1110704380.160.04890.00140.14170.00410.02100.00021426813541341
124691830.380.04880.00370.14230.01100.02110.0002139180135101351
1313715620.130.04890.00070.14250.00230.02110.00021453613521351
1461322540.520.04870.00220.14220.00650.02120.000213310713561351
15103964600.860.04950.00140.14290.00450.02090.00021726713641341
16111905090.370.04940.00160.14390.00480.02110.00021697613651351
17121164710.250.04980.00070.14340.00240.02090.00021863213621331
189434350.100.04920.00130.14280.00420.02100.00021596413641341
19227710.370.04870.00590.14290.01710.02130.0003132287136161362
2037591525.010.04860.00350.14190.01020.02120.0002131168135101351
212109881.230.04820.01060.14220.03090.02140.0003110517135291362
226661590.420.28600.00500.95100.01650.02410.0003339627679121542
2325591085.190.04890.00520.14160.01470.02100.0002143248135141342
Sample PM103
1226829670.710.05010.00110.14380.00340.02080.00021995313631331
22361711160.550.04910.00140.13470.00400.01990.00021516812841271
3174568350.550.04920.00210.13350.00590.01970.000215710012761261
4164077340.550.04870.00160.13910.00470.02070.00021327913241321
5143486340.550.04960.00150.14120.00450.02060.00021777313441321
6101544570.340.04990.00280.14130.00800.02050.000219013313481311
7173877990.480.04980.00130.14150.00370.02060.00021856113441321
8163637460.490.05020.00170.14200.00480.02050.00022027713551311
9112505010.500.04850.00190.14020.00560.02100.00021249313351341
102146610000.470.04990.00110.14100.00340.02050.00021905213431311
11102644590.570.04840.00200.13330.00560.02000.00021219812751271
12204919290.530.04970.00120.13890.00350.02030.00021805813231291
13184288180.520.04890.00130.13820.00380.02050.00021446213141311
14205138740.590.04900.00150.14030.00440.02080.00021467213341331
1571943300.590.04900.00270.14320.00810.02120.000215013013681351
Sample PM104
14781830.420.05010.00480.13930.01340.02020.0003200223132131292
2124265450.780.04930.00160.14020.00470.02060.00021647713341311
35962430.390.04980.00380.14110.01090.02050.0002186180134101312
4113314980.660.04910.00220.13740.00630.02030.000215410513161291
53641600.400.04880.00510.13790.01440.02050.0003137246131141312
64571730.330.05020.00670.14330.01920.02070.0003206308136181322
781474130.360.04900.00240.13720.00680.02030.000214811513161301
82361190.300.04930.00710.14020.02000.02060.0003161339133191322
9165377590.710.04920.00170.13480.00480.01990.00021587912851271
107841620.520.05190.00250.31820.01560.04440.0005283111281142803
1191744290.410.05040.00200.14320.00590.02060.00022149313661311
1271003240.310.05050.00460.14300.01320.02050.0002220210136131312
132592511390.810.04880.00100.13550.00310.02020.00021365012931291
1482573630.710.04860.00220.13970.00660.02080.000212910913361331
152391050.370.04830.00820.13910.02250.02090.0003114402132211332
Sample PM105
127103412700.810.04920.00090.13530.00270.02000.00021574412931271
2207399810.750.04860.00100.13290.00300.01980.00021305112731271
3113775300.710.05000.00150.13800.00440.02000.00021957113141281
42854214440.380.05010.00120.13780.00380.01990.00021995813141271
5101895270.360.04830.00260.13230.00720.01990.000211612512671271
679159838870.410.05100.00070.14270.00220.02030.00022393113521302
7195938980.660.05010.00130.13850.00360.02000.00022015913231281
8196119130.670.05020.00120.13930.00330.02010.00022035413231281
929124213450.920.04990.00090.13560.00250.01970.00021934112921261
1036147117230.850.05060.00110.13540.00310.01940.00022224912931241
11134026390.630.04880.00140.13380.00380.01990.00021376512741271
1230117213560.860.04980.00090.13920.00270.02030.00021864013231291
132377910990.710.05020.00110.13910.00310.02010.00022075113231281
142386110430.820.04870.00110.13460.00330.02010.00021325512831281
1530137613850.990.04970.00100.13470.00300.01970.00021804912831251
1641164718640.880.04900.00080.13440.00240.01990.00021493912821271
17182828970.310.04940.00120.13770.00330.02020.00021675513131291
1830118713100.910.04940.00090.13790.00250.02020.00021674113121291
192797912090.810.04920.00080.13840.00230.02040.00021573913221301
Table 3. Hf isotopic data of zircons extracted from granitoids in southern Great Xing’an Range.
Table 3. Hf isotopic data of zircons extracted from granitoids in southern Great Xing’an Range.
No.Age (Ma)176Yb/177Hf2s176Lu/177Hf2s176Hf/177Hf2s176Hf/177HfiεHf(0)εHf(t)TDM (Ma)T2DM (Ma)fLu/Hf
Sample D5092
D5092.11340.0553740.0003630.0012340.0000050.2828740.0000220.2828713.66.45401045−0.96
D5092.21340.0784900.0005290.0016690.0000220.2828510.0000230.2828472.85.65791121−0.95
D5092.31330.0629890.0008800.0017400.0000180.2828830.0000270.2828783.96.75351022−0.95
D5092.41360.0831080.0009570.0022780.0000180.2828950.0000300.2828904.47.1524983−0.93
D5092.51360.0602140.0003990.0012290.0000050.2828990.0000370.2828964.57.4504962−0.96
D5092.61370.1128870.0007400.0023340.0000070.2829870.0000490.2829817.610.4389687−0.93
D5092.71370.0847800.0006690.0018600.0000200.2828310.0000540.2828262.14.96111184−0.94
D5092.81370.0527820.0003160.0013120.0000070.2829040.0000210.28290157.6497944−0.96
D5092.91370.0851570.0004600.0019300.0000060.2828820.0000520.2828773.96.75391024−0.94
D5092.101360.1040960.0003840.0022620.0000090.2828970.0000290.2828924.47.2521976−0.93
D5092.111340.0897050.0003270.0019960.0000110.2828410.0000230.2828362.45.25991157−0.94
D5092.121350.1074640.0008690.0023750.0000540.2828900.0000390.2828844.26.95331002−0.93
D5092.131350.1179960.0010740.0025730.0000310.2830210.0000500.2830158.811.5342583−0.92
D5092.141350.0604710.0004610.0014160.0000090.2828230.0000460.2828201.84.76151207−0.96
Sample PM103
PM103.11330.0458290.0006920.0011540.0000180.2828200.0000430.2828171.74.56151218−0.97
PM103.21270.0519560.0001950.0013680.0000040.2828630.0000220.2828593.25.95581091−0.96
PM103.31260.0546150.0011680.0015970.0000540.2829080.0000280.2829044.87.4496949−0.95
PM103.41320.0547410.0006580.0013970.0000200.2828540.0000250.2828502.95.75711113−0.96
PM103.51320.0712120.0016580.0020610.0000480.2829310.0000300.2829265.68.3469873−0.94
PM103.61310.0434440.0002950.0015700.0000100.2828570.0000380.2828543.05.85681104−0.95
PM103.81320.0417690.0002720.0010500.0000050.2828500.0000200.2828482.85.65711122−0.97
PM103.91310.0520380.0002760.0012030.0000040.2828880.0000200.2828854.16.95191002−0.96
PM103.101340.0278960.0000720.0007010.0000040.2828210.0000160.2828201.74.66061210−0.98
PM103.111310.0441020.0020380.0010510.0000340.2829780.0000260.2829767.310.1389713−0.97
PM103.121270.0494080.0013270.0018330.0000280.2828880.0000600.2828844.16.85281012−0.94
PM103.131290.0412940.0001340.0010580.0000030.2828520.0000310.2828492.85.65691120−0.97
PM103.141310.0567720.0008260.0012910.0000110.2828920.0000220.2828894.37.0514991−0.96
Sample PM104
PM104.11290.0709420.0002640.0016070.0000040.2828700.0000320.2828663.46.15521069−0.95
PM104.21310.0690490.0008000.0015500.0000270.2828040.0000260.2828001.13.96461276−0.95
PM104.31310.0556110.0002490.0013340.0000020.2828370.0000230.2828342.35.15941169−0.96
PM104.41290.0911810.0010880.0021570.0000150.2828910.0000300.2828864.26.95281002−0.94
PM104.51310.1078870.0015900.0024440.0000450.2829330.0000350.2829275.78.3471870−0.93
PM104.61320.0406510.0004800.0009670.0000070.2828540.0000240.2828522.95.75641109−0.97
PM104.71300.0775450.0013010.0017500.0000200.2829020.0000270.2828984.67.3507965−0.95
PM104.81320.0476540.0000710.0011890.0000050.2828640.0000260.2828613.36.05531080−0.96
PM104.91270.0964820.0015870.0022620.0000260.2829260.0000280.2829205.48.0479896−0.93
PM104.111310.1202600.0025730.0028570.0001200.2829050.0000280.2828984.77.3518962−0.91
PM104.121310.0790620.0006730.0018020.0000370.2829050.0000300.2829004.77.4504955−0.95
PM104.131290.1564810.0023380.0034620.0000580.2828160.0000270.2828071.54.16621256−0.90
PM104.141330.1004190.0006720.0022120.0000070.2828890.0000250.2828844.16.95321005−0.93
Sample PM105
PM105.11270.1316150.0007070.0040850.0000160.2829720.0000560.2829627.19.5433761−0.88
PM105.21270.0504830.0008420.0018290.0000320.2828000.0000550.2827951.03.66561297−0.94
PM105.31280.0930220.0005810.0033880.0000090.2829470.0000480.2829396.28.7461834−0.90
PM105.41270.0519560.0001950.0013680.0000040.2828630.0000220.2828593.25.95581091−0.96
PM105.51270.0402280.0006320.0015500.0000190.2828140.0000340.2828111.54.16301248−0.95
PM105.61300.0814830.0029180.0025870.0000580.2829280.0000320.2829225.58.2479886−0.92
PM105.71280.0306550.0003300.0010050.0000080.2828220.0000310.2828191.84.56101218−0.97
PM105.81280.0850390.0004330.0026530.0000150.2827630.0000360.282757−0.32.37261418−0.92
PM105.91260.0852250.0002730.0030490.0000070.2828950.0000310.2828884.46.95351001−0.91
PM105.101240.0752580.0010600.0029130.0000360.2829330.0000770.2829265.78.2477882−0.91
PM105.111270.0778900.0003120.0025410.0000050.2829070.0000360.2829014.87.3511959−0.92
PM105.121290.1390070.0033500.0039770.0000670.2829210.0000420.2829115.37.8510921−0.88
PM105.131280.0557220.0004530.0019500.0000120.2828260.0000340.2828211.94.66201211−0.94
PM105.141280.1187110.0006270.0034870.0000170.2829070.0000510.2828994.87.3524964−0.89
PM105.151250.1097860.0012710.0036850.0000260.2827590.0000380.282751−0.52.07531442−0.89
PM105.161270.1182660.0023740.0035850.0000520.2828970.0000510.2828884.46.9541999−0.89
PM105.171290.0700230.0004750.0026690.0000130.2828880.0000300.2828814.16.75411018−0.92
PM105.181290.1247980.0010360.0041230.0000260.2828720.0000330.2828623.56.05881081−0.88
PM105.191300.0854530.0017980.0027770.0000490.2827870.0000400.2827800.53.16931341−0.92
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MDPI and ACS Style

Ran, X.; Wang, X.; Sun, Z. Petrogenesis and Tectonic Setting of Early Cretaceous A-Type Granite from the Southern Great Xing’an Range, Northeastern China: Geochronological, Geochemical, and Hf Isotopic Evidence. Minerals 2023, 13, 1523. https://0-doi-org.brum.beds.ac.uk/10.3390/min13121523

AMA Style

Ran X, Wang X, Sun Z. Petrogenesis and Tectonic Setting of Early Cretaceous A-Type Granite from the Southern Great Xing’an Range, Northeastern China: Geochronological, Geochemical, and Hf Isotopic Evidence. Minerals. 2023; 13(12):1523. https://0-doi-org.brum.beds.ac.uk/10.3390/min13121523

Chicago/Turabian Style

Ran, Xiangjin, Xi Wang, and Zhenming Sun. 2023. "Petrogenesis and Tectonic Setting of Early Cretaceous A-Type Granite from the Southern Great Xing’an Range, Northeastern China: Geochronological, Geochemical, and Hf Isotopic Evidence" Minerals 13, no. 12: 1523. https://0-doi-org.brum.beds.ac.uk/10.3390/min13121523

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