Geochronology, geochemistry, and geological significance of early Jurassic intrusive rocks in the Lesser Xing’an- Zhangguangcai Range, northeast China

Abstract

The Lesser Xing’an—Zhangguangcai Range of northeast China is located in the eastern segment of the Central Asian Orogenic Belt (CAOB), which records intense magmatism during the Mesozoic. The petrogenesis and geodynamic setting of the Early Jurassic intrusive rocks in this region are unclear. In this paper, we present new zircon U–Pb age and whole-rock geochemical data for these intrusive rocks to investigate their origins and tectonic setting. Zircon U–Pb dating suggests these intrusive rocks were emplaced during the Early Jurassic (197–187 Ma). The granites are enriched in silica and alkali, and depleted in MgO and CaO. They are metaluminous to weakly peraluminous, and have high A/CNK values and low zircon saturation temperatures (T_Zr ~ 779°C), suggesting they are highly fractionated I-type granites derived by partial melting of lower crustal materials. The granites exhibit negative Nb, Ta, P, Eu, and Ti anomalies due to fractional crystallization. The diorites and gabbros have low SiO₂ contents and high Mg^# values, and are enriched in light rare earth and large-ion lithophile (Ba, K, and Sr) elements, and depleted in heavy rare earth and high field strength (Nb, Ta, and Ti) elements. The geochemical characteristics show that the mafic magmas were derived by partial melting of mantle that had been metasomatized by subduction-related fluids. Based on the geochemical characteristics of coeval intrusive rocks and the regional geological setting, we suggest the Early Jurassic intrusive rocks in the Lesser Xing’an—Zhangguangcai Range were formed along an active continental margin, possibly as a result of bidirectional subduction of the Mudanjiang Oceanic plate between the Jiamusi and Songnen—Zhangguangcai Range massifs.

Introduction

The Lesser Xing’an—Zhangguangcai Range in northeast (NE) China is located between the Jiamusi and Songnen massifs, and contains abundant Late Paleozoic to Mesozoic igneous rocks. It is a complex geological area that has experienced numerous tectonomagmatic events. Previous studies have reported extensive geochronological and geochemical data for plutons in this area, but the origin and tectonic setting of the igneous rocks are debated [1–3]. Some studies consider that delamination occurred beneath the Central Asian Orogenic Belt (CAOB), which led to the magma upwelling [4–6]; Whereas others have proposed that the igneous rocks were generated in a back-arc extensional setting associated with subduction of the Paleo-Pacific Plate [7–9]. Some recent studies have suggested that the igneous rocks are arc-related igneous rocks that formed during subduction in the Mudanjiang Ocean [10–14], which was located between the Jiamusi and Songnen massifs. Based on the arc-related intrusive rocks and active continental margin igneous rocks, subduction in the Mudanjiang Ocean is inferred to have begun the early Permian (>274 Ma) [12], Late Triassic [15, 16], or Early Jurassic [17]. The arc-related igneous rocks indicate the subduction polarity was bidirectional [12, 18] or westward [11.16].

Numerous igneous rocks occur in the Lesser Xing’an—Zhangguangcai Range, mainly granites and sparse intermediate—mafic intrusive rocks [14]. Therefore, previous studies of the intrusive rocks have focused mainly on the granites and their formation ages and petrogenesis. The granites were intruded during the Late Paleozoic and Mesozoic, particularly in the Late Triassic to Early Jurassic [10–12, 19–24]. Other studies have reviewed the spatiotemporal distribution of Late Paleozoic—Mesozoic granites in the Lesser Xing’an—Zhangguangcai Range, and noted that the granites exhibit a westward younging trend [25, 26]. The granites are mainly I- and A-type granites, and there are almost no S-type granite [10–12, 19–30]. Ge et al.(2020b) suggested the granitic magmas were derived by partial melting of Meso—Neoproterozoic crustal material [26]. Other studies have proposed that the granites were generated by partial melting of juvenile crust [19, 21, 24]. The granites might also were formed by the mixing of mantle- and crust-derived magmas [23].

Given that granites can form in a range of tectonic settings, studies of granite cannot uniquely constrain the tectonic evolution of the Lesser Xing’an—Zhangguangcai Range. Mafic igneous rocks are equally important for constraining the tectonic setting and magma sources. The most recent studies indicates the mafic rocks formed in the Early Jurassic [9, 25, 31]. Zircon Hf isotopes and geochemistry of igneous rocks indicate the mafic magmas were derived by partial melting of depleted mantle that had been metasomatized by subduction-derived fluids [9, 25, 31]. Therefore, we investigated the Early Jurassic intrusive rocks in the Shuguang Forest Farm area in the Lesser Xing’an—Zhangguangcai Range. We used petrographic, geochemical, and zircon U–Pb age data to determine the petrogenesis and tectonic setting of the intrusive rocks, which provide new insights into the tectonic evolution of the Lesser Xing’an—Zhangguangcai Range.

Geological background

NE China is located between the North China Plate and the Siberian Plate, in the easternmost CAOB (Fig 1a [32]). It formed by complex tectonic and magmatic processes involving micro-continental plates, including the Ergun, Xing’an, Songliao, and Jiamusi massifs, and Nadanhada Terrane (from west to east) [14, 27, 32–35] (Fig 1b [14]). The study area is located in the Lesser Xing’an—Zhangguangcai Range, near the suture zone between the Jiamusi and Songnen—Zhangguangcai Range massifs, with the Jiamusi and Jiayin—Mudanjiang massifs to the east and Songnen Massif to the west.

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(a) Regional map showing the location of Central Asian Orogenic Belt; (b) Tectonic divisions sketch map of NE China; (c) Distribution of magmatic rocks in the Lesser Xing’an-Zhangguangcai Range. The original basemap was obtained from Natural Earth (http://www.naturalearthdata.com/) and was further processed using software ArcGIS 10.8 version. Digital elevation model was from the USGS National Map Viewer (http://viewer.nationalmap.gov/viewer/).

The strata in the study area comprise the Lower Permian—Lower Triassic Hongguang Formation of the Zhangguangcai Range Group and Cenozoic—Quaternary rocks. The Hongguang Formation is distributed in a NE–SW to nearly N–S direction, and was intruded by Early Jurassic syenogranites, monzogranites, and granodiorites. The Hongguang Formation consists mainly of gray—black migmatites and intermediate—acidic volcanic rocks intercalated with marbles. The Quaternary strata are mostly distributed in linear bands along terraces and valleys on both sides of major rivers, and consist of clay and unconsolidated gravel.

The geological setting of the study area is complex and includes Late Archean—Mesoproterozoic continental breakup, Late Proterozoic—Early Paleozoic oceanic basin formation, Early Paleozoic convergence of the North China and Siberian plates (and other microplates) [36, 37], Late Paleozoic subduction and closure of the Paleo-Asian Ocean, collision of the southern margin of the Siberian Plate and northern margin of the North China Plate [38, 39], and westward subduction of the Pacific Plate and evolution of the Mongol—Okhotsk tectonic domain [19, 20, 40]. The study area contains abundant igneous rocks in a N–S-trending and sporadic upper Paleozoic strata [41] (Fig 1c [10, 14]). These igneous rocks are diverse and include acid, intermediate, and (ultra)mafic rocks, with granites being particularly common.

Petrography

Early Jurassic intrusive rocks are widely distributed in the study area. Acid intrusive rocks are common and intermediate—mafic intrusive rocks are sporadically exposed, including syenogranite, monzogranite, diorite, and gabbro (Fig 2). To constrain the tectonic evolution of the Lesser Xing’an—Zhangguangcai Range, we sampled syenogranites, monzogranites, granodiorites, diorites, and gabbros.

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Image created by the authors in MapGIS6.7 and Core- lDRAW2020; no copyrighted material was used.

The granitoid samples include syenogranite (TW01), monzogranite (TW02), and granodiorite (TW03). The plutons form batholiths and stocks. The Early Jurassic syenogranite intruded the Hongguangyan Formation and Early Jurassic granodiorite and monzogranite. The syenogranite is mainly fine- to medium-grained (Fig 3a–3c). The sample is red in color, with a fine-grained granitic texture and massive structure. It consists mainly of K-feldspar (47 vol.%), quartz (29 vol.%), plagioclase (22 vol.%), and biotite (2 vol.%). The monzogranite has a fine- to medium-grained granitic texture and massive structure (Fig 3d–3f), and consists of quartz (35 vol.%), K-feldspar (32 vol.%), plagioclase (25 vol.%), and biotite (8 vol.%). The granodiorite has a fine- to medium-grained granitic texture and massive structure (Fig 3g–3i), and consists of plagioclase (50 vol.%), quartz (25 vol.%), K-feldspar (15 vol.%), and biotite (10 vol.%). Accessory minerals include magnetite, zircon, titanite, and apatite.

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(a-c) Field photographs and photomicrographs of syenogranite; (d-f) Field photographs and photomicrographs of monzogranite; (g-i) Field photographs and photo- micrographs of granodiorite; (j-k) Microphotographs of the diorite; (l) Microphoto- graphs of the gabbro (Bt: biotite; Kfs: K-feldspar; Pl: plagioclase; Q: quartz; Am: amphibole; Ol: oivine; Px: pyroxene; Ap: apatite; Mag: magnetite).

The diorite (TW04) occurs in the form of a stock. The Early Jurassic diorite intruded a gabbro, and was intruded in turn by granodiorite and monzogranite. The sample is gray—black in color, with a fine-grained granular texture and massive structure (Fig 3j). It consists of plagioclase (70 vol.%), amphibole (20 vol.%), biotite (7 vol.%), and quartz (3 vol.%), with accessory magnetite and zircon.

The gabbro (TW05) occurs as a small stock, and is intruded by Early Jurassic diorite, granodiorite, and monzogranite. The sample is gray—black in color and has a gabbroic texture and massive structure (Fig 3k and 3l). The sample consists of pyroxene (40 vol.%), plagioclase (40 vol.%), amphibole (15 vol.%), olivine (5 vol.%), and accessory minerals are apatite, titanite, and zircon.

Analytical methods

Zircon U-Pb dating

The zircon grains were separated in the laboratory of the Langfang Fengzeyuan Rock and Ore Detection Technology Company, China. After mechanical crushing, and heavy liquid and magnetic separation, we handpicked relatively complete and transparent zircon grains under a binocular microscope. Zircons were mounted in epoxy resin and polished to expose their centres for cathodoluminescence (CL) imaging at the Beijing Createch Testing Technology Company, China. The zircons were dated by laser ablation—inductively coupled plasma—mass spectrometry (LA–ICP–MS). The data processing was undertaken with ICP–MS Data Cal software. The standard zircon 91500 was used as the external standard, and the standard zircon GJ-1 was used for monitoring data quality. NIST 610 were used as an external standard to calibrate zircon trace element contents, and ²⁹Si was used as an internal standard. Common Pb was corrected following Andersen (2002) [42]. The U–Pb age calculations and concordia plots were obtained with Isoplot 3.0. The concordia ages are quoted at the 95% confidence level and the dating results are presented in Table 1.

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Whole-rock major and trace element analyses

We sampled representative intrusive rocks from outcrops and trenches in the study area for geochemical analysis. Major and trace element analysis was carried out at the Geological Research and Testing Center of First Geological Exploration institute of Heilongjiang Province, China. Fresh rock samples were washed with distilled water and air-dried. The samples were then dried in an oven at 120°C and powdered to 200 mesh with an agate mortar and pestle. Major and trace elements were determined by X-ray fluorescence (XRF) spectrometry with an accuracy of <3%. Trace elements were determined by ICP–MS. The major and trace element data are listed in Table 2.

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Results

Zircon U-Pb ages

Zircon grains from five intrusive rocks were selected for zircon U-Pb dating, including syenogranite, monzogranite, granodiorite, diorite and gabbro. The zircon crystals show short columnar, euhedral-subhedral in shape and bipyramidal development, with length:width ratios of 1:1~2:1. The grains have clear oscillatory zoning structure in the CL images (Figs 4a, 4c, 4e, 5a and 5c). All the zircon grains yield high Th/U ratios (0.11–1.80), indicating typical magmatic origin [38, 39].

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The syenogranite was collected from the Yingzuilazi-Diaoshuihu pluton. A total of 20 zircon U-Pb ages were selected and tested, and one discordant age was eliminated. The ²⁰⁶Pb/²³⁸U ages given by 19 zircon grains range from 188 to 197 Ma, and yielded the weighted mean ²⁰⁶Pb/²³⁸U age of 192±2.4 Ma (MSWD = 0.3) (Fig 4b). This indicates the syenogranite was formed in Early Jurassic.

The monzogranite was sampled both sides of south-central Laoyeling highland and the northern part area around the Jiaxinshan-Weixing section. A total of 20 zircon U-Pb ages were selected and tested, excluding one discordant age. The ²⁰⁶Pb/²³⁸U ages given by 19 zircon grains range from 183 to 193 Ma, and yielded the weighted mean ²⁰⁶Pb/²³⁸U age of 187±1.6 Ma (MSWD = 0.81) (Fig 4d). This indicates that the formation age of monzogranite is Early Jurassic.

The granodiorite was collected from the southern pluton of Shuguang forest farm. The zircon grains are small, ranging from 90 to 100 μm, and most of the zircon grains are 90 μm. A total of 20 zircon U-Pb ages were selected and tested, and one discordant age was eliminated. The ²⁰⁶Pb/²³⁸U ages given by 19 zircon grains range from 190 to 197 Ma, and the weighted mean ²⁰⁶Pb/²³⁸U age was 194±2.8 Ma (MSWD = 0.043) (Fig 4f). This suggests that the formation age of granodiorite is Early Jurassic.

The diorite was taken from the 945 highland-698 highland pluton in the north of Laoyeling. The zircon grains are large, ranging from 100 to 130 μm. Most of the zircon grains are 100 μm, and the large ones can reach more than 150 μm. A total of 20 zircon U-Pb ages were selected and tested, and 3 discordant ages were removed. The ²⁰⁶Pb/²³⁸U ages given by 17 zircon grains range from 194 to 204 Ma, and yielded the weighted mean ²⁰⁶Pb/²³⁸U age of 197±2.9 Ma (MSWD = 0.14) (Fig 5b). It indicates that the diorite was formed in Early Jurassic.

The gabbros were collected from the 945 highland pluton in the north of Laoyeling. In the sample, the zircon grains are large, ranging from 100 to 150 μm. A total of 20 zircon U-Pb ages were selected and tested. The ²⁰⁶Pb/²³⁸U ages given by 20 analytical zircon grains range from 189 to 197 Ma, and yielded the weighted mean ²⁰⁶Pb/²³⁸U age of 193±2.5 Ma (MSWD = 0.3) (Fig 5d). It suggests that the gabbros were formed in Early Jurassic.

Major elements

The SiO₂ contents of the granites are 69.64~78.58 wt.%, the contents of total alkali (K₂O+Na₂O) are 6.38%~8.45 wt.%, and the contents of Al₂O₃ are 11.31~15.37 wt.%, with low MgO and P₂O₅ contents. All granitoid samples plot in the granite field in the TAS diagram (Fig 6a). These granites are calc-alkaline series in FeO^T-(Na₂O+K₂O)-MgO diagram (Fig 6b). Granites are high-K calc-alkaline series in K₂O-SiO₂ diagram (Fig 6c). Their A/CNK ratios range from 1.00 to 1.14, belonging to the weakly peraluminous granites (Fig 6d).

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(a) TAS diagram of intrusive rocks (Base map is cited from [43]); (b) FeO^T-(Na₂O+K₂O)-MgO diagram of intrusive rocks (Base map is cited from [44]); (c) K₂O-SiO₂ diagram (Base map is cited from [45]); (d) A/NK-A/CNK diagram of intrusive rocks (Base map is cited from [46]) (Basic rock data cited from [9, 25, 31], Granite data cited from [1, 22, 26, 31, 47–49], The data of diorite and dioritic enclaves are cited from [1, 9, 47, 48]. The date can be referred to S1 Table).

The diorites contain SiO₂ = 54.62~60.58 wt.%, Al₂O₃ = 14.34~19.23 wt.%, MgO = 2.76~3.67 wt.%, Mg^# = 42.07~46.99, and total alkalis contents (Na2O+K2O) = 4.71~6.08 wt.%. Diorite samples plot in the diorite area in the TAS diagram (Fig 6a). They are calc-alkaline series in FeO^T-(Na₂O+K₂O)-MgO diagram (Fig 6b). They are medium-K calc-alkaline series in K₂O-SiO₂ diagram (Fig 6c). Their A/CNK ratios range from 0.67 to 0.71, showing metaluminous composition (Fig 6d).

The gabbros show compositional ranges with SiO₂ = 47.48~49.86 wt.%, Al₂O₃ = 16.57~17.84 wt.%, K₂O = 0.41~1.0 wt.%, MgO = 5.89~6.78 wt.%, Mg^# = 53.0~61.9, and total alkalis contents (Na2O+K2O) = 2.7~3.2 wt.%. Samples plot in the gabbroic area (Fig 6a). They are calc-alkaline series in FeO^T-(Na₂O+K₂O)-MgO diagram (Fig 6b). They are medium-K and high-K calc-alkaline series in K₂O-SiO₂ diagram (Fig 6c).

Rare earth elements and trace elements

The syenogranite, monzogranite, granodiorite, diorite and gabbro all show a right-inclined curve of enrichment light rare earth element (LREE) and depletion heavy rare earth element (HREE) in the chondrite-normalized rare earth element (REE) diagram (Fig 7a and 7c). The syenogranite and monzogranite have obvious negative Eu anomalies. The syenogranite, monzogranite and granodiorite are characterized by enrichment of large-ion lithophile elements (LILE, e.g., Sr, K) and depletion of high field-strength elements (HFSE, e.g., Nb, P, Ti, Ta) in the primitive mantle-normalized spider diagram (Fig 7b). The diorites and gabbros are characterized by enrichment of large-ion lithophile elements (LILE, e.g., Ba, Sr, K) and depletion of high strength-field elements(HFSE, e.g., Nb, P, Ta, Zr) (Fig 7d).

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Discussion

Ages of the intrusive rocks from the Lesser Xing’an- Zhangguangcai Range

In recent years, previous studies have carried out on magmatism, plate amalgamation, tectonic setting in the Lesser Xing’an-Zhangguangcai Range. Moreover, they have conducted extensive research on the formation age and petrogenetic types of rocks [9–12, 19–26, 28–30]. Some studies consider that the formation ages of the granites in the Lesser Xing’an-Zhangguangcai Range were mainly in the Mesozoic-Late Paleozoic, with the most intense magmatic activity occurring from Late Triassic to Early Jurassic [10–12, 19–24]. Only minor granites were formed in the Neoproterozoic and Early Paleozoic [13, 14, 29, 30]. Other studies have proposed that the mafic-ultramafic intrusive rocks exposed in Shuguang forest farm, Liuzhonggou, Xincun, Pingfang and Yichun areas of the Lesser Xing’an-Zhangguangcai Range and the diabase in Tieli area [9, 25, 31]. These studies show that the mafic-ultramafic rocks are formed in the Early Jurassic. In recent years, previous have carried out abundant zircon U-Pb dating studies on the pluton in the Lesser Xing’an-Zhangguangcai Range. And the Early Paleozoic pluton is corrected to late Paleozoic and Mesozoic [27, 51]. In this paper, we conducted zircon U-Pb dating on five types of intrusive rocks in the study area. The ages of intrusive rocks are 197–187 Ma. In summary, this is consistent with the previous geological study results.

The spatiotemporal distribution pattern of intrusive rocks in the Lesser Xing’an-Zhangguangcai Range is of significance to explore the tectonic setting of the region. Ge et al.(2020b) collected formation ages of Late Paleozoic-Mesozoic granites, showing a spatiotemporal characteristic of gradually becoming juvenile from east to west [26]. In this paper, we not only collects the age of granites, but also adds the age of intermediate—mafic intrusive rocks (Table 3). Due to this area is located near the Jiamusi-Yilan fault of the northern section of the Tanlu fault. In order to eliminate the influence of strike-slip displacement caused by the Jiamusi-Yilan fault, the age data are divided into two groups based on the north and south sides of the fault to plot diagrams (Fig 8a–8c). We find that the Late Paleozoic-Mesozoic intrusive rocks gradually become juvenile from east to west.

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Petrogenesis

Petrogenesis and magmatic evolution of the granites.

The types of granitoids include syenogranite, monzogranite, and granodiorite. They consist mainly of quartz, plagioclase, K-feldspar, and amphibole, along with accessory apatite, zircon, magnetite, and titanite. The granitoids do not contain minerals characteristic of typical S-type granites, such as muscovite, garnet, and cordierite [71]. The samples are metaluminous to weakly peraluminous, with A/CNK < 1.1. These geochemical characteristics are distinct from those of S-type granites [72, 73]. All samples plot in the I-type granite field in an AFM diagram (Fig 9d). However, highly fractionated I- and A-type granites can exhibit similar mineralogical and geochemical features [72].

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(a) FeO^T/MgO-w(Zr+Nb+Ce+Y)diagram (Base map is cited from [74]); (b) Zr-Ga/Al diagram (Base map is cited from [74]); (c) Ce-SiO₂ diagram (Base map is cited from [75]); (d) AFC diagram of granite in the study area (Base map is cited from [76]) (The reference data come from [1, 22, 26, 31, 47, 48]).

Alkaline mafic minerals (riebeckite—arfvedsonite and aegirine—augite) and Fe-rich olivine (fayalite) are usually important mineralogical indicators of A-type granites [19, 26]. The studied granites contain alkali feldspar, quartz, plagioclase, and minor biotite and amphibole, but do not include alkaline mafic minerals. The mineralogy is typical of highly fractionated I-type granites. The granite samples plot in the I-type granite field in FeO^T/MgO–(Zr + Nb + Ce + Y), Zr–10000Ga/Al, and Ce–SiO₂ diagrams (Fig 9a–9c). Furthermore, the low zircon saturation temperature (T_zr = ~779°C) of the samples differs from those of A-type granites (>800°C) (Table 2), but is consistent with those of highly fractionated I-type granites.

I-type granites can form by: (1) fractional crystallization of mantle-derived mafic magmas [77]; (2) partial melting of lower crustal material [78]; or (3) mixing of mantle- and crustal-derived magmasl [79]. The studied granitoids are characterized by high silica and alkali contents, and low MgO and CaO contents. They are metaluminous to peraluminous, high-K calc-alkaline rocks, with relatively low Mg^# values. These features indicate the granitic magmas were derived from the crust.

The granites have relatively high SiO₂ contents and A/CNK values, and negative anomalies in Nb, Ta, P, Eu, and Ti, indicating the magmas experienced fractional crystallization [80, 81]. In Harker diagrams (Fig 10), TiO₂, Al₂O₃, MnO, CaO, and Mg^# decrease with increasing SiO₂, whereas K₂O increases. These features are consistent with fractional crystallization of biotite, plagioclase, amphibole, titanite, and apatite. The Eu anomalies are due to fractional crystallization of K-feldspar and plagioclase. The P depletion is due to fractional crystallization of apatite, and the Ti depletion was caused by fractional crystallization of minerals such as ilmenite and titanite. These inferred fractionating phases are consistent with the petrography.

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Petrogenesis and magmatic evolution of the diorites.

Previous studies have proposed three models for the formation of diorites: (1) melting of mafic lower crust [82]; (2) fractional crystallization of mantle-derived magma [83]; and (3) partial melting of mantle metasomatized by subduction-related components [84, 85]. The magmas produced by melting of mafic lower crust typically have Mg^# values of <40. Diorites formed by fractional crystallization of mantle-derived magmas generally have high Mg^# values (>60) and low TiO₂ contents (<0.5 wt.%) [86]. However, the studied diorites have low Mg^# values (42–47) and high TiO₂ contents (0.70–0.94 wt.%). In Harker diagrams (Fig 10), TiO₂, FeO^T, MnO, MgO, and Mg^# are negatively correlated with SiO₂ contents, indicating the diorites underwent fractional crystallization of amphibole and plagioclase. The samples also define a partial melting trend in a La/Yb–La diagram (Fig 11a), which is not consistent with fractional crystallization. Most of the diorite samples do not plot in the crust source field in a (La/Yb)_N–δEu diagram (Fig 11b), indicating the magmas were not derived from the lower crust. Therefore, the diorites were not derived from the mafic lower crust or by fractional crystallization of mantle-derived magma. The diorites have low SiO₂ and high MgO contents, and are enriched in transition elements, such as V, Ni, Co, and Cr. The average Ti/Zr ratio is 36.5, which is inconsistent with the Ti/Zr ratio of crust-derived magmas (Ti/Zr < 30). The Nb/Ta ratios are 16.24–19.05, with an average of 17.17, similar to the mantle average of 17.5 [50]. The samples plot in the subduction-metasomatized lithospheric mantle field on a La/Ba–La/Nb diagram (Fig 12d). Therefore, the source of the diorites was mantle that had been metasomatized by subduction components.

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(a) La/Yb-La diagram (Base map is cited from [87]); (b) (La/Yb)_N-δEu diagram (Base map is cited from [87]).

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(a) La/Nb-SiO₂ diagram (Base map is cited from [87]); (b) Ce/Pb-SiO₂ diagram (Base map is cited from [87]); (c) Ba/Nb-La/Nb diagram (Base map is cited from [91]); (d) La/Ba-La/Nb diagram (Base map is cited from [92]).

Mantle-derived magmas can be contaminated by crust during magma ascent. In general, there is a significant linear relationship between Ce/Pb or Nb/La ratios and SiO₂ contents when diorites experience crustal contamination [88]. However, the studied diorites lack this linear relationship (Fig 12a and 12b). In addition, the diorites have no obvious positive Zr anomalies. In a Ba/Nb–La/Nb diagram (Fig 12c), the samples plot in the arc volcanic field and not between the crust and mantle fields, which precludes the possibility of significant crustal contamination. If the mantle source had been metasomatized by subduction zone melts, it would be relatively enriched in Th and light rare earth elements (LREEs; Th/Yb ≥ 2). However, the Th/Yb ratios of the diorites in the study area are 0.97–1.54, indicating the dioritic magma was not derived from a source that had been metasomatized by sediment-derived melt [89, 90]. In addition, in Th/Yb–Ba/La and Nb/Y–La/Yb diagrams (Fig 13a and 13b) the diorite samples plot in the field of fluid metasomatism, indicating the dioritic magma was derived from a source that had been metasomatized by fluids generated by dehydration of a subducted oceanic plate.

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(a) Th/Yb-Ba/La diagram (Base map is cited from [93]); (b) Nb/Y-La/Yb diagram (Base map is cited from [89]); (c) La/Ba-La/Nb diagram (Base map is cited from [92]); (d) Sm/Yb-Sm diagram(Base map is cited from [94]) (The reference data come from [9, 25, 31]).

Petrogenesis and magmatic evolution of the gabbros.

The studied gabbros consist of pyroxene, plagioclase, amphibole, and olivine, and the amphibole is altered, which may have affected the geochemistry. The element Zr is used to assess the mobility of other elements because of its immobile characteristics [95–97]. There is a positive correlation between Zr and Th, Sm, La, Nb, Ti, and Ta contents, indicating these elements were not affected by alteration (Fig 14) [98].

[Figure omitted. See PDF.]

The gabbros have low SiO₂ contents, high Mg^# values, and high TiO₂ contents, indicating they were derived by partial melting of the mantle [99, 100]. Mantle-derived magmas are susceptible to crustal contamination during magma ascent [101]. The continental crust is strongly depleted in Nb, Ta, and Ti [50, 102]. If the magma undergoes crustal contamination, it will develop island arc-like or crust-like geochemical properties [103]. The studied gabbros are characterized by enrichments in large-ion lithophile elements (LILEs; Ba and K) and depletions in high-field-strength elements (HFSEs; Ta and Ti), indicative of mantle-derived magma contaminated by continental crust. However, other evidence suggests that the mantle-derived magmas were not contaminated by the crust. Despite the relative enrichment of Zr and Hf in the continental crust, Zr in the studied samples does not exhibit obvious positive anomalies in primitive mantle-normalized trace element diagrams (Fig 7d). In addition, compared with the continental crust, the gabbros have lower Th/Ce (0.02–0.06), Th/La (0.04–0.14), and Th/Yb (0.27–0.74) ratios, and higher Nb/Th (2.56–4.45) ratios. These results indicate the mafic magmas might not contaminated by the crust. Therefore, the parental magmas of the gabbros in the Shuguang Forest Farm area were not obviously contaminated by the crust during magma ascent. As such, the negative Ta and Nb anomalies reflect those of the mantle source.

Fractional crystallization also occurs during magma ascent and changes the geochemical composition of the magma. In Harker diagrams (Fig 10), TiO_2, FeO^T, and MgO are correlated negatively with SiO₂, indicating fractional crystallization of plagioclase, Fe–Ti oxides, and pyroxene. On Co–Mg^# and Ni–Cr diagrams (Fig 14), there are positive correlations, indicative of olivine and pyroxene fractional crystallization during formation of the gabbros [104, 105]. The gabbros do not exhibit an obvious negative Eu anomaly in chondrite-normalized REE diagrams (Fig 7c), indicating limited plagioclase fractionation.

The gabbros is enriched in LREEs and LILEs, and depleted in HREEs and HFSEs, and it can be inferred that the gabbroic magma was derived from a mantle source that had been metasomatized by subduction-related fluids or melts [104–109]. Previous studies have shown that fluid derived from a subducted slab is enriched in Ba, Rb, U, and Pb, and depleted in LREEs, Th, and HFSEs (e.g., Zr, Nb, and Ta) [110, 111]. The melts produced by partial melting of subducted sediments are enriched in LREEs, Th, Rb, Ba, U, Sr, and Pb [112]. The gabbroic samples of this study are enriched in Ba, K, and Sr, and depleted in Nb, Ta, and Th (Fig 7d), indicating their source was metasomatized by subduction-related fluids. Source modification by a fluid rather than a sediment-derived melt is consistent with the Th/Yb–Ba/La (Fig 13a) and Nb/Y–La/Yb plots (Fig 13b). In addition, the Th/Yb ratios of the studied gabbros are 0.27–0.74, indicative of the source being modified by subduction-related fluids [89, 90].

The REE contents and ratios can be used to infer the origins and degree of melting of mantle-derived magmas [94, 113]. The Sm/Yb ratio can be used to identify the mineralogy of the mantle source [94]. In La/Ba–La/Nb (Fig 13c) and Sm/Yb-Sm diagrams (Fig 13d), the samples plot in the subduction metasomatized lithospheric mantle field and near the partial melting trend for spinel–garnet (1:1) lherzolite. This indicates the mantle source was spinel–garnet lherzolite, and the degree of partial melting was 10%–20%.

Tectonic implications

The Lesser Xing’an–Zhangguangcai Range is located between the Jiamusi and Songnen massifs, and contains Late Paleozoic-Mesozoic igneous rocks. Most of these rocks are part of the medium- to high-K calc-alkaline series. They are enriched in LREEs and LILEs, and depleted in HREEs and HFSEs. This suggests they have arc-related characteristics typical of igneous rocks associated with subduction zones [1, 25, 26, 47–49, 114, 115]. Discrimination diagrams for the granites, diorites, and gabbros in the study area show the studied rocks plot in the arc-related pluton field (Fig 15a and 15b). Our samples and other granites in this region almost all plot in the island arc granite field (Fig 15c and 15d). In a Th/Yb–Nb/Yb diagram (Fig 16a), the gabbroic samples exhibit geochemical characteristics related to subduction, and plot in the island arc basalt field in a La–La/Nb diagram (Fig 16b). The studied diorites plot mainly in the active continental margin field in a Ta/Yb–Th/Yb tectonic discrimination diagram (Fig 17a). In a Ce/Pb–Ba/La diagram (Fig 17b), the samples all plot in and near the sediment and subduction zone igneous rock fields. This indicates their formation environment was related to subduction and that their source was modified by sediments.

[Figure omitted. See PDF.]

(a) Sr/Y-Y diagram (Base map is cited from [116]); (b) (La/Yb)_N-Yb_N diagram (Base map is cited from [116]); (c) Nb-Y diagram (Base map is cited from [117]); (d) Ta-Yb diagram (Base map is cited from [117]) (The reference data come from [1, 9, 22, 25, 26, 31, 47–49]).

[Figure omitted. See PDF.]

(a) Th/Yb-Nb/Yb diagram (Base map is cited from [96]); (b) La/Nb-La diagram (Base map is cited from [118]) (The reference data comes from [9, 25, 31]).

[Figure omitted. See PDF.]

(a) Th/Yb-Ta/Yb diagram (Base map is cited from [119]); (b) Ba/La-Ce/Pb diagram (Base map is cited from [120]) (The reference data come from [1, 47, 48]).

The Lesser Xing’an—Zhangguangcai Range was located in an active continental margin environment during the Jurassic, and the magma source was modified by subduction-related fluid derived from oceanic lithosphere [1, 9, 121, 122]. Previous studies of Early—Middle Triassic collisional granites from the southern margin of the Xingmeng Orogenic Belt have concluded that the Paleo-Asian Ocean closed in the Early—Middle Triassic. Late Triassic bimodal igneous rocks in the Zhangguangcai Range suggest the region was in an extensional setting during this period, which also indicates the Paleo-Asian Ocean closed before the Late Triassic [3, 31, 123, 124]. Therefore, the tectonic setting in the Early Jurassic was not related to Paleo-Asian Ocean. The ‘Mudanjiang Ocean’ refer to an ancient ocean between the Jiamusi and Songnen—Zhangguangcai Range massifs [14]. The Mudanjiang Ocean may have been the dominant factor in the Mesozoic tectonic evolution of this region. Therefore, the tectonic evolution of the Mudanjiang Ocean is of significance in understanding the tectonic history of these two massifs. The timing and polarity of subduction in the Mudanjiang Ocean are controversial. Liu et al.(2019) determined the age of an ophiolitic melange in northeast China, and concluded that the Mudanjiang Ocean existed from the Late Permian to Middle Jurassic [15]. Based on a study of the Heilongjiang Complex and detrital zircon geochronology, Sun et al.(2018) and Xu et al.(2019) suggested that the Mudanjiang Ocean existed during the Middle Triassic—Early Jurassic [17, 125]. Based on the ages of blueschists and plagioclase amphibolites with ocean island basalts (OIB) and mid ridge island basalts (MORB), Dong Y.(2018a) proposed that the Mudanjiang Ocean existed during the Late Paleozoic—Early Jurassic [12]. Given the temporal and spatial distribution of arc magmatism, as well as its petrogenesis, it is inferred that the subduction polarity in the Mudanjiang Ocean was mainly westward [11, 16] and/or bidirectional [12, 13, 18].

Based on the temporal and spatial distribution, petrogenesis, and tectonic setting of igneous rocks in the Lesser Xing’an—Zhangguangcai Range on the eastern margin of the Songnen and Jiamusi massifs, we consider that the Mudanjiang Ocean existed from the Early Permian to Middle Jurassic, and the subduction polarity was bidirectional (Fig 18).

[Figure omitted. See PDF.]

1. During 288–250 Ma, the Mudanjiang Ocean had already opened and was undergoing bidirectional subduction. Ge et al.(2017, 2018) obtained the protolith ages of blueschists in the Early Permian Heilongjiang Complex in Yilan (tholeiitic series = 288 ± 2 Ma; alkaline series = 288 ± 2 Ma) and showed it had OIB-like features [10, 11], indicating the Mudanjiang Ocean between the Jiamusi and Songnen massifs was open by at least the Early Permian. Dong et al.(2018b) proposed that the Early Permian Yilan amphibolites (274 Ma) in the Heilongjiang Complex formed at an active continental margin [126], indicating the Mudanjiang Ocean had opened and was experiencing subduction at this time. The Permian igneous rocks along the western margin of the Jiamusi Massif and eastern margin of the Songnen Massif are bimodal [6, 13, 127], indicating an extensional environment. The N–S-trending Permian granite belt located along the eastern margin of the Songnen—Zhangguangcai Range Massif (Permian arc-related igneous rocks are distributed in the Lesser Xing’an—Zhangguangcai Range, including the Zhushan [12], Hengtoushan [12], and Huangqigou areas [70]), indicates the Mudanjiang Ocean experienced westward subduction. A N–S-trending belt of Permian granite occurs to the east and west of the Jiamusi Massif. However, Permian arc-related igneous rocks in the eastern Jiamusi Massif (302–260 Ma) [128–132] were formed earlier than Permian arc-related igneous rocks in the western Jiamusi Massif (296–246 Ma) [29, 51, 133, 134], indicating the latter were formed by eastward subduction in the Mudanjiang Ocean.

2. Before 180 Ma, the Mudanjiang Ocean continued to experience bidirectional subduction, and the oceanic basin decreased in size. Triassic and Early Jurassic arc-related igneous rocks along the eastern margin of the Songnen—Zhangguangcai Range indicate the Mudanjiang Ocean experienced westward subduction (e.g., in the Taiqing [14], Lianzhushan [63], Tianqiaogang [62], Xingfulinchang [19] and Shuguang Forest Farm areas). There are no Early—Middle Triassic ophiolites or arc igneous rocks along the eastern margin of the Jiamusi Massif, and only Early Triassic (250–246 Ma) I-type granites occur in the Fuxing Forest Farm and Diaoling Town areas of Linkou County along the western margin of the Jiamusi Massif [51], indicating eastward subduction in the Mudanjiang Ocean. The Early Jurassic (197–187 Ma) intrusive rocks in the Shuguang Forest Farm area of the Lesser Xing’an—Zhangguangcai Range formed along an active continental margin, indicating the Mudanjiang Ocean was experiencing subduction at this time. Late Mesozoic—Paleogene intrusive rocks in the Lesser Xing’an—Zhangguangcai Range gradually young from east to west, which also shows that subduction in the Mudanjiang Ocean occurred during the Mesozoic—Paleogene. The Lesser Xing’an—Zhangguangcai Range contains abundant late Paleozoic and Mesozoic igneous rocks that are medium- to high-K calc-alkaline in composition. They are enriched in LREEs and LILEs, and depleted in HREEs and HFSEs, and have arc-like geochemical properties, suggesting the Mudanjiang Ocean was undergoing subduction during this period.

3. Before 160 Ma, the Mudanjiang Ocean continued to undergo bidirectional subduction and finally closed. The metamorphic ages of the Heilongjiang Complex can constrain the timing of closure of the Mudanjiang Ocean. Phengite ⁴⁰Ar/³⁹Ar ages (186–165 Ma) of metasedimentary and blueschist-facies rocks in the Heilongjiang Complex are younger than [17, 31, 135], and partly overlap, those of metamorphic zircon and arc-related igneous rocks in the Zhangguangcai Range, suggesting the phengite ⁴⁰Ar/³⁹Ar ages record the long-term tectonic exhumation of high-pressure metamorphic rocks due to subduction of the Mudanjiang oceanic lithosphere and collision between the Jiamusi and Songnen massifs. Dong et al. (2018b) reported rutile U–Pb ages (172 ± 5 and 177 ± 11 Ma) for arc-related amphibolites in the Yilan area that are similar to the youngest age of continental arc-related igneous rocks in the Zhangguangcai Range [126]. Yu et al.(2023) suggested the rutile U–Pb ages record local crustal thickening that was caused by the final closure of the Mudanjiang Ocean and the soft collision between the Jiamusi and Songnen massifs [136]. In summary, we conclude that the Mudanjiang Ocean closed during the Middle Jurassic (180–165 Ma).

Conclusions

1. The ages of intrusive rocks in the study area are 197–187 Ma, including syenogranite (192 ± 2.4 Ma), monzogranite (187 ± 1.6 Ma), granodiorite (194 ± 2.8 Ma), diorite (197 ± 2.9 Ma), and gabbro (193 ± 2.5 Ma). These Early Jurassic ages are consistent with the peak period of magmatism in the Lesser Xing’an—Zhangguangcai Range.

2. The Early Jurassic granites in the study area are highly fractionated I-type granites derived by partial melting of the lower crust, which underwent biotite, plagioclase, amphibole, and titanite fractionation crystallization. The dioritic and gabbroic magmas were derived by partial melting of a mantle source that had been metasomatized by subduction-related fluids and did not undergo obvious crustal contamination. The gabbros underwent fractional crystallization of pyroxene, and the diorites experienced fractional crystallization of amphibole.

3. The Early Jurassic intrusive rocks have arc-like geochemical characteristics, similar to igneous rocks formed in a subduction setting along the eastern margin of the Songnen—Zhangguangcai Range Massif. This indicates they formed in an active continental margin environment, perhaps related to bidirectional subduction in the Mudanjiang Ocean during the Early Jurassic.

Supporting information

S1 Table. Whole-rock geochemical data.

https://doi.org/10.1371/journal.pone.0306465.s001

(XLSX)

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Citation: Zhao Z, Li Z, Li H, Cheng B, Yin Y (2024) Geochronology, geochemistry, and geological significance of early Jurassic intrusive rocks in the Lesser Xing’an- Zhangguangcai Range, northeast China. PLoS ONE 19(8): e0306465. https://doi.org/10.1371/journal.pone.0306465

About the Authors:

Zhonghai Zhao

Roles: Conceptualization, Funding acquisition, Resources, Writing – original draft, Writing – review & editing

E-mail: [email protected]

Affiliations: College of Mining, Liaoning Technical University, Fuxin, Liaoning, China, Liaoning Key Laboratory of Green Development of Mineral Resources, LNTU, Fuxin, Liaoning, China, Northeast Geological S & T Innovation Center of China Geological Survey, Shenyang, Liaoning, China

ORICD: https://orcid.org/0000-0002-1452-6113

Zhongju Li

Roles: Data curation, Software, Writing – original draft, Writing – review & editing

Affiliation: College of Mining, Liaoning Technical University, Fuxin, Liaoning, China

Haina Li

Roles: Data curation, Writing – review & editing

Affiliations: College of Mining, Liaoning Technical University, Fuxin, Liaoning, China, Liaoning Key Laboratory of Green Development of Mineral Resources, LNTU, Fuxin, Liaoning, China

Binbin Cheng

Roles: Data curation, Investigation

Affiliation: Shandong No.3 Exploration Institute of Geology and Mineral Resources, Yantai, Shandong, China

Yechang Yin

Roles: Methodology, Software

Affiliations: College of Mining, Liaoning Technical University, Fuxin, Liaoning, China, Liaoning Key Laboratory of Green Development of Mineral Resources, LNTU, Fuxin, Liaoning, China

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