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Article

Late Paleozoic Tectonic Evolution of the Northern Great Xing’an Range, Northeast China: Constraints from Carboniferous Magmatic Rocks in the Wunuer Area

by
Liyang Li
1,2,
Chuanheng Zhang
1 and
Zhiqiang Feng
3,*
1
School of Earth and Resources, China University of Geosciences, Beijing 100083, China
2
Langfang Comprehensive Survey Center of Natural Resources, China Geology Survey, Langfang 065000, China
3
Department of Earth Science and Engineering, Taiyuan University of Technology, Taiyuan 030024, China
*
Author to whom correspondence should be addressed.
Minerals 2023, 13(8), 1090; https://doi.org/10.3390/min13081090
Submission received: 23 June 2023 / Revised: 31 July 2023 / Accepted: 11 August 2023 / Published: 15 August 2023
(This article belongs to the Special Issue Geochronology, Geochemistry and Petrogenesis of Magmatic Rocks)
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Abstract

:
Northeast China composes the main part of the Central Asian Orogenic Belt. Traditionally, Northeast China has been considered a collage of several microcontinental blocks. However, the tectonic evolution of these blocks remains uncertain. Igneous rocks can be used to infer the magmatic histories of the blocks and thus help reconstruct their evolution. In this study, we present new zircon U–Pb and whole-rock geochemical data for Carboniferous igneous rocks from the Wunuer area, northern Great Xing’an Range, Northeast China, to constrain the Carboniferous amalgamation of the united Xing’an–Erguna and Songnen–Zhangguangcai Range massifs. On the basis of zircon U–Pb dating results, we identify two main stages of magmatism, i.e., early Carboniferous (332–329 Ma) and late Carboniferous (312–310 Ma). The early Carboniferous igneous rocks include diorites and granodiorites, with the former being classified as calc-alkaline to tholeiitic and the latter as tholeiitic. Both rock types are enriched in Th and U and depleted in Nb and Ti. The rocks display slightly fractionated rare earth element (REE) patterns, with an enrichment in light REEs and a depletion in heavy (H)REEs. The geochemical characteristics of the early Carboniferous rocks indicate that they formed in a subduction-related continental-arc setting. The late Carboniferous igneous rocks include monzogranites and syenogranites, both of which are classified as high-K calc-alkaline rocks and show enrichment in Th, U, and Rb and depletion in Nb and Ti. The rocks display strongly fractionated REE patterns, with an enrichment in light REEs and a depletion in HREEs. The geochemical characteristics of the late Carboniferous rocks indicate that they formed in a syn-collisional tectonic setting. Combining the new geochronological and geochemical results and inferred tectonic settings with regional magmatic data, we propose a new three-stage model to interpret the late Paleozoic tectonic evolution of the united Xing’an–Erguna and Songnen–Zhangguangcai Range massifs of Northeast China: (1) early Carboniferous (360–340 Ma) subduction of the Paleo-Asian oceanic plate beneath the united Xing’an–Erguna Massif and formation of the Wunuer oceanic basin in the Yakeshi area; (2) early to late Carboniferous (340–310 Ma) sustained subduction of the Paleo-Asian oceanic plate beneath the united Xing’an–Erguna Massif and initiation of subduction of the Wunuer oceanic basin; and (3) late Carboniferous–early Permian (310–275 Ma) syn-collisional to post-collisional tectonic transition between the united Xing’an–Erguna Massif and the Songnen–Zhangguangcai Range Massif.

Graphical Abstract

1. Introduction

The Central Asian Orogenic Belt (CAOB) is one of the largest Phanerozoic accretionary orogens in the world (Figure 1). This belt is bounded by the Siberian Craton to the north and the Tarim and North China cratons to the south and extends from the Ural Mountains in the west through Kazakhstan, Tien Shan, the Altai Mountains, and Mongolia to the Pacific Ocean in the east [1,2,3,4,5,6,7,8,9,10,11,12,13,14,15]. This huge orogenic belt developed as a result of multiple accretionary and collisional events during the closure of the Paleo-Asian Ocean [16,17,18,19,20]. As a prime example of Paleozoic continental crust and modification, the tectonic evolution of the CAOB has been intensely studied [4,17,21,22,23].
Northeast China is located in the eastern CAOB. Traditionally, Northeast China has been considered a collage of several microcontinental blocks from southeast to northeast; i.e., the Jiamusi, Songnen, Xing’an, and Erguna blocks, which are separated by the Mudanjiang fault, the Hegenshan suture zone, and the Xinlin–Xiguitu suture zone, respectively [6,24,25,26,27,28,29,30,31,32,33,34,35,36,37,38,39,40] (Figure 2). Advances in research methods and the development of high-precision geological dating techniques have allowed the attributes of the Precambrian basement of the Erguna and Jiamusi blocks to be established and the Xing’an and Songnen blocks to be recognized as accretionary terranes that formed via subduction and collision [7,8,41,42].
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Figure 1. Tectonic sketch map showing the main units of central and eastern Asia (modified after [31,32]).
Figure 1. Tectonic sketch map showing the main units of central and eastern Asia (modified after [31,32]).
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Uncertainty remains regarding the subduction of paleo-oceanic plates in Northeast China and how and when the amalgamation between the abovementioned blocks/microcontinents took place, especially in regard to the evolution of the Xinlin–Xiguitu suture zone. This suture zone contains the Xinlin ophiolites, Tayuan metagabbros, Jifeng ophiolites, and Yimin blueschists [43,44,45,46,47,48,49,50,51]. Geochronological data for these units include a K–Ar phlogopite age for the Xinlin ophiolite of 539 Ma [43], a U–Pb zircon age for the Gaxian pyroxenite of 628.4 ± 9.7 Ma [52], a U–Pb zircon age for meta-gabbro from the Huanerku area of 696.8 ± 2.9 Ma [51], a U–Pb zircon age for gabbro from the Jifeng area of 647 ± 5 Ma, and a U–Pb zircon age of greenschist from the Toudaoqiao area of 511 ± 2 Ma. Early Paleozoic post-orogenic A-type granites reported from the Tahe area are regarded as a product of the closure of the Xinlin–Xiguitu suture zone caused by the collision of the Erguna and Xing’an blocks [24]. The Wunuer ophiolitic mélange occurs in the southwest of the Xinlin–Xiguitu suture zone. This ophiolitic mélange comprises gabbro, diabase, metabasalt, and radiolarian bedded chert with serpentinized amphibole–pyroxene peridotites. Zircon U–Pb dating of the gabbro and diabase has yielded ages of 341 ± 6 and 346 ± 6 Ma, respectively, which suggest that the ophiolite formed during the early Carboniferous. The ophiolite is classified as SSZ type according to geochemical characteristics and may be a late product of a mature back-arc basin tectonic setting [53]. The Xinlin–Xiguitu oceanic basin is generally considered to have closed during the late Cambrian [5,6,7,8,24,33,41,50,54]. However, the recent discovery of the early Carboniferous Wunuer ophiolite suggests that the Xinlin–Xiguitu oceanic basin may have closed later than previously thought and that the late Paleozoic tectonic evolution of Northeast China needs to be reassessed.
In this study, we present zircon U–Pb and whole-rock geochemical data for Carboniferous igneous rocks from the Wunuer area, northern Great Xing’an Range, Northeast China, to reconstruct the tectonic evolution of this area during the late Paleozoic, including the opening (by subduction initiation) and closure (by collision) of the Wunuer Ocean. The integration of the new results with previous data allows us to reconstruct the late Paleozoic tectonic evolution of Northeast China.
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Figure 2. Tectonic division of the central-northern Great Xing’an Range (modified after [50]). Date from [33,43,50,51,52,53].
Figure 2. Tectonic division of the central-northern Great Xing’an Range (modified after [50]). Date from [33,43,50,51,52,53].
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2. Geological Setting and Sample Descriptions

The study area is in the vicinity of Wunuer town, Yakeshi City, in the northern Great Xing’an Range of Inner Mongolia. Tectonically, the study area is located in the Xinlin–Xiguitu suture zone (Figure 2). Ordovician outcrops in the area are composed mainly of the Duobaoshan and Luohe formations. The Duobaoshan Formation comprises a set of intermediate–felsic volcanic rocks with island-arc characteristics [54,55], whereas the Luohe Formation is a set of clastic rocks that formed in an active-continental-margin setting [56,57]. Silurian strata are absent from the study area. Exposed Devonian strata are mainly the Niqiuhe and Daminshan formations, with the former comprising a set of continental-margin clastic rocks [58] and the latter a set of intermediate–felsic volcanic rocks with island-arc characteristics [59]. A large number of late Paleozoic intrusive rocks occur in the study area, including diorite, granodiorite, monzogranite, and syenogranite [60,61], which are emplaced into Ordovician or Devonian strata and overlain by Mesozoic volcanic rocks and Quaternary cover (Figure 3).
Intrusive rocks in the Wunuer area include diorite, granodiorite, monzogranite, and syenogranite. A diorite pluton is located ~15 km to the southwest of Wunuer town. The pluton forms an approximately ellipsoidal body with an exposed area of 25 km2 and intrudes the Devonian Niqiuhe Formation (Figure 3). The diorite is gray to gray-green and has a fine-grained texture (Figure 4a). The rock consists of plagioclase (~55 vol.%), hornblende (~20 vol.%), quartz (~10 vol.%), biotite (~7 vol.%), and K-feldspar (~5 vol.%), with accessory minerals (~3 vol.%) including magnetite, zircon, and apatite.
A granodiorite pluton is located ~16 km to the southwest of Wunuer town. The pluton is an approximately ellipsoidal body with an exposed area of 15 km2 and intrudes the abovementioned diorite pluton (Figure 3). The granodiorite is light gray to gray-green and has a fine-grained texture (Figure 4b). The rock consists of plagioclase (~45 vol.%), quartz (~20 vol.%), K-feldspar (~15 vol.%), hornblende (~15 vol.%), and biotite (~5 vol.%).
The monzogranite pluton is located ~12 km SE of Wunuer town and is an approximately ellipsoidal body with an exposed area of 20 km2 (Figure 3). The monzogranite is light pink in color and has a coarse-grained texture (Figure 4c). The rock consists of plagioclase (~40 vol.%), quartz (~25 vol.%), K-feldspar (~30 vol.%), and biotite (~5 vol.%).
The syenogranite pluton is located ~18 km SW of Wunuer town. The pluton is an approximately ellipsoidal body with an exposed area of 32 km2 (Figure 3). The syenogranite is pink in color and has a coarse-grained texture (Figure 4d). The rock consists of quartz (~25 vol.%), K-feldspar (~60 vol.%), and plagioclase (~15 vol.%).

3. Analytical Methods

One sample for zircon geochronological analysis (U–Pb2071001) and eight samples for geochemical analysis were collected from the diorite pluton. One sample for zircon geochronological analysis (U–Pb2071003) and four samples for geochemical analysis were obtained from the granodiorite pluton. One sample for zircon geochronological analysis (U–Pb2072001) and two samples for geochemical analysis were collected from the monzogranite pluton. One sample for zircon geochronological analysis (U–Pb2071005) and seven samples for geochemical analysis were obtained from the syenogranite pluton.

3.1. Zircon U–Pb Dating

Zircons were separated from samples using conventional heavy liquid and magnetic techniques. Zircon grains were then randomly handpicked in alcohol under a binocular microscope, mounted in epoxy along with zircon standards, and polished to expose grain centers for cathodoluminescence (CL) imaging and U–Pb analysis. CL images were obtained at Beijing Geoanalysis Co., Ltd., Beijing, China. U–Pb analysis was performed by laser-ablation–inductively coupled plasma–mass spectrometry (LA-ICP-MS) at Beijing Createch Testing Technology Co., Ltd., Beijing, China. The analytical instruments used for the dating were a ThermoFisher Neptune multi-receiver ICP-MS instrument and an SIUP193FXArF LA system. The operating conditions during analyses included a laser denudation spot diameter of 35 μm, a laser energy density of 10–13 J/cm2, and a frequency of 8–10 Hz. Age data were plotted using Isoplot [62].

3.2. Major and Trace Elements

Whole-rock geochemical analyses were performed at the Analytical Laboratory of Beijing Research Institute of Uranium Geology, Beijing, China. Major elements (SiO2, FeO, TiO2, Al2O3, Fe2O3, MgO, MnO, CaO, Na2O, K2O, and P2O5) were analyzed using an AxiosmAX X-ray fluorescence spectrometer, with an analytical precision of approximately ±5%. Trace elements and rare earth elements (REEs) were analyzed using a NexION300D ICP-MS instrument, with an accuracy better than 10%.

4. Results

4.1. Zircon U–Pb Ages

4.1.1. Early Carboniferous Intrusive Rocks

Most zircon grains from the sampled diorite are subhedral, display oscillatory zoning in CL images (Figure 5a), and have Th/U ratios of 0.62–1.40, indicating a magmatic origin. Analyses of zircons from sample U–Pb2071001 yielded 206Pb/238U ages of 347–310 Ma, with a weighted mean age of 329.7 ± 5.0 Ma (MSWD = 2.3, N = 18; Table S1 and Figure 6a), which is interpreted as the crystallization age of the zircons. The emplacement age of the diorite pluton is therefore inferred to be early Carboniferous.
Zircons from the sampled granodiorite are predominantly dark and subhedral, and some display oscillatory zoning in CL images (Figure 5b). The Th/U ratios of the zircons range from 1.04 to 2.68, consistent with a magmatic origin. Analyses of zircons from sample U–Pb2071003 yielded 206Pb/238U ages of 350–322 Ma, with a weighted mean age of 332.6 ± 6.9 Ma (MSWD = 3.1, N = 11; Table S1 and Figure 6b), which is interpreted as the crystallization age of the zircons. The emplacement age of the granodiorite pluton is therefore inferred to be early Carboniferous.

4.1.2. Late Carboniferous Intrusive Rocks

Most zircon grains from the sampled monzogranite are subhedral and display oscillatory zoning in CL images (Figure 5c) with Th/U ratios of 0.63–1.24, indicating a magmatic origin. Analyses of zircons from sample U–Pb2072001 yielded 206Pb/238U ages of 321–308 Ma, with a weighted mean age of 310.8 ± 4.7 Ma (MSWD = 0.26, N = 10; Table S1 and Figure 6c), which is interpreted as the crystallization age of the zircons. The emplacement age of the monzogranite pluton is therefore inferred to be late Carboniferous.
Zircons from the sampled syenogranite are predominantly subhedral, display oscillatory zoning in CL images (Figure 5d), and have Th/U ratios of 0.63–1.19, indicating a magmatic origin. Analyses of zircons from sample U–Pb2071005 yielded 206Pb/238U ages of 331–293 Ma, with a weighted mean age of 312.1 ± 9.4 Ma (MSWD = 4.2, N = 8; Table S1 and Figure 6d), which is interpreted as the crystallization age of the zircons. The emplacement age of the syenogranite pluton is therefore inferred to be late Carboniferous.

4.2. Geochemistry

4.2.1. Major Element Compositions

The sampled diorites have low SiO2 contents (52.59–57.85 wt.%) and contain Al2O3 (15.87–17.11 wt.%), Na2O + K2O (3.492–5.31 wt.%), TiO2 (0.556–1.02 wt.%), Fe2O3T (7.54–9.73 wt.%), MgO (0.125–0.18 wt.%), CaO (5.82–8.68 wt.%), and MnO (3.54–5.96 wt.%) (Table 1). These samples are classified mainly as gabbro diorites in a total-alkali–silica (TAS) diagram (Figure 7a), are metaluminous with A/CNK values of 0.75–0.95 (Table 1 and Figure 7b), and are classified as calc-alkaline to tholeiitic in a K2O vs. SiO2 diagram (Figure 7c).
The sampled granodiorites have low SiO2 contents (62–64.74 wt.%) and contain Al2O3 (12.23–13.77 wt.%), Na2O + K2O (3.11–3.88 wt.%), TiO2 (0.30–0.31 wt.%), Fe2O3T (5.93–6.59 wt.%), MgO (0.10–0.12 wt.%), CaO (5.13–6.37 wt.%), and MnO (4.65–5.31 wt.%) (Table 1). These samples are classified mostly as granodiorites in a TAS diagram (Figure 7a), are metaluminous with A/CNK values of 0.78–0.87 (Table 1 and Figure 7b), and are classified as tholeiitic in a K2O vs. SiO2 diagram (Figure 7c).
The sampled monzogranites have high SiO2 contents (71.07–74.64 wt.%) and contain Al2O3 (13.3–14.21 wt.%), Na2O + K2O (8.36–8.9 wt.%), TiO2 (0.282–0.381 wt.%), Fe2O3T (1.36–3.17 wt.%), MgO (0.036–0.044 wt.%), CaO (0.259–0.332 wt.%), and MnO (0.323–0.618 wt.%) (Table 1). These samples are classified as granites in a TAS diagram (Figure 7a), are peraluminous with A/CNK values of 1.14–1.16 (Table 1 and Figure 7b), and are classified as high-K calc-alkaline in a K2O vs. SiO2 diagram (Figure 7c).
The sampled syenogranites have high SiO2 contents (71.68–78.5 wt.%) and contain Al2O3 (11.65–15.57 wt.%), Na2O + K2O (7.62–9.18 wt.%), TiO2 (0.16–0.24 wt.%), Fe2O3T (0.7–1.48 wt.%), MgO (0.02–0.05 wt.%), CaO (0.42–1.39 wt.%), and MnO (0.14–0.528 wt.%) (Table 1). These samples are classified as granites in a TAS diagram (Figure 7a), are peraluminous with A/CNK values of 1.03–1.12 (Table 1 and Figure 7b), and are classified as high-K calc-alkaline in a K2O vs. SiO2 diagram (Figure 7c).

4.2.2. Trace Element Compositions

The sampled diorites are relatively enriched in Th and U and depleted in some high-field-strength elements (HFSEs; e.g., Nb and Ti). The rocks display slightly fractionated REE patterns between light REEs (LREEs) and heavy REEs (HREEs) (LREE/HREE = 2.93–4.42, (La/Yb)N = 1.7–3.63), with LREE enrichment, HREE depletion, and slight or no negative Eu anomalies (Eu/Eu* = 0.84–0.99) (Table 1 and Figure 8a,b).
The sampled granodiorites are relatively enriched in Th and U and depleted in some HFSEs (e.g., Nb and Ti). The rocks display lightly fractionated REE patterns (LREE/HREE = 4.64–4.98, (La/Yb)N = 3.78–4.28), with LREE enrichment, HREE depletion, and negative Eu anomalies (Eu/Eu* = 0.61–0.69) (Table 1 and Figure 8c,d).
The sampled monzogranites are enriched in Th, U, and large-ion lithophile elements (LILEs; e.g., Rb) and depleted in some HFSEs (e.g., Nb and Ti). The rocks display strongly fractionated REE patterns (LREE/HREE = 13.09–22.34, (La/Yb)N = 14.04–28.77), with LREE enrichment, HREE depletion, and negative Eu anomalies (Eu/Eu* = 0.39–0.44) (Table 1 and Figure 8e,f).
The sampled syenogranites are enriched in Th, U, and LILEs (e.g., Rb and K) and depleted in some HFSEs (e.g., Nb and Ti). The rocks display strongly fractionated REE patterns (LREE/HREE = 11.36–14.03, (La/Yb)N = 12.18–23.22), with LREE enrichment, HREE depletion, and negative Eu anomalies (Eu/Eu* = 0.36–1.04) (Table 1 and Figure 8g,h).

5. Discussion

5.1. Carboniferous Intrusive Rocks in the Great Xing’an Range

According to our geochronological analyses, the studied diorite and granodiorite were emplaced during the early Carboniferous, and the syenogranite and monzogranite were emplaced during the late Carboniferous. There are widespread occurrences of coeval magmatic rocks in the Great Xing’an Range. Most of the early Carboniferous intrusive rocks are distributed in a strip along the Xinlin–Xiguitu and Hegenshan suture zones (Figure 9). The late Carboniferous intrusive rocks have a wider distribution, occurring mainly in the Yakeshi, Duobaoshan, Zhalantun, Heihe, and Wudalianchi areas.

5.2. Petrogenesis of Carboniferous Intrusive Rocks in the Northern Great Xing’an Range

5.2.1. Petrogenesis of the Wunuer Early Carboniferous Igneous Rocks

Early Carboniferous igneous rocks in the Wunuer area comprise diorite and granodiorite. These rocks contain hornblende and biotite but no primary muscovite. The mineral assemblages are consistent with those of I-type granites [74,75,76,77,78,79]. A/CNK values (0.75–0.95) classify the diorites and granodiorites as metaluminous rocks. The rocks are characterized by relatively high Al2O3, Fe, Mg, and Sr and low Si and K contents, the enrichment in LILEs and LREEs, and the depletion in HREEs. The granodiorites plot in the I-type and S-type granite fields in the Nb–(10,000 Ga/Al), Ce–(10,000 Ga/Al), and Y–(10,000 Ga/Al) diagrams (Figure 10a–c) and mainly in the I-type granite field in an ACF diagram (Figure 10d).
The average value of Rb/Sr for the diorite and granodiorite is 0.04, which is close to the primitive mantle (0.03), E-MORB (0.033), and OIB (0.047) [80], but lower than the crustal ratio (0.15). These geochemical characteristics suggest that the diorite and granodiorite are sourced from partial malting of the mantle.
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Figure 10. (a) Nb versus 10,000 Ga/Al diagram (after [81]), (b) Ce versus 10,000 Ga/Al diagram (after [81]), (c) Y versus 10,000 Ga/Al diagram (after [81]), (d) ACF diagram (after [82]).
Figure 10. (a) Nb versus 10,000 Ga/Al diagram (after [81]), (b) Ce versus 10,000 Ga/Al diagram (after [81]), (c) Y versus 10,000 Ga/Al diagram (after [81]), (d) ACF diagram (after [82]).
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5.2.2. Petrogenesis of the Wunuer Late Carboniferous Igneous Rocks

Late Carboniferous igneous rocks in the Wunuer area comprise monzogranite and syenogranite. These rocks are composed predominantly of quartz, K-feldspar, and plagioclase. A/CNK values (1.03–1.16) classify the monzogranites and syenogranites as peraluminous rocks. The rocks are characterized by relatively high SiO2 and K2O and low P2O5 contents, the enrichment in Rb, Th, and U, and the depletion in Ba, Nb, Ta, Sr, P, and Ti. These characteristics are consistent with those of S-type granites. The monzogranites and syenogranites plot in the I-type and S-type granite fields in Nb—(10,000 Ga/Al), Ce—(10,000 Ga/Al), and Y—(10,000 Ga/Al) diagrams (Figure 10a–c) and mostly in the S-type granite field in an ACF diagram (Figure 10d).
The average value of Rb/Sr for the monzogranite and syenogranite is 2.53, which is close to the crustal ratio (0.15) but higher than the primitive mantle (0.03), E-MORB (0.033), and OIB (0.047) [80]. These geochemical characteristics suggest that the monzogranite and syenogranite are sourced from partial melting of the crust.

5.3. Inferred Tectonic Settings

The geochemical characteristics of the diorites and granodiorites (Section 4.2) are consistent with formation in a subduction-related continental-arc setting, and those of the monzogranites and syenogranites suggest formation in a syn-collisional tectonic setting. The granodiorites plot in the volcanic arc fields in Rb–(Y + Nb) and Rb–(Yb + Ta) diagrams (Figure 11a,b) and mostly in the volcanic arc fields in Rb/10–Hf–3Ta and Rb/30–Hf–3Ta diagrams (Figure 11c,d). The syenogranites and monzogranites fall predominantly in the syn-collisional fields in Rb–(Y + Nb) and Rb–(Yb + Ta) diagrams (Figure 11a,b) and in the syn-collisional fields in Rb/10–Hf–3Ta and Rb/30–Hf–3Ta diagrams (Figure 11c,d).

5.4. Tectonic Implications

The integrated results of this study, combined with regional geological data, allow a new model to be proposed for the late Paleozoic tectonic evolution of the northern Great Xing’an Range (Figure 12), as follows. During the early Carboniferous (360–340 Ma), subduction of the Paleo-Asian oceanic plate beneath the united Xing’an–Erguna Massif occurred, with the associated development of a back-arc ocean basin (the Wunuer oceanic basin). The early Carboniferous igneous rocks (360–340 Ma) display markedly different rock associations and geochemical characteristics from east to west across the Xing’an block. Igneous rocks in the east of the Xing’an block (the Heihe, Nenjiang, Zhalantun, and Moguqi areas) are composed of gabbro, gabbro diorite, monzogranite, and syenogranite and are classified as calc-alkaline, consistent with formation in a subduction-related setting [41,85,86,87,88]. In contrast, ophiolites and gabbros in the west of the Xing’an block (the Wunuer area) are consistent with a back-arc ocean basin setting, for example, the age of the Wunuer ophiolitic mélange is 341~346 Ma; the Wunuer ophiolitic mélange is classified as SSZ type according to geochemical characteristics and may be a late product of a mature back-arc basin tectonic setting [53]. We suggest that early Carboniferous igneous rocks formed as a result of northwest-directed subduction of the Paleo-Asian oceanic plate, which was initiated during the late Devonian [66,89]. The continuous subduction of the Paleo-Asian oceanic slab generated a magmatic arc encompassing the Heihe, Nenjiang, Zhalantun, and Mogiqi areas, as well as the Wunuer back-arc oceanic basin in the Wunuer area [53,60,66,90,91,92].
During the early–late Carboniferous (340–310 Ma), sustained subduction of the Paleo-Asian oceanic plate and subduction of the Wunuer oceanic basin occurred. Igneous rocks in the east of the Xing’an block (the Longzhen and Yaergenchu areas) are composed of granodiorite and monzogranite, which are classified as calc-alkaline series, implying formation in a subduction-related setting [93,94]. The diorite, granodiorite, monzogranite, and syenogranite in the west of the Xing’an block (Tahe, Taerqi, and Wunuer areas) formed in a subduction-related setting, indicating that the Wunuer oceanic basin had entered the subduction phase [28,52,95,96].
The late Carboniferous–early Permian (310–275 Ma) was characterized by a syn-collisional to post-collisional tectonic setting between the united Xing’an–Erguna Massif and the Songnen–Zhangguangcai Range Massif. The widely distributed late early Carboniferous–early Permian igneous rocks in the northern Great Xing’an Range are composed mostly of syenogranite and monzogranite and signify a syn-collisional setting [61,67,96]. The occurrence of early Permian alkaline rocks implies a subsequent extensional tectonic environment in a post-collisional setting [52,67]. Therefore, we suggest that the late Carboniferous–early Permian igneous rocks formed in a syn-collisional to post-collisional transitional setting in the Wunuer and Taerqi areas [52,67,96] and in the Heihe, Duobaoshan, Nenjiang, and Zhalantun areas [28,67,68,97], implying that both the Wunuer Ocean and Paleo-Asian Ocean had closed.

6. Conclusions

We generated new zircon U–Pb and whole-rock geochemical data for Carboniferous igneous rocks from the Wunuer area, northern Great Xing’an Range, to reconstruct the late Paleozoic tectonic evolution of this area and, in combination with regional geological and geochronological data, to establish an integrated tectonic history of Northeast China. The main conclusions of this study are as follows:
(1) Intrusive rocks in the Wunuer area include diorite, granodiorite, monzogranite, and syenogranite. The zircon U–Pb mean ages of the diorite and granodiorite are 329.7 ± 5.0 and 332.6 ± 6.9 Ma, respectively, indicating early Carboniferous emplacement of these rocks. The zircon U–Pb mean ages of the monzogranite and syenogranite are 310.8 ± 4.7 and 312.1 ± 9.4 Ma, respectively, indicating late Carboniferous emplacement.
(2) The geochemical signatures of the Wunuer rocks indicate that the diorite and granodiorite formed in a subduction-related continental-arc setting and that the syenogranite and monzogranite formed in a syn-collisional tectonic setting.
(3) A new three-stage model for the late Paleozoic tectonic evolution of Northeast China is proposed: (1) early Carboniferous (360–340 Ma) subduction of the Paleo-Asian oceanic plate beneath the united Xing’an–Erguna Massif and formation of the Wunuer oceanic basin in the Yakeshi area; (2) early Carboniferous–late Carboniferous (340–310 Ma) subduction of the Paleo-Asian oceanic plate beneath the united Xing’an–Erguna Massif and initiation of subduction of the Wunuer oceanic basin; and (3) late Carboniferous–early Permian (310–275 Ma) syn-collisional to post-collisional tectonic transition between the united Xing’an–Erguna and Songnen–Zhangguangcai Range massifs.

Supplementary Materials

The following supporting information can be downloaded froom: https://www.mdpi.com/article/10.3390/min13081090/s1, Table S1: LA-ICP-MS U-Pb-Th data for zircons for the Carboniferous intrusive rocks in Wunuer area.

Author Contributions

Conceptualization, L.L. and Z.F.; methodology, L.L.; software, L.L.; validation, L.L., C.Z. and Z.F.; formal analysis, L.L.; investigation, L.L., C.Z. and Z.F.; resources, L.L. and Z.F.; data curation, L.L.; writing—original draft preparation, L.L.; writing—review and editing, L.L., C.Z. and Z.F.; visualization, L.L.; supervision, L.L., C.Z. and Z.F.; project administration, L.L. and Z.F.; funding acquisition, L.L. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the China Geological Survey Project (DD20230251, DD2016007808) and supported by the National Natural Science Foundation of China (Grant No. 42272251, 42072230 and 41602235) and National Science Foundation for Post-doctoral Scientists of China (Grant No. 2019M661060).

Data Availability Statement

The original contributions presented in the study are included in the article/Supplementary Materials.

Acknowledgments

We thank Yueqiang Qin, and Xin Feng of Langfang Comprehensive Survey Center of Natural Resources for his helpful discussions during research process. Special thanks are due to the reviewers and editors of this journal for their valuable suggestions and revisions of the manuscript.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 3. Geological map of Wunuer area with sample locations (simplified and modified after the 1:50,000 geological map).
Figure 3. Geological map of Wunuer area with sample locations (simplified and modified after the 1:50,000 geological map).
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Figure 4. Representative photomicrographs of the Carboniferous intrusive rocks in Wunuer area. (a) Diorite (+), (b) granodiorite (+), (c) monzogranite (+), (d) syenogranite (+). Hbl = Hornblende, Bt = biotite, Pl = plagioclase, Kfs = K-feldspar, Qz = quartz.
Figure 4. Representative photomicrographs of the Carboniferous intrusive rocks in Wunuer area. (a) Diorite (+), (b) granodiorite (+), (c) monzogranite (+), (d) syenogranite (+). Hbl = Hornblende, Bt = biotite, Pl = plagioclase, Kfs = K-feldspar, Qz = quartz.
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Minerals 13 01090 g005
Figure 5. Representative cathodoluminescence (CL) images of zircons from the Carboniferous intrusive rocks in Wunuer area showing their 206Pb/238U ages. (a) Diorite, (b) granodiorite, (c) monzogranite, (d) syenogranite.
Figure 5. Representative cathodoluminescence (CL) images of zircons from the Carboniferous intrusive rocks in Wunuer area showing their 206Pb/238U ages. (a) Diorite, (b) granodiorite, (c) monzogranite, (d) syenogranite.
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Figure 6. Zircon LA-ICP-MS U-Pb concordant diagrams for zircons from the Carboniferous intrusive rocks in Wunuer area. (a) Diorite, (b) granodiorite, (c) monzogranite, (d) syenogranite.
Figure 6. Zircon LA-ICP-MS U-Pb concordant diagrams for zircons from the Carboniferous intrusive rocks in Wunuer area. (a) Diorite, (b) granodiorite, (c) monzogranite, (d) syenogranite.
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Figure 7. (a) SiO2 versus (Na2O+K2O) (after [63]), (b) A/CNK(Al2O3/(CaO+Na2O+K2O)) versus A/NK(Al2O3/(Na2O+K2O)) diagram (after [64]) and (c) SiO2 versus K2O diagrams (after [65]).
Figure 7. (a) SiO2 versus (Na2O+K2O) (after [63]), (b) A/CNK(Al2O3/(CaO+Na2O+K2O)) versus A/NK(Al2O3/(Na2O+K2O)) diagram (after [64]) and (c) SiO2 versus K2O diagrams (after [65]).
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Figure 8. Primitive-mantle-normalized trace element spidergrams (a,c,e,g) and Chondrite-normalized REE patterns (b,d,f,h).
Figure 8. Primitive-mantle-normalized trace element spidergrams (a,c,e,g) and Chondrite-normalized REE patterns (b,d,f,h).
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Figure 9. Distribution of the Carboniferous intrusive rocks in northern Great Xing’an Range, Northeast China. Date from [28,52,60,66,67,68,69,70,71,72,73].
Figure 9. Distribution of the Carboniferous intrusive rocks in northern Great Xing’an Range, Northeast China. Date from [28,52,60,66,67,68,69,70,71,72,73].
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Figure 11. (a) Rb versus Y+Nb diagram (after [83]), (b) Rb versus Yb+Ta diagram (after [83]), (c) Rb/10-Hf-3Ta diagram (after [84]), (d) Rb/30-Hf-3Ta diagram (after [84]). VAG = volcanic arc granites, WPG = within plate granites, COLG = collisional granites, and ORG = oceanic ridge granites.
Figure 11. (a) Rb versus Y+Nb diagram (after [83]), (b) Rb versus Yb+Ta diagram (after [83]), (c) Rb/10-Hf-3Ta diagram (after [84]), (d) Rb/30-Hf-3Ta diagram (after [84]). VAG = volcanic arc granites, WPG = within plate granites, COLG = collisional granites, and ORG = oceanic ridge granites.
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Minerals 13 01090 g012
Figure 12. Cartoon diagram showing tectonic evolution during late Devonian to early Permian (ca. 360–275 Ma) of the northern Great Xing’an Range, Northeast China. XEM = the united Xing’an–Erguna Massif; SZM = the Songnen–Zhangguangcai Range Massif.
Figure 12. Cartoon diagram showing tectonic evolution during late Devonian to early Permian (ca. 360–275 Ma) of the northern Great Xing’an Range, Northeast China. XEM = the united Xing’an–Erguna Massif; SZM = the Songnen–Zhangguangcai Range Massif.
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Table 1. Major and trace elements of the Carboniferous intrusive rocks in Wunuer area.
Table 1. Major and trace elements of the Carboniferous intrusive rocks in Wunuer area.
RocksDioriteGranodioriteMonzograniteSyenogranite
Sample001002003004005006007008009010011012013014015016017018019020021
Major oxides (wt%)
SiO256.0154.4157.8555.6852.5954.4955.7157.2262.0064.7464.5764.3571.0774.6476.9775.1078.5072.6071.6872.1576.97
TiO20.780.940.770.900.881.020.820.560.310.300.300.310.380.280.160.210.180.240.240.220.17
Al2O316.3516.4317.1116.0016.2816.5816.4115.8713.7712.8612.8112.2314.2113.3012.4113.3311.6514.6815.2815.5712.51
TFe2O37.769.128.238.889.579.738.637.546.535.936.196.593.171.560.820.910.701.481.430.980.72
MgO0.180.160.130.150.160.140.150.130.120.110.100.120.040.040.050.040.020.040.030.020.04
MnO5.135.123.544.695.964.394.444.265.184.655.025.310.620.320.140.250.180.530.530.370.15
CaO7.846.406.585.827.447.787.538.686.375.295.135.750.330.260.430.650.421.001.391.090.42
Na2O3.643.933.383.913.693.693.842.543.123.082.992.923.953.393.633.913.224.424.483.863.52
K2O0.771.380.410.780.830.660.580.950.760.480.460.194.954.974.674.834.403.753.825.324.66
P2O50.140.130.140.150.130.110.150.070.060.060.060.060.070.040.020.040.030.110.100.080.03
LOI1.381.941.832.992.421.381.712.141.762.402.302.151.201.110.610.640.611.071.010.230.73
Total99.4899.4499.5499.4599.3599.4899.5699.5699.5299.4399.4699.4799.9099.8599.9199.9199.9199.9299.9999.9099.91
A/NK2.402.062.852.202.342.452.363.052.312.302.362.441.201.211.121.141.161.301.331.281.15
A/CNK0.780.840.950.900.790.790.800.760.790.850.870.791.141.161.051.041.081.121.091.111.08
Trace elements (ppm)
Rb11.1027.406.7812.1018.408.737.3613.4015.509.826.662.66285.00320.00184.00193.00164.00117.00118.00155.00189.00
Ba144.00192.00158.00200.00113.00115.00107.00145.00177.00147.00157.0082.60546.00346.00179.00179.00141.00428.00553.00870.00164.00
Th1.881.490.941.731.871.431.212.572.503.373.003.6119.6029.8018.4019.8016.709.4011.607.9018.60
U0.370.420.380.300.490.490.300.500.420.780.660.892.492.682.372.111.720.101.070.622.04
Ta0.330.260.150.220.210.450.350.230.150.180.160.191.261.401.091.160.101.301.280.971.23
Nb4.183.082.032.502.546.155.082.512.102.322.052.4911.5012.9011.7012.6011.107.837.395.2313.60
La13.309.067.758.718.9410.5010.609.379.279.858.4910.4031.2022.9029.2035.9029.7018.1022.6014.4039.40
Ce33.7021.7020.0019.3022.3029.6031.2022.3020.6020.8018.6022.3086.0060.3055.5065.4056.2039.1047.3029.4070.60
Sr307.00351.00351.00288.00290.00310.00327.00314.00273.00144.00170.00214.00130.0090.8045.5047.9041.80449.00468.00460.0044.50
Nd18.9014.3013.9012.2014.8021.1025.0013.809.719.408.6310.7023.7016.6017.2020.4017.2016.4019.3012.0021.70
Zr48.3047.5017.3031.9036.1016.8014.4020.7025.7046.1036.1065.9055.2069.1031.2036.9030.6020.8022.0017.5034.90
Hf2.132.071.011.711.781.070.851.281.331.881.612.282.633.102.102.382.040.991.120.862.42
Sm4.373.783.833.123.685.226.653.232.122.021.832.273.533.082.903.422.903.143.512.133.66
Y26.8024.9026.4019.8020.5038.2045.1018.9015.5014.4013.4016.307.3411.2015.6017.0013.709.098.835.8616.90
Yb2.632.422.662.072.023.664.471.991.761.651.561.880.781.171.721.751.320.700.700.481.79
Lu0.410.370.410.310.300.590.690.310.280.260.240.310.190.180.280.270.220.100.100.070.29
La13.309.067.758.718.9410.5010.609.378.499.279.8510.4031.222.9029.2035.9029.7018.1022.6014.4039.40
Ce33.7021.7020.0019.3022.3029.6031.2022.3018.6020.6020.8022.3086.0060.3055.5065.4056.2039.1047.3029.4070.60
Pr4.292.972.792.623.124.505.063.062.152.372.352.606.764.715.206.145.304.265.243.216.56
Nd18.9014.3013.9012.2014.8021.1025.0013.808.639.719.4010.7023.7016.6017.2020.4017.2016.4019.3012.0021.70
Sm4.373.783.833.123.685.226.653.231.832.122.022.273.533.082.903.422.903.143.512.133.66
Eu1.471.251.241.101.201.511.971.000.410.510.470.480.430.430.390.430.360.630.750.700.44
Gd4.924.384.413.664.025.677.073.552.132.402.262.563.022.832.923.512.932.713.001.913.78
Tb0.750.700.730.600.620.911.170.550.330.370.350.400.310.380.400.470.380.350.370.230.49
Dy4.424.244.483.513.605.476.993.202.042.332.172.511.391.962.192.511.991.721.651.092.58
Ho0.930.900.970.750.751.171.470.670.460.530.490.550.250.390.460.520.400.300.290.190.53
Er2.762.672.842.212.233.564.432.031.481.691.591.800.801.161.511.631.250.810.820.541.68
Tm0.400.370.410.310.310.540.660.290.220.260.240.270.110.170.240.250.180.110.110.070.25
Yb2.632.422.662.072.023.664.471.991.561.761.651.880.781.171.721.751.320.700.700.481.79
Lu0.410.370.410.310.300.590.690.310.240.280.260.310.130.180.280.290.220.100.100.070.29
Y26.8024.9026.4019.8020.5038.2045.1018.9013.4015.5014.4016.307.3411.2015.6017.0013.709.098.835.8616.90
ΣREE93.2569.1166.4160.4767.8994.00107.4365.3453.9048.5854.2059.03158.41116.27120.11142.62120.3388.44105.73766.422153.75
LREE/HREE4.423.312.933.513.903.362.994.194.984.744.644.7422.3413.0911.3612.0512.8812.0014.0313.5112.50
δEu0.970.940.920.990.950.840.870.900.660.630.690.610.390.440.410.380.370.650.691.040.36
δCe1.091.021.050.981.031.061.041.021.031.041.051.021.391.351.020.991.011.051.031.020.98
LaN/YbN3.632.692.093.023.172.061.703.384.283.903.783.9728.7714.0412.1814.7216.1518.6023.2221.6115.80
LaN/SmN2.181.721.452.001.741.441.142.083.333.143.503.296.345.347.237.537.354.144.624.857.73
GdN/YbN1.551.501.371.461.651.281.311.481.131.131.131.133.212.001.401.661.843.213.563.311.75
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Li, L.; Zhang, C.; Feng, Z. Late Paleozoic Tectonic Evolution of the Northern Great Xing’an Range, Northeast China: Constraints from Carboniferous Magmatic Rocks in the Wunuer Area. Minerals 2023, 13, 1090. https://doi.org/10.3390/min13081090

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Li L, Zhang C, Feng Z. Late Paleozoic Tectonic Evolution of the Northern Great Xing’an Range, Northeast China: Constraints from Carboniferous Magmatic Rocks in the Wunuer Area. Minerals. 2023; 13(8):1090. https://doi.org/10.3390/min13081090

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Li, Liyang, Chuanheng Zhang, and Zhiqiang Feng. 2023. "Late Paleozoic Tectonic Evolution of the Northern Great Xing’an Range, Northeast China: Constraints from Carboniferous Magmatic Rocks in the Wunuer Area" Minerals 13, no. 8: 1090. https://doi.org/10.3390/min13081090

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