Geochronology and geochemistry of the Neoproterozoic–Mesozoic intrusive rocks in the Xinlin area, northeastern China: new constraints on the tectonic evolution of the Erguna block

Abstract

The occurrence of intrusive rocks within the Xinlin area, northeastern China, provides insights into the Neoproterozoic–Mesozoic geodynamic setting of the Erguna block. In this study, we present petrographic, geochemical, and geochronological data on intrusive rocks from the Xinlin area. Zircon U–Pb and muscovite ⁴⁰Ar/³⁹Ar geochronology reveal that magmatism occurred during the Neoproterozoic (ca. 864.98 Ma), Early Ordovician (ca. 470.0 Ma), Late Carboniferous (ca. 306.9 Ma), Early Permian (ca. 296.9 Ma), and Early Cretaceous (ca. 117.8 Ma) periods. The Neoproterozoic and Early Ordovician intermediate–mafic intrusive rocks have low Rb/Sr contents, high Mg^#, and weakly negative Eu anomalies. These results suggest that the magma sources of these rocks varied: intermediate–acidic magmas were derived from the lower crust, and intermediate–mafic magmas originated from the mantle and were subsequently contaminated by crustal material. In contrast, the Late Carboniferous, Early Permian, Late Triassic–Early Jurassic, and Early Cretaceous intermediate–acidic intrusive rocks display high Rb/Sr contents, low Mg^#, and strongly negative Eu anomalies, indicating derivation from the partial melting of the lower crust. Our findings, along with previous studies, suggest that Neoproterozoic intrusive rocks were formed during the breakup of the Rodinia supercontinent. The Paleozoic intrusive rocks are associated with the collision and amalgamation of the Erguna and Xing’an blocks, as well as the Songnen and Xing’an blocks. Early Mesozoic intrusive rocks were developed during the subduction of the Mongol-Okhotsk oceanic intracontinental system. Finally, the late Mesozoic intrusive rocks were formed in a non-orogenic extensional setting, potentially linked to the final closure of the Mongol-Okhotsk Ocean or the rollback of the Paleo-Pacific Plate.

1 Introduction

The Great Xing’an Range is located within the suture zone between the Siberian and North China cratons (Figure 1A; Liu et al., 2017). This area records evidence of several tectonic events, including the convergence and breakup of the Rodinia supercontinent during the Proterozoic (Zhao, 2017), the closure of the Paleo-Asian Ocean during the late Paleozoic, the closure of the Mongol-Okhotsk Ocean (MOO) in the late Mesozoic, and the subduction of Paleo-Pacific oceanic plate since the Jurassic (Xu et al., 2013). The tectonic setting and geochemical characteristics of the magmatic rocks in this area are notably complex, featuring diverse rock types. Consequently, the region has garnered significant interest from geologists both domestically and internationally (Jia et al., 2011; Liu et al., 2011; Ge et al., 2015; Ouyang et al., 2015; Zheng., 2015).

FIGURE 1

The Xinlin area, located in the Erguna block, is an important gold-mining district (Figure 1B; Liu et al., 2017). The area hosts well-developed intrusive rocks, primarily comprising Neoproterozoic, Paleozoic, and Mesozoic formations (Figure 1C). Extensive research has been conducted on the chronology, geochemistry, and tectonic framework of the magmatic rocks in this area (Wu et al., 2009; Wang et al., 2012; Shi et al., 2013; Feng, 2015; Liu et al., 2016; Tang, 2016; Zhao, 2017; Qian et al., 2018; Liu et al., 2021). However, debates persist regarding the tectonic setting and origin of the Neoproterozoic–Mesozoic intrusive rocks in the Erguna block.

In this study, we present new petrographic, geochemical, and geochronological data on the different types of intrusive rocks within the Xinlin area. We discuss their petrogenesis and reconstruct the tectonic evolution of the region from the Neoproterozoic to the Mesozoic periods.

2 Geological background

The strata exposed in the study area include the Neoproterozoic Xinghuadukou Group; the Lower Cambrian Hongshenggou, Sanyigou, and Jiaobuleshihe formations; the Lower Ordovician Kunasenhe, Huangbanji, and Daxiyikanghe formations; the Lower–Middle Ordovician Tongshan and Duobaoshan formations; the Upper Ordovician Anniangniangqiao and Aihui formations; the Lower Silurian Huanghuagou Formation; the Upper Silurian to Middle Devonian Niqiuhe Formation; and the Lower Cretaceous Longjiang, Guanghua, and Ganhe formations (Figure 1C; HBGMR, 1997).

Intrusive rocks are well-developed in the study area, and they primarily include Neoproterozoic, Paleozoic, and Mesozoic intrusive rocks (Figure 1C). The Neoproterozoic magmatic rocks are mainly distributed in the northern part of Walali, with lithologies predominantly comprising gneiss and schist. The Paleozoic intrusive rocks exposed in the study area are mainly Hercynian and Indosinian in origin. Mesozoic intrusive rocks can be divided into early Yanshanian and late Yanshanian phases. The early Yanshanian intrusive rocks are mainly distributed in the northwest of the study area, with lithologies mainly consisting of monzonitic granite and syenite granite, which are dated to the late Triassic–early Jurassic. The late Yanshanian magmatic rocks are less exposed and show scattered distribution characteristics across the study area, with lithologies primarily comprising granite veins and diorite veins. The majority of the faults within the study area are normal or strike-slip faults, predominantly trending NW–SE and NE–SW, with some trending N–S and E–W. These faults are interpreted to have formed in an extensional setting (Shao and Mu, 1999; Figure 1C).

2.1 Petrology

2.1.1 Neoproterozoic intrusive rocks

The Neoproterozoic intrusive rocks outcrop in the northern part of Walali within the study area. These rocks have undergone regional metamorphism. The dominant lithology is hornblende gneiss (Figure 1C). The hornblende gneisses are gray–black, exhibit a sheet-like, columnar, granular, crystalloblastic structure, and are primarily composed of plagioclase (50 vol.%), quartz (25 vol.%), biotite (20 vol.%), and amphibole (5 vol.%) (Figures 2A, B).

FIGURE 2

2.1.2 Paleozoic intrusive rocks

Paleozoic intrusive rocks primarily include Early Ordovician, Late Carboniferous, and Early Permian intrusive rocks in the study area. The Early Ordovician intrusive rocks mainly outcrop in the Beixili region of the study area. The predominant lithology is gabbro (Figure 1C). The gabbros are gray–black, display a cataclastic structure, and are mainly composed of plagioclase (70 vol.%), pyroxene (15 vol.%), biotite (10 vol.%), and hornblende (5 vol.%) (Figures 2C,D). The Late Carboniferous intrusive rocks outcrop mainly near the Walali gold deposit. The dominant lithologies are monzonitic granite (Figures 2E,F) and potash feldspar granite (Figures 2G,H). The Early Permian intrusive rocks extensively outcrop in the northeastern part of the study area. The lithologies are mainly monzonitic granite and syenogranite.

2.1.3 Early Cretaceous intrusive rocks

Mesozoic intrusive rocks primarily include Late Triassic–Early Jurassic and Early Cretaceous rocks in the study area. The Late Triassic–Early Jurassic intrusive rocks are widely exposed in the northwestern part of the study area. The predominant lithologies are monzonitic granite (Figures 2I,J) and syenogranite. The Early Cretaceous intrusive rocks occur as scattered small exposures resembling “rock trees” across the study area. The dominant lithologies are granite and diorite veins (Figures 2K,L).

3 Sample collection and analytical methods

3.1 Sample collection

Four rock samples were collected for zircon U–Pb geochronology, with rock types including hornblende gneiss (FQ1), gabbro (BQ1), monzonitic granite (DQ1), and diorite (18DN1). One sample was collected for muscovite Ar–Ar geochronology (sample 17XJG-Ar₁). Twenty-seven samples were collected for whole-rock geochemical analyses, with rock types including six hornblende gneisses (samples FQ1, FQ2, FQ4, FQ5, FQ7, and FQ8), five gabbros (samples BQ1, BQ2, BQ3, BQ4, and BQ5), eight monzonitic granites (samples DQ1, DQ2, DQ3, P₆₀GS3, GS1179, GS4075, P₅₄GS1, and P₅₂GS30), three potash feldspar granites (samples WQ15, WQ16, and WQ17), three syenogranites (samples P52GS3, GS4071, and GS 2065), one alkali feldspar granite (sample P₅₀GS9), and one diorite (sample P₆₃GS6).

3.2 Analytical methods

The zircon grains were separated from the crushed samples by using conventional heavy liquid and magnetic techniques, and cathodoluminescence (CL) imaging and zircon U–Pb dating were conducted at the Beijing Createch Testing Technology, Beijing, China. The ICPMSDataCal (version 9.9; Liu et al., 2010) and Isoplot (version 3.0; Ludwig, 2003) programs were used for data reduction. Common Pb was corrected following the method outlined by Andersen (2002). Analytical uncertainties are reported at the 95% (2σ) confidence level.

The muscovite samples were collected from granite closely associated with mineralization. The correction factors used for interfering argon isotopes derived from Ca and K were (³⁹ Ar/ ³⁷ Ar)_Ca = 8.06 × 10⁻⁴, (³⁶ Ar/³⁷ Ar)_Ca = 2.389 × 10⁻⁴, and (⁴⁰ Ar/³⁹ Ar) _K = 5.872 × 10⁻³. ³⁷Ar was corrected for radioactive decay, and the ⁴⁰K decay constant is λ = 5.543 × 10⁻¹⁰a⁻¹ (Steiger and Jager, 1977). The plateau age and the positive and negative isochrones (Ludwig, v2.49) were calculated using the Isoplot program, with the plateau age errors reported at 2 σ. The analytical procedures followed those outlined by Zhang et al. (2006) and Chen et al. (2006).

Major and trace-element analyses were conducted at the Institute of Regional Geology and Mineral Resources, Hebei Province, China. The major elements were analyzed using X-ray fluorescence (XRF), with accuracy better than 5%, and the trace elements were analyzed by inductively coupled plasma–mass spectrometry (ICP–MS), with accuracy better than 10%.

4 Analytical results

4.1 Zircon U–Pb geochronology

Zircons from hornblende gneiss (sample FQ1) are predominantly rounded, with some displaying long columnar shapes (Figure 3A). The U and Th contents of hornblende gneiss (sample FQ1) range from 142.86 to 452.90 ppm and 302.48 to 650.35 ppm, respectively, with Th/U ratios of 0.39–0.72 (n = 17; Table 1), which is consistent with a magmatic origin. Analyses yield ²⁰⁶Pb/²³⁸U ages of 839–883 Ma with a weighted-mean age of 864.9 ± 5.4 Ma (MSWD = 1.02) (Figure 3B).

FIGURE 3

Zircons from gabbro (sample BQ1) are primarily rounded, with some exhibiting columnar shapes (Figure 3C). The U and Th contents of gabbro (sample BQ1) range from 1,020.27 to 10,980.61 ppm and 6,553.42 to 42,051.31 ppm, respectively, with Th/U ratios of 0.13–0.29 (n = 19; Table 1), which is consistent with a magmatic origin. Analyses yield ²⁰⁶Pb/²³⁸U ages of 458–480 Ma with a weighted-mean age of 470.0 ± 2.9 Ma (MSWD = 0.90) (Figure 3D).

Zircons from monzonitic granite (sample DQ1) exhibit well-developed crystals, bright cathodoluminescence, complete growth rings, and pronounced rhythmic zoning (Figure 3E). The U and Th contents range from 42.21 to 572.40 ppm and 92.40 to 521.29 ppm, respectively, with Th/U ratios of 0.86–2.19 (n = 17; Table 1), suggesting a magmatic origin. Analyses yield ²⁰⁶Pb/²³⁸U ages of 304–309 Ma with a weighted-mean age of 306.9 ± 1.9 Ma (MSWD = 0.14) (Figure 3F).

Zircons of diorite (sample 18DN1) are well-crystallized with flattened shapes (Figure 3G). The U and Th contents range from 205.55 to 885.81 ppm and 257.12 to 788.38 ppm, respectively, with Th/U ratios of 0.74–1.28 (n = 10; Table 1), indicative of a magmatic origin. Analyses yield ²⁰⁶Pb/²³⁸U ages of 113–124 Ma with a weighted-mean age of 117.8 ± 3.1 Ma (MSWD = 2.0) (Figure 3H).

4.2 Muscovite ⁴⁰Ar/³⁹Ar dating

The Ar–Ar dating results of muscovite are presented in Table 2. The corresponding plateau age, isochron age (Figure 4A), and inverse isochron age are illustrated in Figure 4B. The muscovite sample yielded an ⁴⁰Ar/³⁹Ar plateau age of 296.9 ± 1.7 Ma (nine-step age-heating spectrum from 850°C to 1,300°C, and 87.9% of ³⁹Ar released), a corresponding isochron age of 300.3 ± 1.7 Ma (950°C–1,200°C, N = 8, MSWD = 3.2), and an inverse isochron age of 299.9 ± 1.7 Ma (950°C–1,200°C, N = 8, MSWD = 3.7). These data indicate that the plateau age (296.9 ± 1.7 Ma) represents the reliable crystallization age of the muscovite.

FIGURE 4

4.3 Geochemistry

The Neoproterozoic hornblende gneisses belong to the calc-alkaline series and exhibit high total alkali contents (Table 3). The samples mainly plot within the monzonite field on the TAS diagram (Figure 5A). In the K₂O–SiO₂ diagram, they fall within the high-K calc-alkaline series and are peraluminous (Figure 5C). The Neoproterozoic hornblende gneisses yielded Eu/Eu* values of 0.62–0.82 and (La/Yb)_N values ranging from 5.30 to 30.62. Rare earth element (REE) fractionation is minimal. The chondrite-normalized REE diagram (Figure 6A) indicates a slight enrichment of light rare earth elements (LREEs) with a subtle positive trend. The primitive-mantle-normalized trace-element spider diagram (Figure 6B) shows enrichment in large-ion lithophile elements (LILEs; e.g., Rb, Ba, Th, U, La, Nd, and Ce) and depletion in high-field-strength elements (HFSEs; e.g., Ta, P, and Nb; Table 3).

FIGURE 5

Frost et al. (2001), respectively.

FIGURE 6

Boynton (1984) and Sun and McDonough (1989), respectively.

The Early Ordovician gabbro rocks are characterized by low Si and high Mg contents (Table 3). These samples primarily plot near the gabbro field on the TAS diagram (Figure 5A). They exhibit Eu/Eu* values ranging from 0.85 to 2.16 and (La/Yb)_N values of 1.10–3.94, with significant REE fractionation. The chondrite-normalized REE diagram (Figure 6C) shows enrichment in LREEs, exhibiting a positive trend. The primitive-mantle-normalized trace-element spider diagram (Figure 6D) indicates enrichment in LILEs (e.g., Rb, Sr, and Ba) and depletion in HFSEs (e.g., Zr, Hf, and P; Table 3).

The Late Carboniferous, Early Permian, Late Triassic–Early Jurassic, and Early Cretaceous intrusive rocks belong to the calc-alkaline series, with high total alkali contents (Table 3). These samples fall in the field of high-K calc-alkaline series on the K₂O–SiO₂ diagram (Figure 5B) and are peraluminous (Figure 5C). The Eu/Eu* values range from 0.36 to 1.30, and (La/Yb)_N values are between 1.3 and 41.54, with significant REE fractionation. The chondrite-normalized REE diagram (Figure 6E) shows enrichment in LREEs, exhibiting a positive trend. The primitive-mantle-normalized trace-element spider diagram (Figure 6F) reveals enrichment in LILEs (e.g., Rb, Th, U, K, and Nd) and depletion in HFSEs (e.g., Ta, P, Eu, Ti, and Nb; Table 3).

5 Discussion

5.1 Neoproterozoic–Mesozoic magmatism in the Xinlin area

Previous geochronological studies reported a wide range of ages for the intrusive rocks of the Erguna block (Table 4). At least ∼929 Ma, ∼887 Ma, ∼850 Ma, ∼819 Ma, ∼792 Ma, ∼764 Ma, and ∼738 Ma magmatic events occurred in the Neoproterozoic Era on the Erguna block (Guo et al., 2016; Zhao et al., 2016; Yang et al., 2017). The Paleozoic magmatic activity in the Erguna block can be divided into the Early and Late Paleozoic activities. The Early Paleozoic magmatic activity can be mainly divided into four stages: ∼500 Ma (Middle-Late Cambrian: 504–500 Ma), ∼480 Ma (Early Ordovician: 485–475 Ma), ∼460 Ma (Middle-Late Ordovician: 465–454 Ma), and ∼440 Ma (Early Silurian: 439–434 Ma) (Zhao, 2017; Wu et al., 2005); the Late Paleozoic magmatic activity occurred from 330 to 241 Ma (Ju et al., 2005; Wang et al., 2012; Feng et al., 2014). The early Late Paleozoic granitic magmatism occurred between 405 and 325 Ma, which can be further refined into three stages: Early Middle Devonian (Stage I, 405 to 380 Ma), Late Devonian–Early Carboniferous (Stage II, 365 to 350 Ma), and Late Early Carboniferous (Stage III, 335 to 325 Ma) (Qian et al., 2018). The Mesozoic magmatism in the Erguna block can be divided into seven stages: ∼246 Ma, ∼225 Ma, ∼205 Ma, ∼185 Ma, ∼155 Ma, ∼137 Ma, and ∼125 Ma (Wang et al., 2012; Tang, 2016).

To obtain a more comprehensive understanding of granitic magmatism in the northern Great Xing’an Range, we selected 66 zircon U–Pb results and combined them with the five new ages of this study. Based on this combined geochronological dataset, three stages of granitic magmatism can be identified, namely, Neoproterozoic, Paleozoic, and Mesozoic granites (Table 4). Neoproterozoic granitoids, which are rarely developed in the Erguna block, comprise hornblende gneisses and mica quartz schists, with isotopic ages ranging from 915 to 791 Ma (Table 4). Paleozoic intrusive rocks are widely distributed in the Erguna block, with ages ranging from 504 to 241 Ma. Mesozoic granitoids are widely exposed in the northern Great Xing’an Range, primarily near the Xinlin–Xiguitu suture, with ages spanning 240 to 116 Ma.

5.2 Petrogenesis

The origin and source of the magmas that formed the intrusive rocks in the Erguna block are varied and have been the focus of numerous studies (Gao et al., 2013; Hu et al., 2014; Liu et al., 2016; Wang et al., 2016; Zhao, 2017; Yang et al., 2017; Lu et al., 2020). However, debates persist regarding the petrogenesis of the Neoproterozoic–Mesozoic intrusive rocks in the Erguna block.

5.2.1 Petrogenesis of Neoproterozoic intrusive rocks

The information regarding the genesis of Neoproterozoic intrusive rocks in the Erguna block is relatively consistent, which is related to the convergence and breakup of the Rodinia supercontinent (Zhao, 2017; Lu, 2019). The approximately 887 Ma granites are similar to post-collisional granites (Liu et al., 2011; Zhao et al., 2016), whereas the 850–737 Ma granitoids are generally similar to A-type granites, and the magmas could have originated not only from the partial melting of a depleted lower crust that accreted during the Meso-Neoproterozoic, with a contribution of ancient crustal materials in their petrogenesis, but also from the partial melting of the residual ancient mafic crustal material (Tang et al., 2013; Zhao et al., 2016).

The Neoproterozoic Xinghuadukou rock group hornblende gneisses in the study area exhibit high Mg^# values (average 50.25), which rules out the possibility that they were derived from partial melting of the lower crust. The hornblende gneisses show Nb contents ranging from 8.20 to 21.70 ppm, higher than those of N-MORB (typically 2–3 ppm; Sun and McDonough, 1989). The TiO₂ contents of hornblende gneisses range from 0.57% to 0.62%, lower than those of OIB (≈2.68%; Ewart et al., 1998). The hornblende gneisses are also characterized by relatively high V, Sr, Ni, Co, and Cr contents and low Si content, suggesting a mantle-derived origin.

5.2.2 Petrogenesis of Early Paleozoic intrusive rocks

The Early Paleozoic intermediate–acidic rocks in the Erguna block mainly originated from the partial melting of the newly accreted lower crust, with the participation of some residual ancient crustal materials; the primitive magma of the basic rocks mainly originated from the partial melting of the depleted lithospheric mantle that was metasomatized by subducting fluids (Zhao, 2017). The collision granite magma on the northern edge of the Erguna block originated from the mantle during the Early Paleozoic and was involved in the crustal material (Wu et al., 2005; Lu et al., 2022).

The Early Paleozoic intrusive rocks in the Xinlin area are predominantly the Early Ordovician gabbros, exhibiting high Mg^# values (average 59.75), which rules out the partial melting of the lower crust as their source. The gabbros have Nb contents of 1.40 to 6.90 ppm (average 4.64 ppm), which is higher than those of N-MORB (generally 2–3 ppm; Sun and McDonough, 1989). The TiO₂ contents of the gabbros are between 1.33% and 6.77% (average 4.64%), which is higher than those of OIB (≈2.68%; Ewart et al., 1998). Additionally, these gabbros yielded an average Rb/Sr value of 0.015, which is close to the primitive mantle value (0.03; Sun and McDonough, 1989). They also exhibit low Si and high Sr (334–835 ppm), Ni (26–101 ppm), Co (39.2–77.2 ppm), and Cr (20–130 ppm) contents, further supporting their origin from the mantle.

5.2.3 Petrogenesis of the intermediate–acidic intrusive rocks

In the Triassic to Early Jurassic period, the primitive magma of basic intrusive rocks originated from the partial melting of the depleted lithospheric mantle, and intermediate–acidic intrusive rocks originated from the partial melting of the newly accreted lower crust and were mixed with a small amount of ancient continental crust material (Tang et al., 2014; Tang, 2016). The Early Jurassic granitic magmas formed from the partial melting of the felsic crust (Wang et al., 2016; Tang, 2016) or crust–mantle mixing (Dai et al., 2013); the Late Jurassic granitic magmas formed as a result of the dismantling/melting of the thickened lower crust in a collisional orogenic belt (Wu et al., 2008) or from crust–mantle interaction (Dai et al., 2013; Hu et al., 2014; Tang, 2016); and the Early Cretaceous granitic magmas were derived from the partial melting of crustal material (Wu et al., 2008; Gao et al., 2013; Shi et al., 2013; Niu et al., 2016), where the lithospheric mantle was metasomatized by subduction-related fluids, forming the parent magmas to the diorites. This process may have involved the partial melting of the subducted plate and metasomatism of the lithospheric mantle by sediment-derived fluids (Liu et al., 2016; Chai et al., 2018).

The Late Carboniferous, Early Permian, Late Triassic–Early Jurassic, and Early Cretaceous intrusive rocks in the study area are predominantly intermediate–acidic, peraluminous, and a part of the high-K calc-alkaline series; the major elements show high SiO₂ content and low Fe₂O_3T and Mg^# values (average 24.12), and the trace elements are enriched in LREEs, such as Rb, Th, U, K, Nd, Zr, and Hf, and relatively depleted in HREEs, such as Ba, Nb, Sr, P, Eu, and Ti. The negative Eu anomalies of the intermediate–acidic intrusive rocks indicate that the plagioclases likely originate from the residual phases (Lightfoot et al., 1987). The intermediate–acidic intrusive rocks yield an average Rb/Sr value of 2.62, which is close to the crustal ratio (0.15) but higher than that of the primitive mantle (0.03), E-MORB (0.033), and OIB (0.047) (Sun and McDonough, 1989), and these geochemical features suggest that they were derived from the partial melting of the lower crust.

5.3 Tectonic setting

5.3.1 Neoproterozoic tectonic setting

The Neoproterozoic magmatism of the Erguna block provides key insights into the convergence and breakup of the Rodinia supercontinent, a significant global geological event, and several magmatic events related to the Rodinia supercontinent breakup have been reported in the Erguna block (Wu et al., 2011; Sun et al., 2012; Tang et al., 2013; Feng, 2015). Magmatisms between 927 Ma and 880 Ma were the result of collision-orogeny during the stage of assembly of the Rodinia supercontinent, whereas the 850–737 Ma magmatisms record the breakup of the Rodinia supercontinent (Zhao, 2017). The study area is located near the Xinlin–Xiguitu suture, and the Neoproterozoic hornblende gneisses of the study area belong to A-type granite, suggesting emplacement in an extensional setting (Figure 5). These gneisses also exhibit characteristics of volcanic-arc granites (Figure 7), indicating their association with the breakup of the Rodinia supercontinent.

FIGURE 7

5.3.2 Paleozoic tectonic setting

For the Paleozoic era, various tectonic settings have been proposed for the Erguna block. Early Paleozoic igneous rocks in the Erguna block were formed in a post-collision extensional environment, likely linked to the collision and amalgamation of the Erguna and the Xing’an blocks (Feng, 2015; Zhao, 2017). Late Paleozoic granitic magmatism is associated with the collision and assembly of the Erguna–Xing’an and Songnen blocks, transitioning from an orogenic to an extensional environment (Wu et al., 2005; Qian et al., 2018). The collision and assembly between the Erguna block and the Xing’an block were completed in the Early Paleozoic era (Ge et al., 2005), forming collisional accretionary terranes that were accreted during the Late Pan-African global event (Zhou et al., 2011).

The Early Ordovician gabbros show characteristics similar to those of volcanic-arc granites (Figure 7), supporting their connection to the collision and merging of the Erguna and Xing’an blocks. Late Carboniferous–Early Permian intrusive rocks include both A-type and I-type granites, suggesting their emplacement during a transition from orogenic to extensional tectonic settings (Figure 5). These rocks display the characteristics of volcanic-arc and collisional granites (Figure 7), suggesting their emplacement in an orogenic setting. Tectonic activity in the study area during this period was primarily controlled by the collision and amalgamation of the Erguna and Xing’an blocks, followed by the Songnen and Xing’an blocks, which resulted in the generation of a large amount of intermediate–acidic magmas.

5.3.3 Mesozoic tectonic setting

The Late Permian–Early Jurassic intrusive rocks on the Erguna block were formed in the subduction environment of the MOO plate; the Late Permian–Early Middle Triassic intrusive rocks were formed in the active continental margin environment; the Late Middle Triassic–Early Late Triassic intrusive rocks were formed in a local extensional setting; the Late Triassic–Early Jurassic intrusive rocks were formed in the active continental margin environment; and the Early Jurassic igneous rocks were formed in the active continental margin environment; the Late Jurassic magmatic activity took place in a lithospheric extensional environment caused by the collapse and subsidence of the thickened continental crust after the closure of the Mongolian Okhotsk Ocean (Tang, 2016). The magmatic activity in the Middle Triassic may be related to the extensional environment after the closure of the ancient Asian Ocean; the Early Middle Jurassic magmatic events may be related to the subduction of the MOO (Wang et al., 2012). The Late Triassic intrusive rocks are related to the subduction of the MOO (Liu et al., 2021). The MOO underwent subduction, collision, and post-collision processes during the Early Jurassic to Early Cretaceous, with its closure in the northern part of the Great Xing’an Range likely occurring between the Late Jurassic and Early Cretaceous (Liu et al., 2021). The Early Cretaceous granites were formed in an extensional tectonic setting (Wu et al. ,2009; Shi et al., 2013; Liu et al., 2016) and were related to the final closure of the MOO (Shi et al., 2013; Liu et al., 2016) or the rollback of the Paleo-Pacific Plate (Gao et al., 2013). The geochronological data and tectonic interpretations suggest that the Early Cretaceous intrusive rocks within the study area were formed during non-orogenic extension and were related to the final closure of the MOO or the rollback of the Paleo-Pacific Plate. These intrusive rocks within the study area are distributed in an NE–SW orientation, parallel to the continental margin, and their age decreases from west to east. The intrusive rocks within the Xinlin area yielded a mean age of 125 Ma, which is consistent with the timing of the final closure of the MOO or of the rollback of the Paleo-Pacific Plate. In the discrimination diagram for A-type granites in Figures 5D–F, all the Late Triassic–Early Cretaceous intrusive samples plot within the A-type granite field, suggesting that they formed in an extensional setting.

6 Conclusion

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