Petrogenesis of Late Jurassic–Early Cretaceous Granitoids in the Central Great Xing’ an Range, NE China

Qian, Cheng; Lu, Lu; Wang, Yan; Fu, Junyu; Yang, Xiaoping; Zhang, Yujin; Ni, Sizhe

doi:10.3390/min15070693

Open AccessArticle

Petrogenesis of Late Jurassic–Early Cretaceous Granitoids in the Central Great Xing’ an Range, NE China

by

Cheng Qian

^1,2

,

Lu Lu

^3,*,

Yan Wang

¹,

Junyu Fu

¹,

Xiaoping Yang

¹,

Yujin Zhang

¹ and

Sizhe Ni

⁴

¹

Shenyang Center of China Geological Survey, Shenyang 110034, China

²

Key Laboratory of Black Soil Evolution and Ecological Effect, Ministry of Natural Resources/Liaoning Province, Shenyang 110034, China

³

Paleontological College, Shenyang Normal University, Shenyang 110034, China

⁴

Shenyang Geotechnical Investigation & Surveying Research Institute Co., Ltd., Shenyang 110034, China

^*

Author to whom correspondence should be addressed.

Minerals 2025, 15(7), 693; https://doi.org/10.3390/min15070693

Submission received: 30 May 2025 / Revised: 26 June 2025 / Accepted: 26 June 2025 / Published: 28 June 2025

(This article belongs to the Special Issue Selected Papers from the 7th National Youth Geological Congress)

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Abstract

The Great Xing’ an Range is located in the eastern part of the Xing’ an-Mongolian Orogenic Belt, which is an important component of the Central Asian Orogenic Belt. To determine the emplacement age and petrogenesis of the granitoids in the Gegenmiao and Taonan areas of the central Great Xing’an Range, and to investigate its tectonic setting, petrographic studies, zircon U-Pb geochronology, whole-rock Sr-Nd isotopic analysis, zircon Hf isotopic analysis, and detailed geochemical investigations of this intrusion were carried out. The results indicate the following, in relation to the granitoids in the study areas: (1) The zircon U-Pb dating of the granitic rocks in the study areas yields ages ranging from 141.4 ± 2.0 Ma to 158.7 ± 1.9 Ma, indicating their formation during the Late Jurassic to Early Cretaceous; (2) the geochemical characteristics indicate that these rocks belong to the calc-alkaline series and peraluminous, classified as highly fractionated I-type granites with adakite features; (3) the Sr-Nd isotopic data show that the εNd(t) values of Gegenmiao granitic rocks are 2.8 and 2.1, while those of Taonan granitic rocks range from −1.5 to 0.7; (4) the Zircon εHf(t) values of the granitic rocks from Gegenmiao and Taonan vary from 2.11 to 6.48 and 0.90 to 8.25, respectively. They are interpreted to have formed through partial melting of thickened lower crustal material during the Meso-Neoproterozoic. The Gegenmiao and Taonan granitic rocks were formed in a transitional environment from post-orogenic compression to extension, which is closely associated with the Mongolia–Okhotsk tectonic system.

Keywords:

granitic rocks; Late Jurassic–Early Cretaceous; Central Great Xing’ an Range; Mongol–Okhotsk Ocean

1. Introduction

The Central Asian Orogenic Belt (CAOB) is the largest and most complex accretionary orogenic belt in the world [1,2,3]. The east of the CAOB, known as the Xing’ an-Mongolian Orogenic Belt (XMOB), serves as a classic region for the superposition and evolution of multiple tectonic systems. This region underwent the evolution of the Paleo-Asian tectonic system in the Paleozoic, characterized by collision–accretion of multiple microblocks and the closure of the Paleo-Asian Ocean [4,5,6]. In the Mesozoic, the region was jointly influenced by the Circum-Pacific and Mongolia–Okhotsk tectonic systems, giving rise to extensive magmatic rocks. Although previous studies on these magmatic rocks have made significant progress, the relationship between them and the two tectonic systems remains highly controversial [7,8].

The Great Xing’ an Range is located in the eastern part of XMOB, which is characterized by the widespread occurrence of Late Mesozoic granites and volcanic rocks. These Mesozoic magmatic rocks record important information about the Mesozoic two tectonic system process of XMOB. Previous studies have made significant advances in the petrology, chronology, and geochemistry of the Late Mesozoic igneous rocks in the Northern Great Xing’ an Range. However, the genesis of these rocks remains a subject of ongoing debate. Currently, there are three different opinions on the petrogenesis of these Mesozoic igneous rocks: (1) their formation is linked to the Mongolia–Okhotsk tectonic system [9,10,11]; (2) they are associated with the Paleo-Pacific tectonic system [7,12]; and (3) they are a result of the combined influence of the Mongolia–Okhotsk tectonic system and the Paleo-Pacific tectonic system [7,8]. Consequently, the genetic study of Mesozoic magmatic rocks from the Central Great Xing’ an Range is crucial for resolving the Mesozoic two tectonic system process of XMOB.

This paper presents a detailed study of the Late Jurassic–Early Cretaceous granitic rocks from the Gegenmiao and Taonan areas in the Middle of Central Great Xing’an Range. To analyze the granitic rocks of the study area and their magma source characteristics, this study systematically analyzed petrography, zircon U-Pb geochronology, geochemistry, and zircon Hf isotopes.

2. Geological Background

Northeastern (NE) China is tectonically located in the eastern segment of CAOB (Figure 1a), and is composed of several micro-continental massifs, including, from northwest to southeast, the Erguna Block, Xing’ an Block, Songnen Block, Jiamusi Block and Khanka Block (Figure 1b). The Great Xing’an Range is located in CAOB (Figure 1a). The Xing’ an block is located between the Erguna Block and Songnen Block, separated by the Tayuan-Xiguitu and Hegenshan–Hehei faults, respectively [12]. It comprises the Great Xing’ an Range and Halar Basin, and is characterized by extensive Mesozoic granitoids and volcanic rocks, as well as Paleozoic strata primarily consisting of Early Paleozoic limestone and Late Paleozoic clastic sediments [13]. The Songnen Block primarily includes the Songliao Basin and the Lesser Xing’an-Zhangguangcai area [14]. Its Precambrian basement is composed of the Dongfengshan Formation in amphibolite facies, as well as Neoarchean to Early Paleoproterozoic granitic gneisses and plagioclase amphibolite [15,16]. Early Paleozoic strata are exposed in this region, predominantly consisting of clastic sedimentary rocks from a shallow marine continental margin environment. Influenced by the closure of the Paleo-Asian Ocean, continental margin arc magmatic activity developed along the southern and western margins of the block during the late Paleozoic. Additionally, a Meso-Cenozoic volcanic basin was superimposed, accompanied by significant Late Triassic to Early Cretaceous granitic magmatic activity [17].

The Gegemiao and Taonan areas are located in the central part of the Great Xing’an Range, to the west of the fault zone along the western margin of the Songliao Basin. The exposed strata in the study area are primarily Late Paleozoic and Jurassic–Cretaceous volcanic rocks, including, from bottom to top, the Wanbao, Manketouebo, Manitu, Baiyingaolao, Longjiang, Guanghua, and Ganhe formations (Figure 2). Additionally, Late Jurassic to Early Cretaceous granitoids are also present in the region.

3. Petrological Analysis of Samples and Analytical Methods

3.1. Petrology

The studied samples were collected from the Gegenmiao and Taonan areas in the central Great Xing’ an Range. The locations of the sample points are shown in Figure 2 and Table 1.

The Gegenmiao pluton is primarily composed of tonalites (samples D16017 and D16018) and monzogranite (samples D16022 and D16023). The tonalites have a gray-white, medium-fine granitic texture with a massive structure, and are mainly composed of plagioclase (~75%), quartz (~20%), and biotite (~5%) (Figure 3a,b). The surfaces of the monzogranite are gray-white (Figure 3c). This rock also exhibits a medium-fine granitic texture and a massive structure. The monzogranite contains ~35% K-feldspar, ~30% quartz, ~30% plagioclase, and ~5% biotite (Figure 3d).

The Taonan pluton is primarily composed of granodiorite (samples D17020, D17028 and D17033), tonalites (sample D17029), and monzogranite (sample D17030). The light red or grayish-white granodiorite has a massive structure and medium-to fine grained texture (Figure 3e). It consists of plagioclase (45%~59%), quartz (25%~30%), K-feldspar (10%~20%), and biotite (5%–10%) (Figure 3f). The grayish-white, medium-fine-grained tonalite generally contains plagioclase (~62%), quartz (~25%), biotite (~10%), and K-feldspar (~3%) (Figure 3g,h). The monzogranite is massive, medium-to-fine-grained, and grayish-white in color (Figure 3i), composed mainly of plagioclase (~40%), K-feldspar (~30%), quartz (~22%), and biotite (~8%) (Figure 3j).

3.2. Major and Trace Element Determinations

After petrographic analysis, fresh samples were selected, crushed, and powdered in an agate mill to ~200 mesh used for major and trace-element analyses. Whole-rock geochemical analyses were conducted at the Northeast China Supervision and Inspection Center of Mineral Resources, Ministry of Land and Resources, Shenyang, China. Major element compositions were determined by X-ray fluorescence spectrometry (XRF), with analytical uncertainties range less than 2%. Trace element compositions were determined by inductively coupled plasma mass spectrometer (ICP-MS, Thermo X Series II), yielding an analytical precision of <5% for element compositions > 10 ppm, <8% for element compositions < 10 ppm, and ~10% for transition metals.

3.3. Zircon U-Pb Dating

Zircons for U-Pb dating were extracted and selected by Yuheng Ore-rock Technical Service co. LTD in Langfang, Hebei province. The selected zircons were mounted onto an epoxy resin disc together with standard zircons, and then ground down and polished to expose their interior structure. Cathodoluminescence (CL) images were taken and applied to check the internal structures of each grain. Then potential target domains avoiding internal cracks and inclusions were selected for subsequent LA-ICP-MS U-Pb dating, which was conducted at the Deep Earth Dynamics Key Lab of Ministry of Natural Resources, Institute of Geology, Chinese Academy of Geological Sciences. Detailed procedures and methods have been described by Hou et al. [18], and isotopic ratios and elemental concentrations were calculated using the ICPMS Data Cal software package (GLITTER 4.4) [19].

3.4. Whole-Rock Sr-Nd Isotope Analyses

Sr-Nd isotopic compositions were determined by thermal ionization mass spectrometry (TIMS) on a Finnigan MAT-261 mass spectrometer at the Analytical Laboratory, Beijing Institute of Uranium Geology, China. The detailed isotopic measurement procedures are described by Wu [20]. Total procedural blanks were <300 pg for Sr and <100 pg for Nd, and the estimated analytical uncertainties of ¹⁴⁷Sm/¹⁴⁴Nd and ⁸⁷Rb/⁸⁶Sr ratios are <0.5%. ⁸⁷Sr/⁸⁶Sr were corrected for mass fractionation by normalization to86Sr/88Sr = 0.1194, and ¹⁴³Nd/¹⁴⁴Nd ratios were normalized to ¹⁴⁶Nd/¹⁴⁴Nd = 0.7219. During the period of data acquisition, the measured values for the NBS-987 Sr and LaJolla Nd standards were ⁸⁷Sr/⁸⁶Sr = 0.710224 ± 0.000008 (2σ) and ¹⁴³Nd/¹⁴⁴Nd = 0.511864 ± 0.00000 (2σ), respectively.

3.5. Zircon Hf Isotope Analyses

In-situ zircon Hf isotopic analyses were conducted on a Neptune multi-collector ICP-MS (NuPlasma II MC-ICPMS) equipped with a GeoLasPro 193 nm laser ablation microprobe, at the Deep Earth Dynamics Key Lab of Ministry of Natural Resources, Institute of Geology, Chinese Academy of Geological Sciences. The instrumental conditions and data acquisition were comprehensively described by Hou [21], and the detailed analytical procedures were described by Wu [22]. Depending on the size of the ablated domains, a stationary spot was used with a beam diameter of 44 μm. During the analyses, zircon GJ1 was used as the reference standard, with a weighted mean ¹⁷⁶Hf/¹⁷⁷Hf ratio of 0.282007 ± 0.000007 (2σ, n = 36). Initial ¹⁷⁶Hf/¹⁷⁷Hf ratios were calculated with measured ¹⁷⁶Hf/¹⁷⁷Hf and ¹⁷⁶Lu/¹⁷⁷Hf ratios, taking the decay constant for 176Lu as 1.865 × 10⁻¹¹ year⁻¹ [23]. εHf(t) values were calculated adopting the present-day chondritic ¹⁷⁶Hf/¹⁷⁷Hf ratios of 0.282772 and ¹⁷⁶Lu/¹⁷⁷Hf ratios of 0.0332 [24]. Hf model ages (single-stage model ages) (TDM1) were calculated based on a depleted-mantle source with a present-day ¹⁷⁶Hf/¹⁷⁷Hf ratio of 0.28325, and “crust” Hf model ages (two-stage model ages) (TDM2) were calculated based on the assumption of a mean ¹⁷⁶Lu/¹⁷⁷Hf value of 0.015 for average continental crust [25].

4. Analytical Results

4.1. Major and Trace Elements

Five samples from the Gegenmiao area and nineteen samples from the Taonan area were selected for geochemical analysis. These include tonalites (B16017, B16018-1, B16018-2) and monzogranites (B16022, B16023) from the Gegenmiao area, and granodiorites (B17020-1, B17020-2, B17020-3, B17020-4, B17020-5, B17028-1, B17028-2, B17028-3, B17028-4, B17033-1, B17033-2, B17033-3, B17033-4, B17033-5), tonalites (D17029-1, D17029-2), and monzogranites (B17030-1, B17030-2, B17030-3) from the Taonan area (Figure 2). The analytical results and geochemical characteristics of the granitic rocks from the Gegenmiao and Taonan areas are presented in Table 2.

The results show that the granitic rocks from the Gegenmiao area have relatively high SiO₂ (65.81 wt.%~73.83 wt.%) and Al₂O₃ (13.65 wt.%~15.38 wt.%), and low MgO (0.31 wt.%~1.30 wt.%), CaO (0.71 wt.%~2.98 wt.%), P₂O₅ (0.08 wt.%~0.22 wt.%), FeO (0.72 wt.%~2.34 wt.%), and Fe₂O₃ (0.73 wt.%~1.83 wt.%) contents (Table 2). They exhibit high K₂O (1.13 wt.%~4.11 wt.%) and Na₂O (4.14 wt.%~5.56 wt.%) contents, with total alkali (Na₂O + K₂O) ranging from 6.85 wt.% to 8.36 wt.% (average = 7.42 wt.%). The Na₂O/K₂O ratios vary between 1.01 and 2.31 (average = 1.82), except for sample B16018-2 (Na₂O/K₂O = 4.92). The major elements of the granitic rocks from the Taonan area are characterized by high silicon (SiO₂ = 70.64 wt.%~77.95 wt.%), rich aluminum (Al₂O₃ = 13.01 wt.%~15.25 wt.%), and low magnesium (MgO = 0.02 wt.%~0.52 wt.%), iron (FeO = 0.29 wt.%~2.07 wt.%, Fe₂O₃ = 0.22 wt.%~1.05 wt.%), calcium (CaO = 0.18 wt.%~2.18 wt.%), and phosphorus (P₂O₅ = 0.36 wt.%~0.98 wt.%). These rocks are rich in potassium and sodium, with K₂O ranging from 0.24% to 3.33%, and Na₂O ranging from 4.60 wt.% to 7.19 wt.%. The total alkali contents (Na₂O + K₂O) range from 6.49 wt.% to 8.62 wt.% (average = 7.42 wt.%). The Na₂O/K₂O ratios range from 1.48 to 5.16 (average = 2.06), except for samples B17028-1 (Na₂O/K₂O = 25.78) and B17028-2 (Na₂O/K₂O = 11.39).

In the K₂O + Na₂O vs. SiO₂ diagram (Figure 4a), most of the samples fall within the granite field. In the K₂O vs. SiO₂ diagram (Figure 4b), most the samples lie within the field of the calc-alkaline series. The aluminum saturation index (A/CNK) of the samples from the Gegenmiao and Taonan areas ranges from 0.99 to 1.16 (average = 1.06) and 1.01 to 1.20 (average = 1.11), respectively. In the A/NK vs. A/CNK diagram (Figure 4c), all the samples plot within the field of metaluminous to strongly peraluminous.

The granitic rocks from the Gegenmiao and Taonan area have relatively low total rare-earth element (ΣREE), ranging from 76.34 × 10⁻⁶ to 126.39 × 10⁻⁶ (average = 106.35 × 10⁻⁶) and from 51.58 × 10⁻⁶ to 107.58 × 10⁻⁶ (average = 86.01 × 10⁻⁶), respectively. The fractionation coefficients of light and heavy rare earth elements (La/Yb) _N range from 11.82 to 26.13 and 8.15 to 18.27, respectively, indicating obvious fractionation characteristics. In the chondrite normalized rare-earth element (REE) diagram, all samples show the obvious right-leaning type feature, with enrichment in light rare-earth elements (LREEs) and depletion in heavy rare-earth elements (HREEs) (Figure 5). The granitic rocks from the Gegenmiao and Taonan areas show minor negative to positive values, with Eu anomalies (δEu) ranging from 0.97 to 1.19 (average = 1.07) and 0.56 to 1.30 (average = 0.95), respectively (Figure 5). In the primitive mantle-normalized trace element diagram, the granitic rocks from the Gegenmiao and Taonan area display similar trace element patterns, characterized by a clear right-leaning trend, with enrichments in K, La, Zr, and Sm, and depletions in Nb, P, Hf, and Ti (Figure 5).

4.2. Zircon U-Pb Ages

Five samples were selected for zircon U-Pb dating, including monzogranite (B16022) from the Gegenmiao area, as well as granodiorites (B17020, B17028, B17033) and monzogranite (B17030) from the Taonan area (Figure 2). Representative cathodoluminescence (CL) images of zircons, along with their corresponding spot ages from the granitic rock samples in the Gegenmiao and Taonan areas, are presented in Figure 6. The zircon U-Pb data are provided in Table 3.

Zircon grains from the monzogranite (sample B16022) range in size from 90 to 200 μm, with length/width ratios varying from 1:1 to 3:1. These zircons are predominantly grey and exhibit a mostly euhedral prismatic to stumpy shape, commonly displaying banded oscillatory zoning (Figure 6). Thirty analyses were performed on thirty zircons from sample B16022, with the results presented in Table 2. The zircons show low concentrations of Th (12.3~483.3 ppm) and U (16.8~422.7 ppm), with moderate to high Th/U ratios (0.12~1.48). Of the thirty analyses, eight were discordant, while the remaining twenty-two were concordant (Figure 7a). The ²⁰⁶Pb/²³⁸U ages range from 136.7 ± 5.2 to 153.0 ± 3.5 Ma, with a weighted average age of 141.4 ± 2.0 Ma (n = 22, MSWD = 2.0), which is interpreted to represent the crystallization age of the Gegenmiao monzogranite, indicating an Early Cretaceous formation.

The zircons from the Taonan granodiorite (B17020) are characterized by a gray color and a long columnar, subhedral to euhedral shape. A few grains are colorless and granular. The zircons range in length from 90 to 240 μm, with length/width ratios varying from 1:1 to 2:1. They exhibit weak or clear magmatic oscillatory zoning in the CL images (Figure 6). A total of 30 U-Pb isotopic analyses were performed on 30 zircon grains, with the results presented in Table 2. The Th and U concentrations in these zircons range from 17.5 to 309.6 ppm and 27.0 to 989.1 ppm, respectively, with moderate to high Th/U ratios (0.02~1.07). Of the 30 analyses, twenty points lie on or near the concordia line, with ages ranging from 145.9 ± 3.7 Ma to 166.4 ± 4.2 Ma, yielding a weighted average age of 154.2 ± 2.9 Ma (n = 20, MSWD = 2.2) (Figure 7b). These results indicate that the granodiorite crystallized during the Late Jurassic.

Zircons from the Taonan granodiorite (B17028) are gray, subhedral to euhedral crystals, ranging in length from 60 to 200 μm, with aspect ratios of 1:1 to 2:1. In the CL images (Figure 6), most zircons exhibit oscillatory zoning. Thirty zircons were analyzed by U-Pb isotopic dating, and their Th/U ratios ranging from 0.08 to 1.37. Twenty-one analyses from sample B17028 yield concordant ²⁰⁶Pb/²³⁸U ages ranging from 148.1 ± 3.3 Ma to 163.3 ± 8.3 Ma. The weighted mean age of 152.3 ± 1.9 Ma (MSWD = 1.7) (Figure 7c) is interpreted as the crystallization age of the granodiorite, indicating that it formed during the Late Jurassic.

Zircons from sample B17030 are columnar, subhedral to euhedral crystals, ranging in length from 50 to 180 μm, with aspect ratios of 1:1 to 3:1. In CL images (Figure 6), most zircons display oscillatory zoning, and the majority of analyses show Th/U ratios ranging from 0.30 to 2.3. A few zircons display inherited cores. Thirty U-Pb isotopic analyses were conducted on 30 zircon grains. Ten measurement points fall on the concordia curve, yielding a ²⁰⁶Pb/²³⁸U weighted average age was calculated as 158.7 ± 1.9 Ma (n = 10, MSWD = 0.78) (Figure 7e), which is interpreted as the emplacement age of the monzogranite (sample B17030). Additionally, nine effective points provide ²⁰⁶Pb/²³⁸U ages ranging from 255.3 ± 4.5 Ma to 264.0 ± 4.6 Ma. These points also plot on the concordia curve of the 206Pb/238U–207Pb/235U diagram, yielding a mean ²⁰⁶Pb/²³⁸U age of 260.3 ± 3.4 Ma (n = 9, MSWD = 0.31) (Figure 7f), indicating Late Permian magmatic activity. Furthermore, the ²⁰⁶Pb/²³⁸U ages of the No. 8 and No. 14 spots are 1556.2 ± 28.7 Ma and 932.7 ± 19.6 Ma, respectively, suggesting the presence of Meso- to Neoproterozoic basement materials in the study area.

The zircon grains extracted from sample B17033 are gray or gray-white in color, columnar in shape, with subhedral to euhedral crystals ranging in length from 150 to 400 μm and length/width ratios of 1:1 to 3:1. They exhibit weak or clear magmatic oscillatory zoning in the CL images (Figure 6) and generally show Th/U ratios ranging from 0.39 to 1.00. Thirty zircon grains from sample B17033 were analyzed, three of which were meaningless due to Pb loss. Thirteen analyses from sample B17033 yielded concordant ²⁰⁶Pb/²³⁸U ages ranging from 141.1 ± 3.9 to 150.7 ± 3.4 Ma. The weighted mean age of 144.9 ± 1.6 Ma (n = 13, MSWD = 0.63) (Figure 7d) is interpreted as the crystallization age of the granodiorite (sample B17033), suggesting that it formed in the Early Cretaceous. The remaining fourteen analyses may represent the crystallization ages of inherited or captured zircons.

4.3. Whole-Rock Sr-Nd Isotopes

Two samples from the Gegenmiao area and eight samples from the Taonan area were selected for Sr-Nd isotope analysis. These included monzogranite samples (B16022, B16023) from the Gegenmiao area, and granodiorite samples (B17020-1, B17020-2, B17028-1, B17028-2, B17033-1, B17033-2), along with monzogranite samples (B17030-1, B17030-2) from the Taonan area (Figure 2). The Sm-Nd radiogenic isotopic data for these samples are presented in Table 4.

The Gegenmiao granitic rocks have initial ⁸⁷Sr/⁸⁶Sr ratios [(⁸⁷Sr/⁸⁶Sr)_i] of 0.702371 and 0.703987, and ¹⁴³Nd/¹⁴⁴Nd ratios of 0.512610 and 0.512600. The age-corrected εNd(t) values are 2.8 and 2.1, respectively, with single-stage model ages (tDM) of 851 Ma and 1006 Ma. In contrast, the Taonan granitic rocks exhibit higher(⁸⁷Sr/⁸⁶Sr)_i ratios (0.704324–0.705226), lower ¹⁴³Nd/¹⁴⁴Nd ratios (0.512384–0.512500), and lower εNd(t) values (−1.5 to +0.7) compared to the Gegenmiao granitic rocks. The corresponding single-stage Nd model ages are strikingly older, ranging from 977 to 1250 Ma.

4.4. Zircon Hf Isotopes

Based on the zircon U-Pb isotopic analyses, LA-MC-ICP-MS was carried out to analyze the isotopic composition of Lu-Hf. Five of these samples (B16022, B17020, B17028, B17030, and B17033) were analyzed for Hf isotopes. The locations and data of the analyzed zircon points are shown in Figure 4 and Table 5. The Lu-Hf isotopic data for the Gegenmiao and Taonan granitic rocks were obtained from the same zircon locations where the zircon U-Pb dating was conducted (or close to them). All analyses yielded ¹⁷⁶Lu/¹⁷⁷Hf ratios of <0.002, indicating that that the ¹⁷⁶Hf formed by radiation can be negligible, and the ¹⁷⁶Lu/¹⁷⁷Hf values represent the Hf isotope characteristics of magma crystallization [29].

Ten zircon Hf isotopic analyses of the Gegenmiao monzogranite (B16022) show ¹⁷⁶Hf/¹⁷⁷Hf ratios ranging from 0.282743 to 0.283022. The calculated εHf(t) values range from 2.11 to 6.48, with the exception of point 10, which has an εHf(t) value of 12.05. The single-stage zircon Hf model ages (TDM1) vary between 542 and 713 Ma, while the two-stage zircon Hf model ages (TDM2) range from 699 to 943 Ma.

Ten zircon spots from the Taonan granodiorite (B17020) were analyzed for Lu-Hf isotopic compositions. The ¹⁷⁶Hf/¹⁷⁷Hf ratios range from 0.282726 to 0.282872, and the εHf(t) values vary from 2.10 to 6.89. The single-stage zircon Hf model ages (TDM1) range from 539 to 756 Ma, while the two-stage Hf model ages (TDM2) range from 686 to 1007 Ma.

Ten zircon spots from the Taonan granodiorite (B17028) were analyzed for Lu-Hf isotopic compositions. The zircons exhibit relatively homogeneous Hf isotopic compositions, with ¹⁷⁶Hf/¹⁷⁷Hf ratios ranging from 0.282720 to 0.282872, calculated for the inferred time of formation. The εHf(t) values range from 1.57 to 3.86. The single-stage model ages (TDM1) range from 530 to 744 Ma, while the two-stage model ages (TDM2) range from 683 to 982 Ma.

Ten zircon spots from the Taonan monzogranite (B17030) were analyzed for Hf isotopic compositions, yielding ¹⁷⁶Hf/¹⁷⁷Hf ratios ranging from 0.282645 to 0.282843 and εHf(t) values between 2.34 and 6.02, with the exception of point 10, which has an εHf(t) value of −0.95. The TDM1 and TDM2 model ages range from 576 to 851 Ma and from 739 to 1128 Ma, respectively.

A total of 10 zircon spots from the Taonan granodiorite (B17033) were analyzed for Lu-Hf isotopic compositions. The zircons have ¹⁷⁶Hf/¹⁷⁷Hf ratios ranging from 0.282715 to 0.282914, corresponding to εHf(t) values ranging from 0.90 to 8.25. The TDM1 and TDM2 model ages vary from 572 to 766 Ma and from 603 to 1013 Ma, respectively.

5. Discussion

5.1. Petrogenesis

Granitic rocks are commonly classified into I-, S-, M-, and A-types [30,31]. The 10,000 × Ga/Al ratios of the Gegenmiao and Taonan granitic rocks range from 2.5 to 2.9 (average 2.7) and 2.1 to 2.4 (average 2.3), respectively, which are either lower than or approximately equal to the A-type granite value of 2.6 [32]. The Zr, Y, Ce and Nb contents of the Gegenmiao and Taonan granitic rocks are lower than those of the A-type granites. The combined contents of (Zr + Y + Ce + Nb) of the Gegenmiao and Taonan granitic rocks range from 124.43 × 10⁻⁶ to 349.4 × 10⁻⁶ and from 88.75 × 10⁻⁶ to 236.54 × 10⁻⁶, respectively, both of which are lower than the inferior limit value of A-type granites (350 × 10 ⁻⁶). Furthermore, the Gegenmiao and Taonan granitic rocks do not contain any alkaline dark minerals. The calculated zircon saturation temperatures for the Gegenmiao and Taonan granitic rocks range from 720 to 815 °C (average 752 °C) and from 711 to 798 °C (average 751 °C), respectively, which are significantly lower than the typical zircon saturation temperature of A-type granites (greater than 900 °C) [33]. Most of the samples fall within the I- and S-type fields (Figure 8a,b). These characteristics suggest that the Gegenmiao and Taonan granitic rocks in the study area are likely I-type or S-type granites. The Gegenmiao and Taonan granitic rocks are predominantly peraluminous, with A/CNK values ranging from 0.99 to 1.16 (average 1.06) and 1.01 to 1.20 (average 1.11), respectively, which are different from the strongly peraluminous characteristic of S-type granites [34]. The P₂O₅ content in most samples is less than 0.11% and exhibits a significant negative correlation with SiO₂ content (Figure 8c). Additionally, the Al₂O₃ content shows a significant negative correlation with SiO₂ content (Figure 8d). These characteristics are consistent with those of I-type granites [34,35]. The samples from the Gegenmiao and Taonan areas exhibit high differentiation indices (DI), ranging from 76.48 to 91.77 and 83.94 to 95.66, respectively, indicating that the rocks have undergone strong fractionation. Most of the samples fall within the fractionated granite field (Figure 8a,b). The calculated zircon saturation temperatures for the Gegenmiao and Taonan granitic rocks are closer to those of highly fractionated I-type granites (764 °C) [36]. Therefore, the granitic rocks in Gegenmiao and Taonan areas are classified as highly fractionated I-type granites.

The Gegenmiao granitic rocks are typically characterized by high SiO₂ (65.81%~73.83%), high Al₂O₃ (13.65%~15.38%), low MgO (0.31%~1.33%), low Mg# (26.12~40.26), high Sr (210~631 ppm), and low Y and Yb (5.88~9.05 ppm and 0.56~0.93 ppm, respectively). Similarly, the Taonan granitic rocks display similar characteristics, including high SiO₂ (70.64~77.95%) and Al₂O₃ (13.01~15.25%), low MgO (0.04~1.11t%), low Mg# (3.65~28.58), high Sr (132.76~751.32 ppm), and low Y and Yb (4.65~11.09 ppm and 0.38~0.91 ppm, respectively). Through the comparison and analysis, it can be found that the Gegenmiao and Taonan granitic rocks are chemically consistent with adakites. All samples plot in the field of the adakite in the Sr/Y vs. Y and (La/Yb)_N vs. (Yb)_N (Figure 9a,b). These suggest that the Gegenmiao and the Taonan granitic rocks in the central Great Xing’ an Range belong to adakitic rocks.

Currently, several genetic models have been proposed to explain the origin of adakitic rocks, including (1) partial melting of subducted oceanic slabs [39,40]; (2) mixing of acidic and basic magmas [41,42]; (3) fractional crystallization of parental basaltic magmas [43,44]; (4) partial melting of the delaminated lower crust [45,46]; or (5) partial melting of thickened mafic lower crust [47,48].

Granitic rocks from the Gegenmiao and Taonan areas exhibit high K₂O (average = 2.48%) and Rr/Sr values, and lower Mg # values and Cr contents, which are obviously different from the adakite formed by partial melting of subducted oceanic slabs with lower K contents (<1.72%) and Rr/Sr ratios (0.04~0.05), and higher Mg # values (Mg # > 47) and Cr contents (Cr > 36 × 10⁻⁶) [39,49]. The granitic rocks from the Gegenmiao and Taonan areas display significantly higher SiO₂, and lower MgO and Mg# values, compared to adakitic rocks formed magmas by the mixing of acidic and basic magmas. These characteristics, coupled with the general absence of mafic components in the region, suggest that magma mixing did not play a major role during their formation. The high SiO₂ contents and insignificant negative Eu anomalies of the granitic rocks from the Gegenmiao and Taonan areas indicate that they are not the products of primary basaltic magma by fractional crystallization. In addition, in the Rb vs. Rb/Sr (Figure 10a) diagrams, the study samples do not display the characteristic evolutionary trends associated with fractional crystallization [50], indicating that they cannot be derived from primary basaltic magma by fractional crystallization. Thus, the granitic rocks in the Gegenmiao and Taonan areas are likely the result of partial melting of thickened lower crust or delaminated lower crust. The partial melting of thickened mafic lower crust material generates adakitic magmas with notably lower MgO (<2.5%), Mg# (<50), Cr (<36 × 10⁻⁶), and Rb/Sr ratios (0.01~0.40) [51,52], which aligns with the geochemical characteristics observed in the Gegenmiao and Taonan granitic rocks. Additionally, in the TiO₂% vs. SiO₂% (Figure 10b) and MgO% vs. SiO₂% (Figure 10c) diagrams, most of the samples fall within the adakite field associated with partial melting of the thickened lower crust.

Both the Gegenmiao and Taonan granitic rocks are enriched in Sr and depleted in HREEs and Y, suggesting that the residual phase in the magma source is dominated by garnet without plagioclase. The Eu anomalies (δEu) values also suggests that the magmas from the source areas did not have obviously separated crystallization of plagioclase during their evolution, or that plagioclase was absent in residue of the source areas. It has been proposed that the rocks are strongly depleted in Y and HREE with steep HREE patterns, and have high Y/Yb (>10) ratios, suggestive of garnet-bearing residues during the partial melting as residual hornblende will generate melts with flat HREE patterns and Y/Yb ≈ 10 [54]. The granitic rocks from the Gegenmiao area have lower Y/Yb ratios (7.31~10.96) and exhibit flat HREE patterns (Figure 5). In comparison, the granitic rocks from the Taonan area show higher Y/Yb ratios (11.21~15.93) and steeper HREE patterns (Figure 5). The Sr/Y vs. Y and (La/Yb) _N vs. (Yb) _N diagrams (Figure 9a,b) further suggest that the Gegenmiao and Taonan granitic rocks may have formed by the partial melting of thickened mafic lower crust, with approximately 10%~25% garnet–amphibolite residual phase.

In the εHf(t) vs. age diagram, the majority of εHf(t) values for the Gegenmiao and Taonan granitic rocks are positive, and most of them plot in the region between the depleted mantle and the chondrite evolution line (Figure 11). Additionally, the granitic rocks from the study area yield relatively young two-stage model ages (TDM2), ranging from 699 Ma to 943 Ma for the Gegenmiao area, and 603 Ma to 1128 Ma for the Taonan area. These data suggest that the Gegenmiao and Taonan granitic rocks were derived from the partial melting of thickened lower crustal material during the Meso-Neoproterozoic.

5.2. The Age of Granitic Rocks in the Gegenmiao and Taonan Area

Zircon U-Pb dating of granitic rocks from the Gegenmiao area yielded an age of 141.4 ± 2.0 Ma (sample B16022), while zircon U-Pb dating of granitic rocks from the Taonan area provided ages of 154.2 ± 2.9 Ma (sample B17020), 152.3 ± 1.9 Ma (sample B17028), 158.7 ± 1.9 Ma (sample B17030), and 144.9 ± 0.8 Ma (sample B17033). These ages represent the crystallization ages of the magmas, indicating late Jurassic to early Cretaceous igneous activity in the study area. Previous studies on igneous rocks in the central Great Xing’an Range have yielded a wealth of zircon U-Pb age data [9,56,57,58,59,60,61]. These results suggest that Jurassic to Early Cretaceous magmatic activity was widespread in the central Great Xing’an Range. The ages obtained in this study are generally consistent with these regional magmatic events.

The dating results of 150 zircons from five samples reveal two prominent age peaks: 164~141 Ma and 265~250 Ma, with peak values at 153 Ma and 260 Ma, respectively (Figure 12). Permian igneous rocks are well developed in the Great Xing’an Range [62,63], and previous studies have suggested that Permian magmatic activity in the Great Xing’ an Range is related to post-collisional extension between the Xing’an and Songnen blocks [60,62,63]. The peak age range of 265~250 Ma obtained in this study is generally consistent with the ages of Permian granites, implying that the study area was also affected by the post-collisional extension of these blocks. Additionally, zircon U-Pb ages of 1556.2 ± 28.7 Ma and 932.7 ± 19.6 Ma obtained from the Taonan monzogranite (sample B17030) suggest the presence of the Meso-Neoproterozoic metamorphic basement in the study area, which aligns with the chronologic results for the Precambrian crystalline basement in the region [64,65,66].

5.3. Tectonic Setting and Geodynamics Implication

In the Y + Nb-Rb tectonic discrimination diagram (Figure 13a), all the samples from the Gegenmiao and Taonan areas fall within the volcanic arc granite field. In the R₁-R₂ structure discrimination diagram (Figure 13b), the sample points are situated in the syn-collision and post-orogenic granite regions. It is suggested that the granitic rocks from the study areas formed in a post-orogenic transitional environment from compression to extension.

Due to the superposition and interaction of the Paleo-Pacific and Mongolia–Okhotsk tectonic systems, a significant volume of magmatic rocks were generated in the Great Xing’an Range during the Late Mesozoic, particularly in the Late Jurassic to Early Cretaceous. Previous studies indicate that the Mongol–Okhotsk Ocean finally closed from the Late Jurassic possibly until the Early Cretaceous [67,68]. In this study, the formation of granitic rocks in the Gegenmiao and Taonan areas of the central Great Xing’an Range is dated to the Late Jurassic to Early Cretaceous, closer to the time of Mongol-Okhotsk Ocean closure. The study area lies on the southeastern margin of the Xing’ an block and the west of the Songliao basin. Previous studies suggest that the magmatic activity related to the subduction of the Mongol-Okhotsk Ocean is primarily distributed in the western region of the Songliao basin [69,70]. Therefore, the formation of granitic rocks in the Gegenmiao and Taonan areas is closely associated with the Mongolia–Okhotsk tectonic system. Furthermore, Shi et al. [56] proposed that early Middle Jurassic to Early Cretaceous magmatic activity in the Great Xing’an Range may not be related to the Paleo-Pacific tectonic system. In conclusion, the formation of the granitic rocks in the Gegenmiao and Taonan areas of the Great Xing’an Range is strongly linked to the closure of the Mongol–Okhotsk Ocean.

The regional stratigraphic unconformity observed in northern Hebei and western Liaoning [71], the thrust-nappe structures in the Great Xing’ an Range associated with the evolution of the Mongolia–Okhotsk Orogenic Belt [72], the Middle Jurassic adakitic granitic rocks in the Xing’ an block [73], and the Late Jurassic–Early Cretaceous granitic rocks discussed in this paper, which display adakitic characteristics and are formed by partial melting of a thickened lower crust, collectively indicate a widespread continental crust thickening event across the region during the Middle Jurassic. Following intense intracontinental compression, significant extension occurred in the Early Cretaceous (145~120 Ma) due to gravitational collapse or delamination [69,70]. This extensional event resulted in the formation of numerous igneous rocks in the western Songliao basin [69,70,74]. The granitic rocks from the study areas formed in a post-orogenic transitional environment from compression to extension. Moreover, a large number of Late Jurassic to Early Cretaceous magmatic rocks associated with the post-collisional extensional tectonics following the closure of the Mongol–Okhotsk Ocean have been discovered in the Great Xing’ an Range [74,75,76,77]. Based on the above discussion, we propose that the Late Jurassic to Early Cretaceous granitic rocks in the Gegenmiao and Taonan areas of the Great Xing’ an Range may have formed in a transitional environment from compression to extension after the closure of the Mongol–Okhotsk Ocean and the thickening of the continental crust.

Figure 13. Tectonic setting discrimination diagrams of the granitic rocks from the central Great Xing’an Range. (a) Y + Nb-Rb diagram (modified from [78]); (b) R₁-R₂ diagram (modified from [79]), R₁ = 4Si-11(Na + K) − 2(Fe + Ti), R₂ = 6Ca + 2Mg + Al.

6. Conclusions

Zircon U-Pb dating of the granitic rocks in the Gegenmiao and Taonan areas yields ages ranging from 141.4 ± 2.0 Ma to 158.7 ± 1.9 Ma, indicating their formation during the Late Jurassic to Early Cretaceous. The granitic rocks from the Gegenmiao and Taonan areas in the central Great Xing’ an Range are characterized by high silica, high alumina, high alkalis, and low iron, magnesium, and calcium contents, along with a weak negative Eu anomaly. These rocks belong to the calc-alkaline series and peraluminous, classified as highly fractionated I-type granites with adakite features. They are interpreted to have formed through partial melting of thickened lower crustal material during the Meso-Neoproterozoic. The Gegenmiao and Taonan granitic rocks were formed in a transitional environment from post-orogenic compression to extension. The formation of granitic rocks in the Gegenmiao and Taonan areas is closely associated with the Mongolia–Okhotsk tectonic system, which may be related to a transition environment from compression to extension after the closure of the Mongol–Okhotsk Ocean and the thickening of the continental crust.

Author Contributions

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

Funding

This research was funded by a project from the China Geological Survey (No. DD20230089, No. DD20190039 and No. DD202402079).

Data Availability Statement

The original contributions presented in this study are included in the article. Further inquiries can be directed to the corresponding author.

Conflicts of Interest

Author Sizhe Ni was employed by the company Shenyang Geotechnical Investigation & Surveying Research Institute Co., Ltd. The remaining authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

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Figure 1. (a) Tectonic sketch map of Central Asian Orogenic Belt; (b) tectonic sketch map of NE China.

Figure 2. Simplified geological map of the study area.

Figure 3. Field photographs and microphotographs of tonalite (a,b) and monzogranite (c,d) from Gegenmiao pluton, as well as granodiorite (e,f), tonalite (g,h), and monzogranite (i,j) from Taonan pluton. Mineral abbreviations: Q–quartz; Pl–plagioclase; Kf–K-feldspar; Bt–biotite.

Figure 4. (a) TAS diagrams (modified from [26]); (b) SiO₂ versus K₂O diagrams (modified from [27]); (c) A/NK vs. A/CNK diagrams from the granitic rocks in the central Great Xing’an Range (modified from [27]).

Figure 5. Chondrite-normalized REE patterns (normalization values after Sun and McDonough [28]) and primitive mantle-normalized trace element spidergrams (normalization values after Sun and McDonough [28]) of the granitic rocks in the central Great Xing’an Range.

Figure 6. Cathodoluminescence (CL) images of some zircons from the granitic rocks in the central Great Xing’ an Range (The red circles represent zircon U-Pb analysis, and the yellow circles represents Hf isotopic analyses).

Figure 7. U-Pb zircon concordia diagrams for sample B16022 (a), B17020 (b), B17028 (c), B17033 (d), and B17030 (e,f) from the granitic rocks in the central Great Xing’an Range.

Figure 8. (a) (Zr + Nb + Ce + Y)-(Na₂O + K₂O)/CaO diagram (modified from [32]); (b) (Zr + Nb + Ce + Y)-(TFeO/MgO) diagram (modified from [32]); (c) SiO₂-P₂O₅ diagram (modified from [37]); (d) SiO₂-Al₂O₃ diagram (modified from [37]) of the granitic rocks from the central Great Xing’an Range. A—A-type granite, FG—fractionated granite, OGT—unfractionated I, S, and M-type granite.

Figure 9. (a) Y vs. Sr/Y diagram (modified from [38]); (b) Yb_N-(La/Yb)_N diagram (modified from [39]) diagrams of the granitic rocks from the central Great Xing’an Range.

Figure 10. (a) Rb-Rb/Sr diagram (modified from [50]); (b) SiO₂-MgO diagram (modified from [52]); (c) SiO₂-TiO₂ (modified from [53]) diagrams of the granitic rocks from the central Great Xing’an Range.

Figure 11. Diagram of εHf(t)-Age(Ma)for the granitic rocks from the central Great Xing’an Range (modified from [55]).

Figure 12. Frequency histogram of zircon U-Pb dating of the granitic rocks from the central Great Xing’an Range.

Table 1. Sample locations of the granitic rocks in the central Great Xing’ an Range.

Location		Sample No.	Latitude and Longitude	Rock Type
Gegenmiao area		D16017	45°54′37.4″ N 122°18′16.9″ E	Tonalites
		D16018	45°54′39.1″ N 122°18′28.2″ E	Tonalites
		D16022	45°54′28.4″ N 122°19′8.1″ E	Monzogranite
		D16023	45°54′27.2″ N 122°18′40.9″ E	Monzogranite
Taonan area	Xiaoyu village	D17020	45°24′9.9″ N 122°15′59.2″ E	Granodiorite
	Xiaoyu village	D17028	45°22′45.8″ N 122°17′24.9″ E	Granodiorite
	Dapaozitun village	D17029	45°26′3.6″ N 122°8′29.1″ E	Tonalites
	Dapaozitun village	D17030	45°26′35.3″ N 122°8′55.2″ E	Monzogranite
	The east of Jinshan village	D17033	45°42′57.1″ N 122°10′12.6″ E	Granodiorite

Table 2. Major elements (wt. %), trace elements and REE (ppm) of the granitic rocks from the central Great Xing’an Range.

Sample No	B16017	B16018-1	B16018-2	B16022	B16023	B17020-1	B17020-2	B17020-3	B17020-4	B17020-5	B17028-1	B17028-2
Major elements (wt.%)
SiO₂	65.81	66.51	69.94	73.13	73.83	72.45	72.45	72.02	70.84	72.47	77.95	75.08
Al₂O₃	15.38	15.34	14.16	14.53	13.65	14.97	15.02	14.82	15.05	14.86	13.01	14.52
Fe₂O₃	0.73	0.75	1.83	0.82	1.01	0.73	0.63	0.55	0.70	0.44	0.77	0.57
FeO	2.34	2.29	1.84	0.58	0.72	0.85	1.12	1.03	1.26	1.28	0.40	0.58
CaO	2.98	2.71	1.25	0.71	1.28	1.70	1.72	1.77	1.91	1.73	0.21	0.25
MgO	1.07	1.11	1.30	0.31	0.32	0.24	0.24	0.23	1.10	0.26	0.02	0.04
K₂O	2.32	2.21	1.13	4.11	2.36	2.92	3.10	3.08	3.12	3.17	0.24	0.63
Na₂O	4.34	4.58	5.56	4.14	5.46	4.78	4.60	4.75	4.63	4.69	6.19	7.19
TiO₂	0.61	0.58	0.49	0.20	0.16	0.18	0.19	0.19	0.21	0.19	0.19	0.25
P₂O₅	0.22	0.20	0.12	0.10	0.08	0.07	0.07	0.07	0.08	0.07	0.06	0.07
MnO	0.04	0.03	0.05	0.04	0.04	0.05	0.05	0.05	0.06	0.05	0.02	0.03
LOI	3.81	3.51	2.40	1.21	0.86	0.92	0.89	1.06	0.96	0.88	0.73	0.89
SUM	99.64	99.83	100.07	99.88	99.77	99.87	100.09	99.64	99.92	100.09	99.79	100.08
Mg#	39.12	40.26	40.16	29.75	26.12	22.09	20.07	21.46	51.22	21.67	3.65	5.75
K₂O/Na₂O	0.53	0.48	0.20	0.99	0.43	0.61	0.67	0.65	0.67	0.68	0.04	0.09
Na₂O + K₂O	6.95	7.05	6.85	8.36	7.91	7.78	7.76	7.94	7.84	7.92	6.49	7.88
σ	1.88	1.91	1.64	2.25	1.98	2.00	2.00	2.10	2.15	2.09	1.18	1.90
DI	76.48	77.76	83.71	91.77	90.72	87.71	87.11	87.53	84.07	87.26	95.12	95.56
A/NK	1.59	1.55	1.37	1.29	1.18	1.36	1.38	1.33	1.37	1.33	1.25	1.16
A/CNK	1.02	1.03	1.12	1.16	0.99	1.06	1.07	1.03	1.04	1.04	1.20	1.12
T_zr°C	745	749	815	729	720	737	737	734	736	731	770	784
Tarce elements (ppm⁶)
La	22.20	24.00	41.40	20.40	14.30	16.08	15.84	19.60	19.84	20.45	17.14	18.38
Ce	46.60	49.30	83.00	42.70	31.00	30.77	30.65	38.26	38.67	43.44	30.07	33.60
Pr	5.79	5.79	9.52	4.80	3.43	3.60	3.52	4.38	4.45	4.94	4.33	4.56
Nd	23.70	23.40	36.80	18.30	12.60	12.95	12.61	15.63	15.90	17.45	16.82	17.45
Sm	4.47	4.66	7.81	3.40	2.61	2.33	2.20	2.79	2.84	2.83	3.63	3.73
Eu	1.29	1.56	1.31	0.98	0.96	0.78	0.78	0.78	0.81	0.78	0.69	0.60
Gd	3.36	3.51	6.79	2.62	2.21	1.91	1.74	2.13	2.30	2.18	2.52	2.67
Tb	0.44	0.44	1.07	0.33	0.29	0.27	0.26	0.29	0.33	0.26	0.37	0.39
Dy	1.93	2.11	6.36	1.50	1.42	1.55	1.52	1.65	1.94	1.47	2.03	2.20
Ho	0.33	0.36	1.33	0.24	0.24	0.25	0.24	0.26	0.33	0.22	0.30	0.34
Er	0.92	0.97	3.86	0.62	0.61	0.70	0.70	0.68	0.95	0.57	0.81	0.96
Tm	0.15	0.18	0.73	0.09	0.09	0.09	0.09	0.08	0.12	0.07	0.11	0.12
Yb	0.83	0.93	4.54	0.56	0.61	0.63	0.66	0.66	0.85	0.55	0.76	0.91
Lu	0.13	0.13	0.72	0.08	0.09	0.07	0.07	0.07	0.09	0.05	0.08	0.09
Y	7.76	9.05	33.20	6.14	5.88	7.97	7.78	8.01	10.49	6.61	9.63	11.09
ΣREE	112.14	117.34	205.24	96.62	70.46	71.98	70.88	87.26	89.42	95.27	79.66	86.00
LREE	104.05	108.71	179.84	90.58	64.90	66.51	65.61	81.44	82.51	89.89	72.67	78.32
HREE	8.09	8.63	25.40	6.04	5.56	5.47	5.27	5.83	6.91	5.38	6.98	7.68
L/H	12.86	12.60	7.08	15.00	11.68	12.17	12.44	13.98	11.94	16.70	10.41	10.19
La_N/Yb_N	19.19	18.51	6.54	26.13	16.82	18.25	17.32	21.17	16.84	26.50	16.13	14.47
δEu	0.98	1.13	0.54	0.97	1.19	1.09	1.18	0.94	0.94	0.92	0.66	0.56
Li	30.30	37.30	40.70	7.64	6.20	24.66	24.89	23.77	28.99	24.94	3.96	4.19
Be	2.16	2.52	2.32	1.82	1.73	2.64	2.41	2.56	2.57	2.54	1.79	2.02
Sc	5.31	6.05	11.30	2.60	2.75	3.19	3.16	3.34	3.54	3.06	2.78	3.51
V	55.60	53.90	64.20	17.80	14.80	16.33	14.16	16.13	16.41	16.00	15.43	14.24
Cr	18.40	14.10	25.40	14.20	16.00	3.37	1.84	4.64	2.69	6.36	4.65	4.18
Co	4.97	6.10	9.20	1.97	1.93	2.68	3.05	3.62	4.64	3.46	3.01	2.52
Ni	5.59	5.90	9.48	4.72	3.18	1.92	1.94	2.22	2.28	1.90	2.12	2.17
Ga	21.60	22.10	22.20	21.00	20.40	17.35	17.39	18.09	18.28	17.64	14.50	17.12
Rb	59.10	60.30	51.30	125.00	58.10	75.97	80.27	80.70	85.58	81.96	11.74	24.82
Sr	575.00	631.00	210.00	355.00	324.00	509.21	498.84	494.45	503.52	497.76	132.76	157.53
Zr	143.00	142.00	220.00	82.10	82.50	102.70	103.56	104.94	110.82	99.49	94.57	125.96
Nb	5.54	5.45	13.20	5.87	6.68	8.21	8.38	8.15	9.63	8.48	8.50	9.79
Ba	663.00	652.00	223.00	599.00	529.00	786.96	807.98	823.27	782.94	794.60	67.35	92.81
Hf	0.65	0.63	6.50	0.62	0.72	0.85	0.80	0.82	0.89	0.77	0.59	0.80
Ta	0.37	0.43	1.05	0.39	0.50	0.39	0.42	0.39	0.49	0.53	0.39	0.94
Th	3.94	3.81	8.10	3.87	3.04	3.87	3.46	4.32	4.35	5.11	3.63	5.31
U	1.34	1.26	3.30	0.52	0.58	0.46	0.48	0.46	0.51	0.46	0.40	0.41
Sample No.	B17028-4	B17028-5	B17029-1	B17029-2	B17030-1	B17030-2	B17030-3	B17033-1	B17033-2	B17033-3	B17033-4	B17033-5
Major elements (wt.%)
SiO₂	73.53	73.56	70.69	71.50	70.64	71.28	71.53	73.45	72.78	73.21	73.94	74.20
Al₂O₃	15.25	14.93	14.92	14.92	15.23	15.24	15.17	14.66	15.11	15.04	14.66	14.67
Fe₂O₃	1.05	0.77	0.39	0.22	0.32	0.52	0.62	0.77	0.90	0.79	0.52	0.63
FeO	0.29	0.45	1.80	1.84	2.07	1.53	1.66	0.38	0.54	0.45	0.54	0.72
CaO	0.52	0.78	2.18	1.55	1.55	1.27	0.78	0.81	0.73	0.92	0.73	0.18
MgO	0.10	0.12	0.45	0.45	0.52	0.43	0.47	0.08	0.06	0.07	0.06	0.04
K₂O	1.26	2.06	2.66	2.81	2.40	2.31	2.39	3.23	3.33	3.18	3.18	2.06
Na₂O	6.49	5.74	4.86	4.86	5.14	5.08	5.34	5.15	5.07	4.99	4.90	6.50
TiO₂	0.25	0.26	0.33	0.32	0.39	0.37	0.38	0.13	0.14	0.14	0.13	0.13
P₂O₅	0.07	0.08	0.11	0.10	0.13	0.12	0.12	0.05	0.05	0.04	0.02	0.04
MnO	0.02	0.02	0.05	0.04	0.05	0.04	0.04	0.03	0.05	0.04	0.03	0.05
LOI	1.09	1.07	1.50	1.15	1.47	1.27	1.21	0.83	0.93	0.98	0.90	0.60
SUM	99.93	99.83	99.94	99.75	99.90	99.45	99.69	99.57	99.70	99.85	99.58	99.82
Mg#	13.09	16.20	27.31	28.58	28.41	27.94	27.51	11.73	7.30	9.29	9.10	5.68
K₂O/Na₂O	0.19	0.36	0.55	0.58	0.47	0.45	0.45	0.63	0.66	0.64	0.65	0.32
Na₂O + K₂O	7.84	7.89	7.64	7.77	7.66	7.52	7.85	8.49	8.51	8.27	8.19	8.62
σ	1.96	3.36	2.03	2.05	2.04	1.91	2.08	2.30	2.36	2.20	2.10	2.34
DI	93.05	92.23	83.94	86.18	85.21	86.94	88.77	92.83	92.26	91.64	92.72	95.66
A/NK	1.27	1.28	1.37	1.35	1.38	1.40	1.33	1.23	1.27	1.29	1.27	1.14
A/CNK	1.17	1.14	1.01	1.08	1.10	1.16	1.19	1.09	1.14	1.13	1.14	1.11
Tzr°C	784	767	763	771	784	791	798	708	716	714	711	730
Tarce elements (ppm)
La	18.50	18.25	21.45	19.50	21.02	20.05	18.46	10.11	11.87	10.50	15.32	10.24
Ce	37.11	34.76	44.61	40.60	44.33	44.68	40.53	19.21	23.83	17.62	22.28	20.38
Pr	4.43	4.21	5.33	4.74	5.29	5.68	4.91	2.30	2.81	2.31	3.39	2.35
Nd	16.06	15.27	20.13	17.53	20.34	19.42	18.72	9.04	10.24	8.55	12.52	8.49
Sm	2.96	2.70	3.40	3.07	3.52	3.40	3.37	1.66	1.95	1.83	2.46	1.59
Eu	0.61	0.70	0.92	0.96	0.97	0.87	0.82	0.64	0.58	0.68	0.76	0.42
Gd	2.33	2.13	2.36	2.16	2.44	2.51	2.33	1.25	1.39	1.47	1.78	1.22
Tb	0.30	0.32	0.28	0.26	0.30	0.30	0.28	0.19	0.20	0.25	0.25	0.17
Dy	1.73	1.77	1.41	1.29	1.49	1.52	1.47	1.13	1.15	1.57	1.39	1.02
Ho	0.29	0.30	0.20	0.19	0.22	0.22	0.22	0.20	0.18	0.25	0.22	0.14
Er	0.83	0.82	0.52	0.51	0.57	0.62	0.56	0.55	0.53	0.69	0.56	0.41
Tm	0.10	0.11	0.06	0.06	0.07	0.06	0.06	0.07	0.06	0.09	0.07	0.05
Yb	0.80	0.80	0.38	0.41	0.44	0.48	0.41	0.51	0.50	0.70	0.53	0.40
Lu	0.08	0.08	0.04	0.04	0.04	0.04	0.04	0.05	0.05	0.07	0.06	0.04
Y	8.96	9.28	6.07	5.85	6.53	6.40	6.41	6.26	5.81	8.40	6.39	4.65
ΣREE	86.14	82.22	101.08	91.32	101.05	99.87	92.20	46.92	55.35	46.57	61.58	46.93
LREE	79.67	75.89	95.83	86.40	95.47	94.10	86.82	42.97	51.28	41.49	56.72	43.47
HREE	6.47	6.33	5.25	4.93	5.58	5.77	5.38	3.95	4.07	5.09	4.86	3.46
L/H	12.32	11.99	18.27	17.54	17.10	16.32	16.15	10.88	12.61	8.15	11.67	12.58
La_N/Yb_N	16.60	16.38	40.38	33.87	34.04	30.07	32.14	14.09	16.96	10.79	20.85	18.60
La_N/Sm_N	0.69	0.86	0.94	1.09	0.96	0.87	0.85	1.30	1.02	1.23	1.05	0.88
Gd_N/Yb_N	18.50	18.25	21.45	19.50	21.02	20.05	18.46	10.11	11.87	10.50	15.32	10.24
δEu	0.69	0.86	0.94	1.09	0.96	0.87	0.85	1.30	1.02	1.23	1.05	0.88
Li	6.32	7.76	15.30	14.11	13.22	15.49	12.93	14.08	13.48	15.22	20.67	10.17
Be	2.89	2.94	2.19	2.39	2.25	3.04	2.79	2.60	2.58	3.18	2.95	2.45
Sc	3.61	3.85	3.93	3.92	4.51	4.82	4.72	3.06	3.17	3.10	2.81	2.86
V	18.08	19.94	26.78	24.83	29.14	28.84	29.39	12.93	11.04	14.14	10.42	9.69
Cr	4.96	3.62	5.26	6.88	7.37	4.14	16.31	7.43	4.27	7.62	5.08	3.53
Co	3.60	3.31	5.08	4.60	5.31	5.14	5.84	1.64	2.11	2.04	1.87	2.77
Ni	2.50	2.21	3.76	3.54	6.27	4.16	4.27	2.74	2.72	2.60	2.05	3.62
Ga	17.94	18.35	17.65	18.05	18.59	19.16	19.21	18.11	19.45	17.64	18.61	19.06
Rb	37.67	52.76	44.14	45.67	37.38	42.16	43.44	87.34	95.42	89.13	95.46	61.21
Sr	314.84	342.54	691.91	666.23	726.00	751.32	724.81	503.90	497.94	542.97	531.71	290.67
Zr	130.74	118.05	159.63	153.29	170.98	168.04	170.07	62.87	67.44	66.87	61.39	72.00
Nb	8.61	8.99	5.33	5.61	6.09	6.14	5.09	6.28	6.26	6.85	6.31	6.73
Ba	238.91	359.75	1100.00	957.98	991.47	1100.00	890.90	776.77	775.87	760.64	748.25	393.33
Hf	0.74	0.67	0.39	0.49	0.72	1.03	0.74	0.53	0.49	0.48	0.51	0.51
Ta	0.45	0.39	0.34	0.36	0.58	0.55	0.95	0.50	0.51	0.51	0.36	0.32
Th	3.79	2.73	2.73	2.59	2.87	2.55	2.52	2.79	3.43	2.56	2.94	2.91
U	0.45	0.39	0.35	0.38	0.42	0.51	0.38	0.48	0.31	0.38	0.59	0.28

Note: Mg^# = 100 × (MgO)/(MgO + FeO^T) (mol), Rittmann index (σ) = (Na₂O + K₂O)²/(SiO₂ − 43) (wt%), differentiation index (DI) = Qz + Or + Ab +Ne + Lc + Kp, in which Qz, Or, Ab, Ne, Lc and Kp are calculated with CIPW, A/NK = Al₂O₃/(Na₂O + K₂O) (mol), A/CNK = Al₂O₃/(CaO + Na₂O + K₂O) (mol), T_zr°C = 129,000/[2.95 + 0.85M + ln496000/Zr_melt], M = [n(Na) + n(K) + 2n(Ca)]/n(Al) × n(Si), and L/H is LREE/HREE.

Table 3. Zircon U-Pb dating results of the granitic rocks from the Central Great Xing’ an Range.

Spot No.	Pb	Th	U	Th/U	Isotopic Ratios						Ages (Ma)
Spot No.	(10⁻⁶)			Th/U	²⁰⁷Pb/²⁰⁶Pb	1σ	²⁰⁷Pb/²³⁵U	1σ	²⁰⁶Pb/²³⁸U	1σ	²⁰⁷Pb/²³⁵U	1σ	²⁰⁶Pb/²³⁸U	1σ
B16022
1	19.6	85.7	107.4	0.80	0.0692	0.0038	0.2181	0.0152	0.0228	0.0008	200.4	12.7	145.2	4.8
2	3.02	15.2	16.8	0.90	0.0576	0.0057	0.1694	0.0160	0.0215	0.0009	158.9	13.9	137.4	5.5
3	17.0	82.2	164.0	0.50	0.0536	0.0031	0.1686	0.0134	0.0226	0.0007	158.2	11.6	144.3	4.6
4	34.6	177.6	193.2	0.92	0.0494	0.0017	0.1590	0.0064	0.0233	0.0005	149.8	5.6	148.7	3.0
5	14.3	71.7	141.2	0.51	0.0503	0.0016	0.1590	0.0063	0.0229	0.0005	149.8	5.6	145.9	3.3
6	23.2	42.2	907.2	0.05	0.0506	0.0009	0.1775	0.0049	0.0255	0.0007	165.9	4.3	162.2	4.5
7	85	483.3	327.0	1.48	0.0496	0.0015	0.1509	0.0047	0.0221	0.0005	142.7	4.1	140.7	3.0
8	47.8	220.5	315.4	0.70	0.0576	0.0031	0.1801	0.0113	0.0227	0.0006	168.2	9.8	144.4	3.6
9	50.0	140.9	252.6	0.56	0.0519	0.0011	0.2955	0.0100	0.0413	0.0012	262.9	7.9	260.9	7.3
10	22.4	116.6	241.0	0.48	0.0497	0.0015	0.1544	0.0064	0.0225	0.0006	145.8	5.6	143.4	3.9
11	102	229.6	203.1	1.13	0.0548	0.0012	0.4069	0.0129	0.0538	0.0014	346.7	9.3	338.0	8.5
12	5.24	26.3	22.6	1.17	0.0679	0.0059	0.2062	0.0196	0.0220	0.0008	190.4	16.5	140.4	5.1
13	63	168.7	565.0	0.30	0.0518	0.0009	0.2499	0.0102	0.0349	0.0013	226.5	8.3	221.4	8.2
14	13.1	52.8	422.7	0.12	0.0496	0.0011	0.1496	0.0047	0.0219	0.0004	141.5	4.2	139.4	2.7
15	46.1	263.0	288.7	0.91	0.0496	0.0013	0.1474	0.0042	0.0215	0.0003	139.6	3.7	137.4	1.9
16	6.2	26.5	40.6	0.65	0.0709	0.0107	0.2154	0.0403	0.0215	0.0008	198.1	33.7	137.4	5.2
17	2.29	12.3	20.0	0.61	0.0533	0.0072	0.1567	0.0215	0.0214	0.0008	147.8	18.9	136.7	5.2
18	14.5	81.6	90.0	0.91	0.0502	0.0024	0.1499	0.0077	0.0216	0.0004	141.8	6.8	138.0	2.6
19	10.7	41.9	320.5	0.13	0.0497	0.0014	0.1542	0.0046	0.0225	0.0004	145.6	4.0	143.5	2.7
20	3.33	17.0	20.8	0.82	0.0574	0.0074	0.1769	0.0211	0.0226	0.0009	165.4	18.2	143.9	5.7
21	6.0	33.2	33.5	0.99	0.0573	0.0052	0.1687	0.0140	0.0215	0.0007	158.3	12.2	137.1	4.3
22	20.2	111.5	155.6	0.72	0.0504	0.0017	0.1512	0.0053	0.0217	0.0004	142.9	4.7	138.6	2.6
23	20.2	113.2	89.0	1.27	0.0566	0.0049	0.1701	0.0167	0.0217	0.0005	159.5	14.5	138.5	3.4
24	32.8	188.8	201.9	0.94	0.0512	0.0031	0.1540	0.0105	0.0218	0.0004	145.4	9.2	138.8	2.8
25	4.72	23.0	47.0	0.49	0.0521	0.0031	0.1649	0.0100	0.0229	0.0006	155.0	8.7	146.2	3.7
26	184	477.8	451.0	1.06	0.0521	0.0008	0.3469	0.0065	0.0482	0.0007	302.4	5.0	303.6	4.4
27	8.8	45.9	64.7	0.71	0.0494	0.0033	0.1580	0.0101	0.0232	0.0005	148.9	8.8	148.0	3.2
28	10.5	57.4	54.3	1.06	0.0490	0.0034	0.1516	0.0101	0.0225	0.0006	143.3	8.9	143.3	3.9
29	18.9	96.7	106.1	0.91	0.0504	0.0019	0.1669	0.0068	0.0240	0.0006	156.7	5.9	153.0	3.5
30	15.3	91.2	89.3	1.02	0.0501	0.0030	0.1481	0.0086	0.0215	0.0004	140.3	7.6	136.9	2.6
B17020
1	17.7	89.4	208.8	0.43	0.0490	0.0015	0.1603	0.0061	0.0237	0.0006	150.9	5.4	150.9	3.6
2	21.7	17.5	989.1	0.02	0.0493	0.0008	0.1724	0.0063	0.0253	0.0008	161.5	5.4	161.3	5.1
3	19.6	49.9	385.4	0.13	0.0508	0.0010	0.2540	0.0079	0.0362	0.0009	229.8	6.4	229.4	5.4
4	88	309.9	272.3	1.14	0.0520	0.0010	0.2706	0.0085	0.0377	0.0010	243.2	6.8	238.5	6.3
5	108	328.5	538.7	0.61	0.0513	0.0009	0.2826	0.0084	0.0399	0.0010	252.7	6.7	252.4	6.2
6	13.2	66.4	149.0	0.45	0.0494	0.0016	0.1693	0.0092	0.0248	0.0010	158.8	8.0	158.2	6.6
7	181	227.1	2419.4	0.09	0.0737	0.0013	0.2952	0.0071	0.0291	0.0006	262.7	5.6	184.7	4.1
8	6.7	35.9	74.6	0.48	0.0478	0.0032	0.1475	0.0101	0.0224	0.0007	139.7	8.9	142.7	4.2
9	127	351.6	950.1	0.37	0.0509	0.0009	0.2946	0.0088	0.0420	0.0013	262.2	6.9	264.9	7.9
10	41.6	194.5	418.2	0.47	0.0505	0.0012	0.1780	0.0080	0.0255	0.0010	166.3	6.9	162.6	6.3
11	40.0	225.6	300.8	0.75	0.0490	0.0014	0.1547	0.0054	0.0229	0.0006	146.0	4.7	145.9	3.7
12	49.5	205.2	468.8	0.44	0.0488	0.0010	0.1969	0.0069	0.0292	0.0009	182.5	5.8	185.7	5.3
13	128	590.6	809.2	0.73	0.0531	0.0009	0.2099	0.0071	0.0287	0.0008	193.4	6.0	182.1	5.1
14	5.51	29.5	44.4	0.66	0.0479	0.0029	0.1514	0.0093	0.0230	0.0007	143.1	8.2	146.5	4.4
15	5.33	27.9	43.3	0.64	0.0478	0.0033	0.1559	0.0106	0.0238	0.0008	147.1	9.3	151.6	5.2
16	12.9	65.6	123.5	0.53	0.0479	0.0018	0.1658	0.0070	0.0251	0.0007	155.8	6.1	159.9	4.3
17	16.4	90.1	147.3	0.61	0.0476	0.0018	0.1541	0.0061	0.0235	0.0006	145.5	5.4	149.6	3.5
18	38.1	133.9	420.5	0.32	0.0659	0.0032	0.2132	0.0157	0.0233	0.0007	196.2	13.2	148.2	4.6
19	11.6	56.9	139.3	0.41	0.0483	0.0021	0.1635	0.0088	0.0245	0.0006	153.7	7.7	156.2	4.1
20	5.36	29.6	27.8	1.07	0.0479	0.0041	0.1614	0.0138	0.0245	0.0007	151.9	12.1	156.0	4.7
21	14.0	71.4	116.8	0.61	0.0492	0.0018	0.1727	0.0075	0.0254	0.0007	161.7	6.5	162.0	4.1
22	8.1	43.9	68.7	0.64	0.0491	0.0026	0.1596	0.0084	0.0236	0.0005	150.3	7.4	150.2	3.3
23	22.8	117.5	234.2	0.50	0.0487	0.0016	0.1637	0.0057	0.0244	0.0006	153.9	5.0	155.5	3.6
24	108	318.2	310.0	1.03	0.0509	0.0011	0.3091	0.0083	0.0441	0.0008	273.5	6.5	278.0	5.2
25	17.6	91.8	118.5	0.77	0.0481	0.0018	0.1654	0.0071	0.0249	0.0005	155.4	6.2	158.6	3.4
26	5.28	28.1	27.0	1.04	0.0483	0.0041	0.1656	0.0137	0.0249	0.0007	155.6	12.0	158.7	4.5
27	62	309.6	403.2	0.77	0.0557	0.0015	0.1870	0.0077	0.0243	0.0006	174.1	6.6	154.7	3.5
28	139	310.0	389.8	0.80	0.0541	0.0008	0.4448	0.0083	0.0596	0.0010	373.6	5.9	373.3	5.9
29	65	315.9	663.4	0.48	0.0488	0.0009	0.1761	0.0050	0.0262	0.0007	164.7	4.3	166.4	4.2
30	82.3	17.9	616.7	0.03	0.0728	0.0008	1.5670	0.0314	0.1560	0.0029	957.2	12.6	934.3	16.5
B17028
1	47.6	148.4	201.3	0.74	0.0510	0.0013	0.2852	0.0104	0.0406	0.0012	254.8	8.3	256.5	7.5
2	35.6	193.2	153.3	1.26	0.0503	0.0018	0.1709	0.0077	0.0247	0.0007	160.2	6.7	157.0	4.5
3	51.2	175.7	120.4	1.46	0.0509	0.0014	0.2767	0.0098	0.0395	0.0009	248.0	7.8	249.4	5.7
4	9.6	51.5	59.8	0.86	0.0500	0.0025	0.1641	0.0090	0.0238	0.0005	154.3	7.9	151.5	3.1
5	19.5	107.6	148.6	0.72	0.0481	0.0018	0.1694	0.0088	0.0257	0.0013	158.9	7.7	163.3	8.3
6	9.7	53.3	53.0	1.01	0.0514	0.0033	0.1653	0.0108	0.0233	0.0006	155.3	9.4	148.7	3.7
7	108	236.8	199.7	1.19	0.0828	0.0094	0.5758	0.0747	0.0497	0.0012	461.8	48.2	312.6	7.6
8	49.8	99.8	1115.2	0.09	0.0506	0.0008	0.2782	0.0113	0.0398	0.0014	249.3	9.0	251.8	8.8
9	57	190.0	216.5	0.88	0.0505	0.0011	0.2810	0.0094	0.0403	0.0010	251.5	7.4	254.8	6.2
10	96	487.5	1239.1	0.39	0.0486	0.0009	0.1640	0.0043	0.0245	0.0005	154.2	3.8	155.8	3.3
11	58.5	291.2	741.5	0.39	0.0479	0.0010	0.1614	0.0048	0.0244	0.0006	151.9	4.2	155.5	3.7
12	78	332.1	444.4	0.75	0.0497	0.0011	0.2125	0.0061	0.0310	0.0005	195.7	5.1	196.9	3.3
13	60	95.5	175.0	0.55	0.0565	0.0011	0.6220	0.0168	0.0798	0.0017	491.1	10.6	494.9	10.0
14	23.6	92.9	636.9	0.15	0.0489	0.0010	0.1616	0.0055	0.0239	0.0006	152.1	4.8	152.5	4.0
15	25.2	83.4	88.0	0.95	0.0526	0.0027	0.2893	0.0195	0.0397	0.0010	258.0	15.4	251.1	6.2
16	14.0	74.5	139.4	0.53	0.0491	0.0017	0.1597	0.0064	0.0236	0.0005	150.5	5.6	150.2	3.1
17	5.69	28.8	45.3	0.64	0.0507	0.0028	0.1670	0.0101	0.0239	0.0007	156.8	8.8	152.4	4.3
18	22.3	124.3	172.5	0.72	0.0505	0.0023	0.1646	0.0092	0.0236	0.0009	154.7	8.0	150.6	5.9
19	10.8	57.7	114.3	0.51	0.0494	0.0020	0.1612	0.0070	0.0236	0.0004	151.7	6.2	150.7	2.8
20	42.3	216.1	360.2	0.60	0.0493	0.0015	0.1690	0.0054	0.0248	0.0004	158.5	4.7	158.2	2.4
21	13.0	73.1	67.1	1.09	0.0495	0.0027	0.1583	0.0087	0.0232	0.0005	149.3	7.7	148.1	3.3
22	20.4	97.4	217.6	0.45	0.0496	0.0016	0.1747	0.0057	0.0256	0.0005	163.5	4.9	162.8	3.1
23	10.6	33.1	403.6	0.08	0.0491	0.0012	0.1599	0.0049	0.0236	0.0004	150.6	4.3	150.3	2.4
24	52.4	247.0	1082.3	0.23	0.0493	0.0009	0.1585	0.0038	0.0233	0.0004	149.4	3.4	148.3	2.4
25	9.1	53.7	39.3	1.37	0.0487	0.0037	0.1563	0.0128	0.0232	0.0006	147.4	11.3	148.2	3.8
26	5.62	32.4	39.3	0.83	0.0499	0.0036	0.1595	0.0115	0.0232	0.0005	150.3	10.0	147.7	2.9
27	10.7	22.6	21.0	1.08	0.1745	0.0370	0.7468	0.2179	0.0282	0.0022	566.4	126.7	179.4	13.5
28	10.1	53.8	41.2	1.31	0.0508	0.0029	0.1750	0.0118	0.0249	0.0007	163.7	10.2	158.5	4.2
29	54.8	284.6	694.9	0.41	0.0494	0.0010	0.1623	0.0041	0.0238	0.0004	152.7	3.6	151.8	2.2
30	36.1	174.7	585.5	0.30	0.0500	0.0028	0.1638	0.0116	0.0237	0.0005	154.0	10.1	151.0	3.1
B17030
1	5.8	27.8	32.7	0.85	0.0477	0.0042	0.1667	0.0148	0.0254	0.0009	156.6	12.9	161.6	5.5
2	18.6	84.0	166.0	0.51	0.0527	0.0027	0.1885	0.0123	0.0259	0.0008	175.3	10.5	164.7	4.8
3	104	230.1	584.1	0.39	0.0530	0.0009	0.3183	0.0108	0.0436	0.0013	280.6	8.3	274.9	7.8
4	54.7	159.0	165.3	0.96	0.0513	0.0013	0.3030	0.0124	0.0429	0.0015	268.7	9.7	270.6	9.4
5	76	236.9	194.7	1.22	0.0515	0.0012	0.2911	0.0098	0.0410	0.0011	259.4	7.7	259.2	6.9
6	126	390.2	445.9	0.88	0.0513	0.0010	0.2916	0.0077	0.0412	0.0007	259.8	6.1	260.3	4.3
7	57.6	122.1	280.3	0.44	0.0535	0.0010	0.4071	0.0086	0.0552	0.0009	346.8	6.3	346.5	5.7
8	211	79.4	376.9	0.21	0.0909	0.0012	3.4196	0.0712	0.2730	0.0057	1508.9	16.7	1556.2	28.7
9	136	356.1	964.5	0.37	0.0508	0.0008	0.3070	0.0093	0.0438	0.0012	271.8	7.2	276.3	7.4
10	17.2	75.8	220.8	0.34	0.0489	0.0013	0.1730	0.0062	0.0256	0.0007	162.0	5.3	163.2	4.1
11	27.6	115.4	378.9	0.30	0.0487	0.0011	0.1706	0.0047	0.0254	0.0004	159.9	4.1	161.7	2.8
12	31.6	154.2	244.5	0.63	0.0495	0.0014	0.1667	0.0052	0.0244	0.0005	156.5	4.5	155.6	2.9
13	409	930.7	431.0	2.16	0.0633	0.0036	0.4643	0.0417	0.0526	0.0019	387.2	28.9	330.2	11.7
14	434	338.3	579.6	0.58	0.0697	0.0008	1.4962	0.0371	0.1557	0.0035	928.8	15.2	932.7	19.6
15	30.4	146.7	155.2	0.95	0.0497	0.0016	0.1713	0.0064	0.0250	0.0006	160.5	5.5	159.1	3.5
16	47.5	152.6	66.2	2.30	0.0528	0.0020	0.2959	0.0123	0.0407	0.0011	263.2	9.6	257.4	6.8
17	6.8	29.2	59.6	0.49	0.0487	0.0022	0.1905	0.0124	0.0285	0.0015	177.1	10.6	181.1	9.6
18	5.57	23.8	67.2	0.35	0.0495	0.0029	0.1735	0.0111	0.0255	0.0009	162.5	9.6	162.2	5.5
19	77	218.2	353.4	0.62	0.0518	0.0011	0.2942	0.0089	0.0412	0.0009	261.9	7.0	260.4	5.8
20	8.7	41.7	71.5	0.58	0.0503	0.0032	0.1731	0.0119	0.0250	0.0008	162.1	10.3	159.0	4.8
21	146	513.8	298.4	1.72	0.0623	0.0032	0.3308	0.0228	0.0384	0.0011	290.2	17.4	242.9	6.7
22	77	163.1	324.5	0.50	0.0846	0.0219	0.3081	0.0928	0.0248	0.0011	272.7	72.1	157.9	7.1
23	117	313.3	461.6	0.68	0.0551	0.0020	0.3131	0.0147	0.0412	0.0011	276.6	11.4	260.2	7.0
24	32.5	87.3	198.4	0.44	0.0515	0.0013	0.2970	0.0085	0.0418	0.0007	264.0	6.6	264.0	4.6
25	54.7	154.8	273.2	0.57	0.0519	0.0010	0.2977	0.0077	0.0416	0.0007	264.6	6.1	262.7	4.3
26	146	414.4	533.4	0.78	0.0542	0.0015	0.3105	0.0144	0.0414	0.0009	274.6	11.2	261.6	5.9
27	84	233.9	296.6	0.79	0.0530	0.0010	0.3163	0.0088	0.0433	0.0008	279.1	6.8	273.1	5.0
28	21.2	103.0	153.3	0.67	0.0506	0.0017	0.1724	0.0058	0.0247	0.0003	161.5	5.0	157.3	1.7
29	32.3	93.5	178.7	0.52	0.0518	0.0013	0.2886	0.0096	0.0404	0.0007	257.5	7.6	255.3	4.5
30	42.2	208.1	335.1	0.62	0.0488	0.0013	0.1658	0.0045	0.0246	0.0004	155.7	3.9	156.8	2.5
B17033
1	31.9	174.0	263.2	0.66	0.0487	0.0012	0.1531	0.0054	0.0228	0.0006	144.7	4.8	145.5	3.9
2	49.4	127.9	381.3	0.34	0.0517	0.0009	0.3175	0.0113	0.0445	0.0012	280.0	8.7	280.4	7.6
3	5.77	19.5	45.7	0.43	0.0517	0.0026	0.2490	0.0136	0.0350	0.0011	225.7	11.0	221.7	6.6
4	33.6	85.7	116.0	0.74	0.0522	0.0016	0.3611	0.0149	0.0502	0.0016	313.1	11.1	315.7	9.7
5	17.1	80.3	256.6	0.31	0.0493	0.0015	0.1640	0.0063	0.0241	0.0008	154.2	5.5	153.7	4.9
6	26.9	130.4	160.8	0.81	0.0493	0.0016	0.1807	0.0068	0.0266	0.0006	168.7	5.8	169.3	3.5
7	64	339.2	836.5	0.41	0.0490	0.0009	0.1556	0.0035	0.0230	0.0003	146.9	3.0	146.6	2.1
8	14.7	81.4	132.5	0.61	0.0491	0.0019	0.1506	0.0062	0.0223	0.0004	142.4	5.5	141.9	2.7
9	35.2	208.4	209.1	1.00	0.0493	0.0016	0.1505	0.0065	0.0221	0.0006	142.4	5.7	141.1	3.9
10	23.8	131.5	212.4	0.62	0.0488	0.0016	0.1524	0.0059	0.0227	0.0005	144.0	5.2	144.4	3.2
11	16.4	87.6	129.4	0.68	0.0500	0.0020	0.1577	0.0064	0.0229	0.0005	148.7	5.6	145.9	3.3
12	8.59	8.4	319.4	0.03	0.0512	0.0010	0.2880	0.0076	0.0408	0.0009	257.0	6.0	257.6	5.7
13	13.3	67.6	213.9	0.32	0.0501	0.0016	0.1562	0.0059	0.0226	0.0004	147.4	5.2	144.0	2.2
14	79	221.7	737.5	0.30	0.0513	0.0008	0.2854	0.0107	0.0404	0.0014	255.0	8.4	255.1	8.5
15	14.2	76.2	160.5	0.47	0.0496	0.0016	0.1631	0.0059	0.0239	0.0004	153.5	5.2	152.1	2.5
16	17.6	96.5	160.7	0.60	0.0494	0.0017	0.1556	0.0075	0.0228	0.0006	146.9	6.6	145.4	3.7
17	57.6	173.4	307.0	0.56	0.0520	0.0010	0.2987	0.0075	0.0417	0.0009	265.4	5.9	263.2	5.3
18	15.9	86.6	114.1	0.76	0.0486	0.0019	0.1560	0.0068	0.0233	0.0006	147.2	6.0	148.3	3.5
19	15.1	87.0	118.9	0.73	0.0498	0.0021	0.1544	0.0071	0.0225	0.0005	145.7	6.3	143.4	3.3
20	19.0	91.7	97.5	0.94	0.0508	0.0019	0.1886	0.0079	0.0269	0.0005	175.4	6.7	171.2	3.3
21	106	266.0	760.4	0.35	0.0537	0.0010	0.3308	0.0100	0.0447	0.0009	290.2	7.6	281.7	5.7
22	11.3	62.2	106.2	0.59	0.0486	0.0023	0.1507	0.0075	0.0225	0.0004	142.6	6.6	143.3	2.3
23	18.8	79.2	411.0	0.19	0.0495	0.0013	0.1667	0.0060	0.0244	0.0006	156.6	5.2	155.7	3.9
24	10.0	54.2	93.7	0.58	0.0483	0.0023	0.1513	0.0074	0.0227	0.0005	143.1	6.5	145.0	3.1
25	117	303.9	696.2	0.44	0.0527	0.0008	0.3274	0.0093	0.0450	0.0009	287.6	7.2	283.6	5.6
26	6.6	31.0	80.1	0.39	0.0491	0.0029	0.1599	0.0092	0.0236	0.0005	150.6	8.1	150.7	3.4
27	36.4	90.3	133.5	0.68	0.0558	0.0025	0.3750	0.0144	0.0489	0.0008	323.4	10.7	307.5	4.7
28	1.62	8.7	15.3	0.57	0.0581	0.0058	0.1827	0.0192	0.0229	0.0009	170.4	16.5	145.7	5.9
29	126	563.9	1275.0	0.44	0.0498	0.0007	0.1845	0.0036	0.0268	0.0004	171.9	3.1	170.7	2.5
30	40.2	100.6	122.1	0.82	0.0547	0.0019	0.3767	0.0174	0.0498	0.0010	324.6	12.8	313.4	6.5

Table 4. Sr-Nd isotope compositions of the granitic rocks in the central Great Xing’an Range.

Sample No.	B16022	B16023	B17020-1	B17020-2	B17028-1	B17028-2	B17030-1	B17030-2	B17033-1	B17033-2
Rb (×10⁻⁶)	125.00	58.10	80.27	85.58	24.82	37.67	37.38	43.44	95.42	95.46
Sr (×10⁻⁶)	355.00	324.00	498.84	503.52	157.53	314.84	726.00	724.81	497.94	531.71
⁸⁷Rb/⁸⁶Sr	0.994558	0.506500	0.454507	0.480069	0.445027	0.337957	0.145429	0.169283	0.541266	0.507101
⁸⁷Sr/⁸⁶Sr	0.707051	0.70637	0.706578	0.706583	0.70732	0.706684	0.705589	0.705826	0.706902	0.706735
2σ	1.004706	1.004706	1.004706	1.004706	1.004706	1.004706	1.004706	1.004706	1.004706	1.004706
(⁸⁷Sr/⁸⁶Sr)_i	0.702371	0.703987	0.704439	0.704324	0.705226	0.705094	0.704905	0.705029	0.704355	0.704349
Sm (×10⁻⁶)	3.40	2.61	2.20	2.84	3.73	2.96	3.52	3.37	1.95	2.46
Nd (×10⁻⁶)	18.30	12.60	12.61	15.90	17.45	16.06	20.34	18.72	10.24	12.52
¹⁴⁷Sm/¹⁴⁴Nd	0.116773	0.130192	0.109603	0.112262	0.134311	0.115765	0.108645	0.113179	0.119687	0.123343
¹⁴³Nd/¹⁴⁴Nd	0.512610	0.512600	0.512484	0.512474	0.512500	0.512384	0.512423	0.512444	0.512484	0.512486
2σ	1.002164	1.002164	1.002164	1.002164	1.002164	1.002164	1.002164	1.002164	1.002164	1.002164
εNd (t)	2.8	2.1	0.7	0.4	−0.1	−1.5	−0.5	−0.3	0.2	0.1
f_Sm/Nd	−0.41	−0.34	−0.44	−0.43	−0.32	−0.41	−0.45	−0.42	−0.39	−0.37
t_DM (Ma)	851	1006	977	1018	1250	1194	1056	1072	1082	1122

Table 5. Results of zircon Hf isotope of the granitic rocks in the central Great Xing’an Range.

Sample No.	Age/Ma	¹⁷⁶Yb/¹⁷⁷Hf	2 σ	¹⁷⁶Lu/¹⁷⁷Hf	2 σ	¹⁷⁶Hf/¹⁷⁷Hf	2 σ	εHf(t)	T_DM1/Ma	T_DM2/Ma	f_Lu/Hf
B16022
1	141.40	0.009912	0.000181	0.000332	0.000008	0.282835	0.000017	5.42	576	758	−0.99
2	141.40	0.017712	0.000594	0.000561	0.000012	0.282846	0.000013	5.80	563	737	−0.98
3	141.40	0.014621	0.000085	0.000447	0.000003	0.282841	0.000015	5.65	568	746	−0.99
4	141.40	0.026059	0.000146	0.000777	0.000006	0.282862	0.000017	6.32	545	708	−0.98
5	141.40	0.028240	0.000951	0.000784	0.000023	0.282743	0.000014	2.11	713	943	−0.98
6	141.40	0.014512	0.000099	0.000449	0.000004	0.282840	0.000015	5.59	571	749	−0.99
7	141.40	0.029484	0.000377	0.000867	0.000011	0.282812	0.000015	4.56	617	807	−0.97
8	141.40	0.031101	0.000934	0.000914	0.000021	0.282835	0.000014	5.37	585	761	−0.97
9	141.40	0.034629	0.000913	0.001040	0.000017	0.282867	0.000019	6.48	542	699	−0.97
10	141.40	0.010098	0.000259	0.000372	0.000007	0.283022	0.000013	12.05	314	387	−0.99
B17020
1	154.20	0.030483	0.000186	0.000968	0.000005	0.282811	0.000021	4.78	620	804	−0.97
2	154.20	0.024891	0.000262	0.000785	0.000005	0.282802	0.000019	4.49	629	820	−0.98
3	154.20	0.012874	0.000196	0.000414	0.000005	0.282733	0.000015	2.10	718	954	−0.99
4	154.20	0.046366	0.001423	0.001362	0.000028	0.282872	0.000017	6.89	539	686	−0.96
5	154.20	0.020748	0.001070	0.000681	0.000039	0.282760	0.000019	3.03	686	902	−0.98
6	154.20	0.016042	0.000463	0.000518	0.000018	0.282794	0.000017	4.24	635	834	−0.98
7	154.20	0.021869	0.000218	0.000701	0.000003	0.282774	0.000016	3.52	667	875	−0.98
8	154.20	0.017199	0.000733	0.000490	0.000024	0.282779	0.000017	3.69	657	865	−0.99
9	154.20	0.012904	0.000529	0.000386	0.000012	0.282706	0.000017	1.14	756	1007	−0.99
10	154.20	0.025058	0.001002	0.000767	0.000034	0.282726	0.000015	1.80	736	971	−0.98
B17028
1	152.30	0.064685	0.000821	0.002108	0.000024	0.282783	0.000019	3.65	679	866	−0.94
2	152.30	0.029717	0.000285	0.000971	0.000015	0.282734	0.000017	2.02	729	957	−0.97
3	152.30	0.036370	0.000543	0.001188	0.000011	0.282743	0.000016	2.31	720	940	−0.96
4	152.30	0.024396	0.001084	0.000802	0.000031	0.282720	0.000018	1.57	744	982	−0.98
5	152.30	0.046906	0.000598	0.001362	0.000013	0.282744	0.000015	2.33	722	940	−0.96
6	152.30	0.019468	0.000435	0.000619	0.000011	0.282775	0.000013	3.51	664	874	−0.98
7	152.30	0.013338	0.000342	0.000393	0.000006	0.282747	0.000014	2.55	699	927	−0.99
8	152.30	0.023765	0.000601	0.000778	0.000024	0.282785	0.000017	3.86	652	854	−0.98
9	152.30	0.056754	0.000216	0.001703	0.000015	0.282745	0.000017	2.35	727	938	−0.95
10	152.30	0.025991	0.001086	0.000785	0.000034	0.282872	0.000016	6.93	530	683	−0.98
B17030
1	158.70	0.028383	0.000457	0.000901	0.000020	0.282739	0.000016	2.34	720	944	−0.97
2	158.70	0.023211	0.000346	0.000701	0.000005	0.282811	0.000017	4.90	616	801	−0.98
3	158.70	0.054127	0.001111	0.001731	0.000022	0.282825	0.000018	5.30	612	779	−0.95
4	158.70	0.035954	0.000540	0.001107	0.000010	0.282843	0.000016	6.02	576	739	−0.97
5	158.70	0.019467	0.000771	0.000560	0.000018	0.282816	0.000014	5.09	606	790	−0.98
6	158.70	0.010718	0.000043	0.000333	0.000003	0.282791	0.000013	4.25	637	837	−0.99
7	158.70	0.024310	0.000490	0.000733	0.000010	0.282798	0.000017	4.45	634	827	−0.98
8	158.70	0.018126	0.000218	0.000560	0.000011	0.282776	0.000017	3.69	662	868	−0.98
9	158.70	0.032534	0.000143	0.001027	0.000013	0.282759	0.000013	3.02	695	906	−0.97
10	158.70	0.029346	0.000313	0.000869	0.000008	0.282645	0.000016	−0.97	851	1128	−0.97
B17033
1	144.90	0.031268	0.000209	0.000941	0.000005	0.282768	0.000017	3.06	680	893	−0.97
2	144.90	0.039493	0.001315	0.001139	0.000021	0.282900	0.000014	7.71	496	633	−0.97
3	144.90	0.046260	0.001315	0.001373	0.000027	0.282715	0.000017	1.14	764	1000	−0.96
4	144.90	0.014819	0.000199	0.000459	0.000004	0.282869	0.000013	6.70	530	690	−0.99
5	144.90	0.027794	0.000254	0.000944	0.000011	0.282707	0.000013	0.90	766	1013	−0.97
6	144.90	0.029098	0.001891	0.000829	0.000042	0.282914	0.000016	8.25	472	603	−0.98
7	144.90	0.052766	0.000402	0.001565	0.000007	0.282779	0.000016	3.39	676	874	−0.95
8	144.90	0.019623	0.000384	0.000607	0.000013	0.282873	0.000015	6.81	527	684	−0.98
9	144.90	0.029078	0.000264	0.000926	0.000004	0.282791	0.000021	3.89	647	847	−0.97
10	144.90	0.020030	0.000337	0.000663	0.000005	0.282726	0.000016	1.62	734	973	−0.98

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Qian, C.; Lu, L.; Wang, Y.; Fu, J.; Yang, X.; Zhang, Y.; Ni, S. Petrogenesis of Late Jurassic–Early Cretaceous Granitoids in the Central Great Xing’ an Range, NE China. Minerals 2025, 15, 693. https://doi.org/10.3390/min15070693

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Qian C, Lu L, Wang Y, Fu J, Yang X, Zhang Y, Ni S. Petrogenesis of Late Jurassic–Early Cretaceous Granitoids in the Central Great Xing’ an Range, NE China. Minerals. 2025; 15(7):693. https://doi.org/10.3390/min15070693

Chicago/Turabian Style

Qian, Cheng, Lu Lu, Yan Wang, Junyu Fu, Xiaoping Yang, Yujin Zhang, and Sizhe Ni. 2025. "Petrogenesis of Late Jurassic–Early Cretaceous Granitoids in the Central Great Xing’ an Range, NE China" Minerals 15, no. 7: 693. https://doi.org/10.3390/min15070693

APA Style

Qian, C., Lu, L., Wang, Y., Fu, J., Yang, X., Zhang, Y., & Ni, S. (2025). Petrogenesis of Late Jurassic–Early Cretaceous Granitoids in the Central Great Xing’ an Range, NE China. Minerals, 15(7), 693. https://doi.org/10.3390/min15070693

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Petrogenesis of Late Jurassic–Early Cretaceous Granitoids in the Central Great Xing’ an Range, NE China

Abstract

1. Introduction

2. Geological Background

3. Petrological Analysis of Samples and Analytical Methods

3.1. Petrology

3.2. Major and Trace Element Determinations

3.3. Zircon U-Pb Dating

3.4. Whole-Rock Sr-Nd Isotope Analyses

3.5. Zircon Hf Isotope Analyses

4. Analytical Results

4.1. Major and Trace Elements

4.2. Zircon U-Pb Ages

4.3. Whole-Rock Sr-Nd Isotopes

4.4. Zircon Hf Isotopes

5. Discussion

5.1. Petrogenesis

5.2. The Age of Granitic Rocks in the Gegenmiao and Taonan Area

5.3. Tectonic Setting and Geodynamics Implication

6. Conclusions

Author Contributions

Funding

Data Availability Statement

Conflicts of Interest

References

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