Liye Liu
Mingxin Duan
Jimin Huang1,3*- 1 Harbin Center for Integrated Natural Resources Survey, China Geological Survey, Harbin, China
- 2 The Northeast Geological Science and Technology Innovation Center of the China Geological Survey, Shenyang, China
- 3 Observation and Research Station of Earth Critical Zone in Black Soil, Ministry of Natural Resources, Harbin, China
- 4 School of Earth Sciences and Resources, China University of Geosciences Beijing, Beijing, China
The Lesser Xing’an-Zhangguangcai Range tectonic belt in northeastern China is located along the eastern margin of the Central Asian Orogenic Belt and serves as the key to understanding the tectonic transition between the Paleo-Asian Ocean and Paleo-Pacific regimes during the Early Mesozoic. This study presented the zircon U-Pb geochronology, Hf isotope, and whole-rock geochemistry of Early Jurassic syenogranites from the northern Zhangguangcailing Range. The LA-ICP-MS zircon dating result indicates a crystallization age of 194 ± 2 Ma. Integrated with regional data, this study confirmed that the Early Mesozoic magmatism in the region was concentrated in the Early Jurassic (180–200 Ma). The granites displayed typical arc-related features, including (1) high SiO2 (70.59–76.81 wt.%), alkali enrichment (Na2O + K2O = 7.65–8.38 wt.%), low Mg and Fe contents, classifying them as the high-K calc-alkaline metaluminous to weakly peraluminous (A/CNK = 0.99–1.04); (2) strong LREE enrichment with weak Eu anomalies (δEu = 0.44–0.81) and HREE depletion ((La/Yb)N = 3.38–16.17); and (3) enrichment in LILEs (Rb, K) with the corresponding depletion in HFSEs (Nb, Ta, and Ti). Harker diagrams showed negative correlations between SiO2 and MgO, TiO2, CaO, TFeO, P2O5, and Eu, indicating fractional crystallization involving amphibole, ilmenite, apatite, and feldspar. The zircon εHf(t) values (+2.7 to +5.0) and the corresponding Meso-to Neoproterozoic crustal model ages (TDM2 = 915–1067 Ma) suggested that the magma originated from partial melting of the Meso-Neoproterozoic mafic lower crust at amphibolite facies. The geochemical and isotopic data collectively identified these rocks as I-type granite. In a regional tectonic context, their formation was interpreted to reflect an active continental margin environment driven by the westward subduction of the Paleo-Pacific Plate during the Early Jurassic, potentially influenced by the closure of the Mudanjiang Ocean, a branch of the Paleo-Pacific.
1 Introduction
Northeast China has experienced extensive phanerozoic magmatism, producing large volumes of Paleozoic-Mesozoic granitoids (Wu et al., 2011; Xu et al., 2013b). Zircon geochronology demonstrates that regional magmatic activity mainly occurred from the Late Paleozoic to Early Mesozoic, with subordinate events occurring during the Neoproterozoic-Early Paleozoic (Ge et al., 2017; Ge et al., 2018). Mesozoic magmatism occurred in three distinct stages: Late Triassic-Early Jurassic (205–158 Ma), Late Jurassic-Early Cretaceous (157–136 Ma), and Late Cretaceous (135–90 Ma) (Ji et al., 2021; Yang et al., 2022). Late Triassic-Early Jurassic granitoids, including quartz diorite, granodiorite, monzogranite, and syenogranite with minor alkali feldspar granite, generally exhibit medium-to high-K calc-alkaline affinities (Xu et al., 2009; Xu M. J. et al., 2013; Li et al., 2016; Ge et al., 2017; Ge et al., 2018; Yin et al., 2021; Zhang et al., 2021). Geochemical trends have consistently shown decreasing P2O5 with increasing SiO2 (Dong et al., 2017; Zhou et al., 2018; Duan et al., 2021), and these rocks are metaluminous to weakly peraluminous (A/CNK <1.1; Liu et al., 2017). Predominantly composed of I- and A-type granites with limited S-type occurrences (Ge et al., 2017; Ge et al., 2018), these plutons record the extended histories of fractional crystallization (Wu et al., 2003a; Wu et al., 2003b). The spatiotemporal distributions demonstrate a westward younging trend of Late Paleozoic-Mesozoic granitoids (Ge et al., 2020a; Ge et al., 2020b), and their Sr-Nd-Hf isotopic compositions reflect juvenile crustal sources, signifying substantial Phanerozoic crustal accretion within the Central Asian Orogenic Belt (Wu et al., 2000; Jahn et al., 2004).
Despite progress in geochronological and geochemical studies, the petrogenetic mechanisms and tectonic settings of granitoids in the Lesser Xing’an-Zhangguangcai Range remain contentious (Wu et al., 2011; Ge et al., 2017; Ge et al., 2018; Ge et al., 2019; Zhu C. Y. et al., 2017). Three main models have been proposed to explain magmatism in the Songnen Block: (1) post-subduction or collisional extension following the closure of the Paleo-Asian Ocean (Guo et al., 2018; Long et al., 2020a; Long et al., 2020b); (2) mantle wedge or crustal melting triggered by subduction of the Paleo-Pacific Plate (Ge et al., 2018; Yu et al., 2013); and (3) crustal thickening due to the collision between the Songnen and Jiamusi blocks (Zhu et al., 2017b; Dong et al., 2017; Dong, 2018). However, there is no consensus regarding which tectonic processes play a dominant role. This study investigated the Early Jurassic syenogranite from the northern Zhangguangcai Range through integrated petrological, geochronological, geochemical, and Lu-Hf isotopic analyses to constrain its petrogenesis and tectonic setting. The results could contribute to refining our understanding of the Mesozoic tectonic evolution mechanisms in Northeast China.
2 Geological background
The Xingmeng Orogenic Belt in northern China is a key segment of the Central Asian Orogenic Belt, forming a tectonic connection between the Siberian Plate and North China Plate (Figure 1a). From the Paleozoic to the Mesozoic era, this region experienced a series of tectonic events, including collision, subduction, and metamorphism, among several micro-blocks, such as the Erguna, Xing’an, Songnen, Jiamusi, Khanka, and Nadanhada terranes, ultimately shaping a complex tectonic framework (Figure 1b) (Şengör et al., 1993). This study focused on the Zhangguangcai Range tectonic belt, which is situated in the eastern portion of the Xingmeng Orogenic Belt. The Dun-Mi Fault defines the southern boundary of the block. While early scholars believed that the region contained an ancient Proterozoic metamorphic crystalline basement (Jilin Bureau of Geology and Mineral Resources, 1988; Heilongjiang Bureau of Geology and Mineral Resources, 1993), recent chronological evidence has indicated that the majority of these geological units, previously considered Precambrian, were primarily formed during the Paleozoic and early Mesozoic periods (Wang F. et al., 2017; Feng et al., 2019; Xu et al., 2019), with only a small number dating to the Neoproterozoic (Quan et al., 2013; Wang et al., 2014).
Figure 1. Simplified tectonic map (a) and geological sketch map (b) of the study area (Xu et al., 2019).
The study area is characterized by the extensive presence of Paleozoic to Early Mesozoic intrusive rocks (Dong, 2018). During the Early Jurassic, vigorous magmatic activity, predominantly felsic in nature, led to the widespread formation of granites, mainly syenogranites, which exhibit a northeast-trending distribution (Figure 2). The exposed strata in the region are primarily represented by the Neoproterozoic Hongguang Formation, a shallow marine marginal clastic sequence composed of metamorphosed intermediate to intermediate-basic volcanic rocks interbedded with phyllite, slate, two-mica schist, and marble. Additionally, the Quaternary strata are extensively developed along the Songhua River within the study area.
Figure 2. Simplified tectonic maps of the study area.
3 Samples and analytical techniques
3.1 Lithofacies characteristics of samples
The syenogranites in the study area are extensively distributed and appear as stocks in the field, with exposed plutons primarily consisting of slightly weathered and altered fine-to medium-grained syenogranites. Their mineral composition is predominantly potassium feldspar (50%–55%), plagioclase (20%), quartz (25%), and a minor amount of biotite (2%–3%) (Figure 3). Potassium feldspar, mainly microcline and orthoclase, forms subhedral plates, typically 2–5 mm in size, with some intergrown quartz in graphic textures and sodic stripes arranged in a dendritic pattern. A few fine plagioclase crystals are embedded within the potassium feldspar, and local plagioclase alteration is present. Plagioclase forms subhedral plates 2–4 mm in size, showing sericitization and weak polysynthetic twinning. Quartz occurs as anhedral grains, generally 2–4 mm in size, with a random distribution, clean surfaces, and light-wavy extinction. Biotite appears as flakes, randomly distributed, with flake sizes ranging from 0.2 to 1.3 mm.
Figure 3. Hand specimen (a) and microphotographs (b) of syenogranite in the study area. Abbreviations: Kfs—K feldspar; Pl—plagioclase; Q—quartz; Bt—biotite.
3.2 Analytical methods
3.2.1 Zircon U–Pb dating
U-Pb dating analyses were conducted using LA-ICP-MS at Beijing Createch Testing Technology Co., Ltd., following the operational procedures described by Hou, 2009. Laser sampling was performed using a 193 nm laser ablation system, and the ion signal intensities were measured using an Analytik Jena PQMS Elite ICP-MS instrument. Helium served as the carrier gas, whereas argon was utilized as the makeup gas and combined with the carrier gas through a T-connector before entering the ICP. Each analysis included a background acquisition phase of approximately 15–20 s (gas blank) followed by 45 s of data acquisition from the sample. Data processing, including raw data selection, background and analyte signal integration, time-drift correction, and quantitative calibration for U-Pb dating, was conducted offline using LADR_1.1.07 (Norris and Danyushevsky, 2018).
Zircon GJ-1 was employed as the external standard for U-Pb dating and analyzed twice for every 5–10 sample analyses. The time-dependent drifts in the U-Th-Pb isotopic ratios were corrected via linear interpolation, based on the variation observed in the GJ-1 standards (i.e., 2 GJ-1 zircons + 5–10 samples +2 GJ-1 zircons). The uncertainty in the preferred values for GJ-1 was propagated to the final sample results. Common Pb correction was unnecessary for all analyzed zircon grains because of the low 204Pb signal and high 206Pb/204Pb ratios. The U, Th, and Pb concentrations were calibrated using NIST 610. Concordia diagrams and weighted mean age calculations were generated using IsoPlot 4.15. The zircon Plešovice analyzed as an unknown sample yielded a weighted mean 206Pb/238U age of 337.4 ± 1.8 Ma (n = 7, 2SD), which could be consistent with its recommended age of 337.13 ± 0.37 Ma (2SD) (Sláma et al., 2008).
3.2.2 Whole-rock major and trace element analysis
Major and trace element analyses were conducted at the Analysis and Testing laboratory of the Harbin Center for Integrated Natural Resources Survey and China Geological Survey. Fresh rock samples were processed using an agate, contamination-free grinding system to a fineness of 200 mesh and then divided into two portions: approximately 15 g sealed in a white polyethylene bottle for XRF analysis and a 50 mg portion for ICP-MS analysis. Major elements were determined using X-ray fluorescence spectrometry (XRF) with an AXIOSMAX spectrometer from Malvern Panalytical utilizing the instrument’s built-in quantitative analysis software with an analytical accuracy generally exceeding 5%. Trace elements were analyzed using a Thermo Fisher XSERIES II ICP-MS instrument, where the solutions were introduced into the high-temperature plasma, and element concentrations were automatically calculated by the mass spectrometer, with an analytical error typically below 5%.
3.2.3 Lu-Hf isotopes of zircon
Hf isotope measurements of zircon micro-areas were performed at the Beijing Createch Testing Technology Co., Ltd. using a laser ablation multi-collector inductively coupled plasma mass spectrometer. The analysis employed a RESOlution-SE solid-state laser ablation system coupled with a NEPTUNE Plus multi-collector plasma mass spectrometer. Internal zircon structures were observed using cathodoluminescence (CL) imaging to select precise analytical spots. Laser ablation was performed for a duration of 27 s, spot diameter of approximately 30 μm, energy density of 6 J/cm2, and frequency of 6 Hz. The Plešovice zircon standard was used as a calibration reference to ensure the analytical accuracy. The measured 176Hf/177Hf ratio remained stable at 0.282488 ± 20 (2SD, n = 6), which is consistent with the values reported by Sláma et al. (2008) within acceptable error margins.
4 Results
4.1 Zircon U–Pb geochronology
The LA-ICP-MS zircon U-Pb dating results for the syenogranite samples from the study area are presented in Table 1. Under a microscope, the selected zircons predominantly appeared as well-formed, colorless, translucent crystals with short-to long-columnar habits (Figure 4), exhibiting long axis lengths ranging from 60 to 220 μm and aspect ratios between 1.5:1 and 4:1. Most zircon grains displayed distinct and consistent oscillatory zoning, characteristic of magmatic origin, without sharp core-rim boundaries but with gradually increasing zoning density from core to rim, possibly reflecting the variations in the crystal growth rates during magma cooling. A few zircons demonstrated clear core-rim structures, likely representing inherited cores from earlier geological events that experienced partial hydrothermal or solid-state recrystallization during subsequent magmatic activity (Gong et al., 2009). The high Th/U ratios of 0.35–0.55 further support their magmatic origin (Rubatto, 2002; Wu and Zheng, 2004).
Table 1. LA-ICP-MS zircon U-Pb dating data of syenogranite in the study area.
Figure 4. Zircon cathodoluminescence diagram of syenogranite in the study area. The red circle is the U-Pb dating position, the green circle is the Lu-Hf isotope analysis position, and the number represents the analysis point number. The ages and 176Hf/177Hf isotope ratios of the test points are labeled below.
All 20 zircon analysis points from the syenogranite sample exhibited good concordance, aligning closely with the U-Pb concordia line (Figure 5), indicating no significant lead loss or post-crystallization isotopic disturbance. The weighted average 206Pb/238U age was calculated to be 194 ± 2 Ma (Figure 5), representing the formation age of the pluton.
Figure 5. Zircon LA-ICP-MS U-Pb concordia diagram from syenogranite in the study area.
4.2 Whole-rock major and trace elements
The whole-rock major and trace element results for the seven syenogranite samples are summarized in Table 2. The major element compositions exhibited limited variability, with SiO2 ranging from 70.59% to 76.81%, Al2O3 from 10.92% to 14.72%, K2O from 4.17% to 5.28%, and Na2O from 3.1% to 4.1%. The TiO2, MnO, and P2O5 contents were all below 1%, and the loss on ignition (LOI) values ranged from 0.03% to 1.61%, suggesting a minimal influence of late-stage alteration or fluid activity and preservation of the original geochemical signatures. The aluminum saturation index (A/CNK) ranged from 0.99 to 1.04, averaging 1.02, placing the samples in the metaluminous to weakly peraluminous fields on the A/NK-A/CNK diagram (Figure 6a). The K2O/SiO2 ratio ranged from 0.06 to 0.07, averaging 0.06, and the samples plotted within the high-K calc-alkaline series on the K2O-SiO2 diagram (Figure 6b). In the TAS and QAP classification diagrams for intrusive rocks (Figures 6d,e), all the samples fell within the granite field, whereas in the R1-R2 diagram (Figure 6c), they were located within or near the syenogranite field. The Rittmann index (σ = (Na2O + K2O)2/(SiO2-43)) ranged from 1.73 to 2.45, confirming their classification as calc-alkaline granite.
Table 2. Major (wt%) and trace (×10−6) elements compositions of syenogranite in the study.
Figure 6. A/NK vs. A/CNK diagram (Maniar and Piccoli, 1989) (a), SiO2 vs.K2O diagram (Peccerillo and Taylor,1976) (b), R1-R2 diagram (De La Roche et al., 1980) (c), TAS diagram (Middlemost, 1994) (d) and QAP diagram (Streckeisen, 1973) (e) of syenogranite in the study area. 1—Alkaline Gabbro; 2—Olivine Gabbro; 3—Gabbro Syenite; 4—Monzonitic Gabbro; 5—Dioritic Gabbro; 6—Gabbro; 7—Monzonite; 8—Monzonite; 9—Monzodiorite; 10—Diorite; 11—Nepheline Syenite; 12—Syenite; 13—Quartz Syenite; 14—Quartz Monzonite; 15—Tonalite; 16—Alkali Granite; 17—Syenogranite; 18—Monzograiite; 19—Granodiorite; 20—Essexite; 21—Peridotite; 22—Ijolite; a—Gabbroic Diorite; b—Diorite; c—Granodiorite; d—Granite; e—Monzodiorite; f—Monzosyenite; g—Quartz Monzonite; h—Syenite; i—Foid Monzosyenite; j—Foidolite Syenite.
The total rare earth element (REE) content of the samples was relatively low, ranging from 75.31 to 159.24 ppm. In the chondrite-normalized REE diagram (Figure 7), the samples exhibited a right-leaning distribution pattern with (La/Yb)N values from 3.38 to 16.17, indicating enrichment in light rare earth elements (LREEs) (67.01–146.72 ppm) and depletion in heavy rare earth elements (HREEs) (6.58–15.41 ppm), along with a relatively weak negative europium anomaly (δEu = 0.35–1.03). In the primitive mantle-normalized trace element diagram (Figure 7), the samples displayed consistent distribution patterns, showing the enrichment in large ion lithophile elements (LILEs) such as Rb and K, and the depletion in high field strength elements (HFSEs) including Nb, Ta, and Ti. Additionally, the samples exhibited varying degrees of Ba depletion and significant depletion in Sr and P.
Figure 7. Chondrite⁃normalized REE distribution patterns diagram and primitive mantle⁃normalized trace element patterns diagram of syenogranite in the study area (Sun and McDonough, 1989).
4.3 Hf isotope characteristics
The Lu-Hf isotope results for zircon in Table 3 present minimal variation in 176Hf/177Hf value (0.282730–0.282797), indicating the strong isotopic consistency. The analyzed zircons exhibited relatively low 176Lu/177Hf ratios (0.001164–0.002033), mostly below or near 0.002, suggesting minimal radiogenic Hf accumulation since formation and confirming that the measured 176Hf/177Hf ratios accurately represent the Hf isotopic composition at the time of zircon crystallization (Amelin et al., 1999). Additionally, the fLu/Hf values ranged from −0.96 to −0.94, significantly lower than those of mafic crust (−0.34) and felsic crust (−0.72) (Vervoort et al., 1996; Amelin et al., 2000), indicating that the two-stage Hf model age could provide a reliable estimate of the magma source’s initial separation time or its average crustal residence age (Liu et al., 2014). The εHf(t) values of sample SHD0042 ranged from +2.7 to +5.0, with corresponding depleted mantle two-stage model ages (TDM2) between 915 and 1067 Ma.
Table 3. Zircon Hf isotopic analysis results of syenogranite in the study area.
5 Discussion
5.1 Jurassic magmatism in the Zhangguangcai Range orogenic belt
The Zhangguangcai Range preserves evidence of intense Late Paleozoic to Early Mesozoic magmatism, notably marked by extensive ∼190 Ma granitic plutons comprising granodiorite, monzogranite, syenogranite, and alkali feldspar granite. These granitoids exhibit characteristic I-type features (Liu et al., 2016; Liu et al., 2017; Ge et al., 2017; Ge et al., 2018) and were interpreted by Wu et al. (2003a), Wu et al. (2003b) as highly fractionated products of prolonged crystal differentiation. Petrogenetic models suggest that their magmas originated either from juvenile crustal melting (Xu M. J. et al., 2013; Li et al., 2016) or mantle-crust magma mixing (Ren, 2019). In contrast, mafic magmatism is spatially and temporally limited, represented by several suites: the Xinxinglinchang gabbro (293 Ma; Long et al., 2020a), Hongguang Formation gabbro-diorite (259 Ma; Wang et al., 2012), Shuguanglinchang hornblende gabbro (215 Ma) and gabbro (210 Ma; Long et al., 2020b), and Tangwanghe-Yichun-Mulan gabbro-gabbro-diorite-amphibolite suite (186–182 Ma; Yu et al., 2012). Early Jurassic mafic rocks (Yu et al., 2012; Ge et al., 2020a) exhibit zircon Hf isotopic and geochemical signatures indicative of derivation from partial melting of the subduction-fluid-metasomatized depleted mantle. Comparative analyses revealed contrasting mantle sources: Lesser Xing’an-Zhangguangcai mafic rocks reflect deep-sea sediment contributions, while their Yanbian counterparts can be characterized by terrestrial sediment-dominated sources (Zhao et al., 2018).
The spatiotemporal evolution of intrusive rocks in the Lesser Xing’an–Zhangguangcai Range provides critical insights into the tectonic evolution of the region. By integrating regional zircon U-Pb geochronological datasets, this study confirmed that Early Mesozoic magmatism peaked during the Early Jurassic (180–200 Ma) (Supplementary Table S1; Figure 8a). These intrusive rocks were primarily concentrated between 127° and 130°E (Figure 8b), forming a prominent north-south-trending magmatic belt. Importantly, Early Mesozoic intrusive rocks exhibited distinct spatiotemporal patterns. After accounting for strike-slip displacement along the Yitong-Yilan Fault (a northern extension of the Tanlu Fault Zone) and categorizing the data into north and south of the fault, our study identified a westward-younging magmatic migration trend (Figure 8b). This finding reinforces previous models of westward migration of magmatic activity based on granite data (Ge et al., 2020b) and extends their applicability by including chronological evidence from intermediate-mafic intrusions. The syenogranite dated in this study yielded a zircon LA-ICP-MS U-Pb weighted mean age of 194 ± 2 Ma, with zircon grains showing typical magmatic growth zoning and Th/U ratios between 0.35 and 0.55. The narrow age range of 8 Ma among all the analyzed points indicated that the syenogranite was emplaced in the early Jurassic. Together with regional data, these results confirmed that extensive magmatism occurred in the Lesser Xing’an-Zhangguangcai Range during the Early Jurassic.
Figure 8. Zircon U-Pb ages characterization of intrusive rocks in the Lesser Xing’an- Zhangguangcai Range (a, b).
5.2 Petrogenesis of the syenogranites
Most sample points on the genetic discriminant diagrams fell within the I- and S-type granite fields, with only a few near the boundary separating the A-type from the I-and S-type granites (Figures 9a,b). Based on the zircon saturation temperature calculation method of Watson and Harrison (1983), the syenogranites yielded temperatures between 688°C and 791°C, which were significantly lower than the typical formation temperatures of A-type granites (>900°C) (Eby, 1992), indicating that the studied rocks were not A-type granites. Additionally, the samples showed only a slight negative Eu anomaly, in contrast to the strongly negative Eu anomaly generally observed in the A-type granites. Microscopic analysis revealed no alkali-rich minerals, such as riebeckite or aegirine, and the plagioclase content was relatively high. Both features were inconsistent with the A-type granite mineralogy (Chappell, 1999), further confirming that the syenogranites were not of A-type affinity.
Figure 9. Identification of genetic types of syenogranite in the study area (Sylvester, 1989; Whalen et al., 1987) (a) K2O + N2O–Ga/Al diagram; (b) TFeO/MgO–Zr + Nb + Ce + Y diagram; (c) (Al2O3 + CaO)/TFeO + K2O + Na2O–100*(MgO + TFeO + TiO2)/SiO2 diagram; (d) Th–Rb diagram.
The S-type granite magmas generally originated from phosphorus-rich sedimentary rocks, where phosphorus cannot be fully incorporated into minerals during magmatic evolution, resulting in simultaneous increases in SiO2 and P2O5 contents. In contrast, the I-type granite magmas were derived from crustal mafic rocks or mantle materials, with phosphorus being progressively excluded as the SiO2 content increased and the P2O5 content decreased. This trend is consistent with the granite characteristics observed in the study area (Figure 10) (Chappell, 1999; Qiu et al., 2024). Moreover, the complete absence of aluminum-rich minerals such as garnet, muscovite, tourmaline, and cordierite, coupled with the weakly peraluminous nature (A/CNK = 0.99–1.04) and the positive correlation between Rb and Th, further supported the interpretation that the syenogranites were not S-type but belonged to the I-type granite category (Figure 9d) (Qiu et al., 2008).
Figure 10. Harker variation diagrams for the samples.
The rock samples displayed a high SiO2 content (>70%), elevated K2O/Na2O ratios (>1), enrichment in large ion lithophile elements (LILE) such as K and Rb, and depletion in high field strength elements (HFSE), including Nb, Ta, and Ti. These geochemical features, combined with the high differentiation indices (DI = 96–98), were consistent with the traits of the highly fractionated I-type granites (Wang Z. Z. et al., 2017). Furthermore, the syenogranite sample points plotted on the TFeO/MgO-Zr + Nb + Ce + Y (Figure 9b) and (Al2O3+CaO)/TFeO + K2O + Na2O–100×(MgO + TFeO + TiO2)/SiO2 diagrams (Figure 9c) were situated within the highly fractionated field. Thus, based on their geochemical and mineralogical characteristics, the syenogranites in the study area were identified as highly fractionated I-type granites.
5.2.1 Fractional crystallization process
The samples displayed a right-leaning rare earth element (REE) distribution pattern characterized by relative enrichment in light rare earth elements (LREEs) and depletion in heavy rare earth elements (HREEs), accompanied by a weak negative Eu anomaly. They were enriched in large ion lithophile elements (LILEs) such as Rb and K and depleted in high field strength elements (HFSEs) including Nb, Ta, and Ti, with varying degrees of Ba depletion and notable depletion in Sr and P. The negative Eu anomaly commonly observed in granites is generally attributed to fractional crystallization of plagioclase or retention of plagioclase in the magma source. Sr was concentrated in feldspars through the isomorphous substitution of Ca and Na, whereas Ba was preferentially incorporated into K-rich minerals such as potassium feldspar and biotite during the late stages of magma evolution, occupying K sites in early crystallized K-bearing phases. Consequently, plagioclase fractionation led to Eu-Sr depletion, while the crystallization of potassium feldspar and biotite contributed to Ba depletion and further enhanced the negative Eu anomaly. The negative anomalies of P and Ti were primarily linked to the fractionation of accessory minerals, such as apatite and titanite. Furthermore, because apatite typically displays a negative Eu anomaly (Sha and Chappell, 1999), its separation may partially offset Eu depletion caused by plagioclase fractionation (Qian et al., 2002).
In the Harker diagrams of the samples, increasing SiO2 content was accompanied by decreasing concentrations of MgO, TiO2, CaO, TFeO, P2O5, and Eu (Figure 10), reflecting the fractional crystallization of various mineral phases during magma evolution. The negative correlations between SiO2 and TiO2, TFeO, and P2O5, along with the pronounced P and Ti depletion in the primitive mantle-normalized trace element spider diagram (Figure 7), suggested the fractional crystallization of titanomagnetite and apatite. Similarly, the inverse relationships between MgO, CaO, Eu, and SiO2 indicated that amphibole and plagioclase also underwent fractional crystallization. Overall, these compositional variations in the syenogranites were primarily attributed to fractional crystallization processes.
5.2.2 Characteristics of magma sources
There are three main interpretations of the magma source of highly fractionated high-K calc-alkaline I-type granites: (1) fractional crystallization of mantle-derived basaltic magma (Soesoo, 2000; Li et al., 2007); (2) magma generation through crust-mantle mixing during underplating of mantle-derived magma in the lower crust (Wu et al., 2003a; Wu et al., 2003b; Xia et al., 2015); and (3) partial melting of mafic lower crustal rocks (Chappell and White, 2001). The Early Jurassic granites investigated in this study were widely distributed across the eastern Songnen Block, while the coeval intermediate to mafic rocks were much less extensive, rendering it unlikely that such large volumes of felsic magma formed solely through the fractional crystallization of mantle-derived melts. Furthermore, the absence of contemporaneous mafic enclaves and the uniform zircon Hf isotopic compositions indicated that the crust-mantle magma mixing was not the dominant mechanism for syenogranite formation. Geochemical evidence supports a crustal origin for syenogranites. Nb/Ta (7.29–11.82, avg. 9.62), Th/Ta (6.08–18.18, avg. 16.62), and Sm/Nd (0.14–0.24, avg. 0.18) ratios were more consistent with crustal values (Nb/Ta = 11, Th/Ta = 11.67, Sm/Nd = 0.25) (Rudnick and Gao, 2003; Sun and McDonough, 1989; Taylor and McLennan, 1985) than with mantle values (Nb/Ta = 17.5, Th/Ta = 2.3, Sm/Nd = 0.33). The rocks also exhibited high SiO2, Al2O3, and total alkali contents; low MgO levels; the enrichment in K, Rb, and Th; and the depletion in Ba, Nb, Ta, P, and Ti. These could align with the characteristics of crust-derived magmas (Green, 1995; Barth et al., 2000), thereby reinforcing a crustal origin for syenogranites.
Experimental petrological studies have demonstrated that magmas generated by the partial melting of basic rocks typically exhibit low MgO content, low Mg# values (<40), and depletion of Cr and Ni (Rapp and Watson, 1995). The geochemical characteristics of syenogranite samples from this region (MgO = 0.06–0.38 wt.%, average 0.18; Mg# = 11.69–25.26, average 18.25; Cr = 14.7–28.8 ppm, average 22.01; Ni < 5 ppm) are highly consistent with this petrogenetic model and overlapped with the major element composition of melts derived from the amphibolite-facies basic rocks in the lower crust (Qian and Hermann, 2013), indicating a source region from partial melting of lower crustal basic rocks. The rare earth element (REE) patterns show the strong fractionation between light and heavy REEs ((La/Yb)N = 3.38–16.17), low HREE contents (Yb = 1.05–3.23 ppm; Y = 8.77–26.5 ppm), and relatively flat HREE distribution curves ((Gd/Yb)N = 0.85–1.7). These features are consistent with amphibole as the dominant residual phase, given the high partition coefficient of Yb in felsic melts (Klein et al., 1997), which tends to produce flatter HREE patterns than garnet-bearing systems. This is further supported by the observed Y/Yb ratios (6.3–8.75, average 7.78), which are significantly lower than those typical of garnet-residue systems (Y/Yb > 10) and align more closely with amphibole-controlled systems (≈10) (Rollinson, 1993). Additionally, the samples plotted within the Hf isotopic composition field of the Phanerozoic igneous rocks in the Xingmeng Orogenic Belt on the t vs εHf(t) diagram (Figure 11), with TDM2 model ages ranging from 915 to 1067 Ma, indicating a Mesoproterozoic to Neoproterozoic lower crustal source. The consistent Hf isotopic signatures suggest a relatively homogeneous magma source, reinforcing the interpretation that the syenogranites in the study area were primarily derived from the partial melting of amphibolite-facies basic rocks in the juvenile lower crust formed during the Mesoproterozoic to Neoproterozoic.
Figure 11. The diagrams between Hf isotopic compositions and the U-Pb age of zircons for the syenogranite in the study area. (a) 176Hf/177Hf-t diagram (Wu F. et al., 2007); (b) εHf(t)-t diagram (Yang et al., 2006).
5.3 Tectonic background
The identification of Early-Middle Triassic collision-type granites along the southern margin of the Xing’an-Mongolian Orogenic Belt provides critical constraints on the timing of the Paleo-Asian Ocean closure, which is estimated to have occurred during the Early-Middle Triassic period. The recognition of Late Triassic bimodal igneous rock assemblages in the Zhangguangcai Range (Wu et al., 2011; Tang et al., 2018; Xu et al., 2019) further supports the interpretation that the Paleo-Asian Ocean could be already closed prior to the Late Triassic period. From the Late Triassic to Early Jurassic, the Mongol-Okhotsk Oceanic Plate subducted beneath the Siberian-Erguna Block in a “scissors-like” closure pattern (Li, 2013; Xu et al., 2019), while the region east of the Songliao Basin was governed by the westward subduction system of the Paleo-Pacific Plate (Xu et al., 2013c; Tang et al., 2018). This tectonic configuration is corroborated by multiple lines of evidence: (1) the widespread presence of Early Jurassic high-K calc-alkaline granite belts in the Yanji-Liaoyuan and Lesser Xing’an-Zhangguangcai Range regions (Zhang et al., 2004; Xue et al., 2024) and (2) the subduction-related geochemical characteristics of Early Jurassic calc-alkaline volcanic rocks in the Jiamusi and Songnen Blocks (Yu et al., 2012; Qin et al., 2016; Wang F. et al., 2017; Wang et al., 2017 Z. H.).
The Mudanjiang Ocean, a paleo-oceanic tectonic unit between the Jiamusi and Songnen Blocks (Wu et al., 2011), has been proposed by previous studies to have existed since at least the Early Permian (Dong et al., 2017; Du et al., 2022; Jing et al., 2022; Yu et al., 2023) and could have evolved continuously as a branch of the Paleo-Pacific Ocean (Sun et al., 2015; Yang et al., 2015; 2019; Yu et al., 2023). The protolith records of OIB-MORB-type blueschists in the Heilongjiang Complex (Jing et al., 2022) together with regional arc magmatic rock belts provide robust constraints on the occurrence of subduction in the Mudanjiang Ocean during the Early Mesozoic. The key supporting evidence includes: (1) Middle-Late Permian arc-affinity mafic rock assemblages in the Luobei-Yilan accretionary complex (Ren, 2017; Dong, 2018) and (2) Late Triassic to Middle Jurassic forearc sedimentary successions in the Heilongjiang Complex (Jing et al., 2022), as well as associated arc magmatic rocks (Dong et al., 2017; Zhu et al., 2017c; Ge et al., 2018; Sun et al., 2018). Additional support can be obtained from the metamorphic evolution data, including the clockwise P-T path of the Heilongjiang Complex (Han, 2018) and metamorphic ages of OIB-MORB-type rocks from metamorphosed sedimentary units in the Luobei region (209–185 Ma) (Jing et al., 2022), which collectively indicate subduction processes during the Early Mesozoic.
The syenogranites in the study area are classified as I-type granites with a high K calc-alkaline affinity and are typically formed in convergent plate margin tectonic settings (Wilson, 1989). These rocks are enriched in light rare earth elements (LREEs) and large ion lithophile elements (LILEs), such as Rb and K, and depleted in heavy rare earth elements (HREEs) and high field strength elements (HFSEs), such as Nb, Ta, and Ti, which exhibit geochemical signatures characteristic of igneous rocks generated in subduction zone environments (McCulloch and Gamble, 1991). In the tectonic discrimination diagrams based on trace elements, all granite samples were within the arc-related magmatic rock field (Figure 12), suggesting a volcanic arc tectonic setting. Considering the regional tectonic background, the Early Jurassic (194 Ma) syenogranite in the northern Zhangguangcai Range formed in an active continental margin setting, which could be closely associated with the westward subduction of the Paleo-Pacific Plate and potentially influenced by the overlapping subduction and closure of the Mudanjiang Ocean, a branch of the Paleo-Pacific. First, the Early Mesozoic magmatic belt in the Lesser Xing’an-Zhangguangcai Range was oriented nearly north-south, parallel to the Heilongjiang Complex, and temporally concentrated in the Early Jurassic (200–180 Ma), displaying geochemical traits indicative of subduction fluid-modified magma sources: (1) medium-to high-K calc-alkaline rocks enriched in LREEs and LILEs but depleted in HREEs and HFSEs, consistent with continental arc environments (Zhao et al., 2018; Ge et al., 2020a; Ge et al., 2020b; Xiao et al., 2023); and (2) mafic rocks (gabbro-amphibolites) showing relatively homogeneous Hf isotopic compositions (εHf = +2.7 to +12.0), suggesting the derivation from partial melting of a depleted mantle wedge metasomatized by slab-derived melts (Yu et al., 2012). The tectonic and geophysical evidence further corroborated the subduction setting: (1) the metamorphic age of the Heilongjiang Complex (202–172 Ma) coincided with the formation age of the studied granites, indicating synchronous subduction-related metamorphism and magmatism (Wu et al., 2008; Zhou et al., 2009; Ge et al., 2016; Dong, 2018); (2) geophysical imaging revealed a high-conductivity wedge-shaped anomaly beneath the Songnen Block, interpreted as a relic subducted slab (Liang et al., 2017); and (3) structural evidence, including regional-scale sinistral ductile shear zones and tectonic fabric analysis, suggested an Early Jurassic oblique compression regime (Shao et al., 2013). Additionally, the analysis of the spatial and temporal distribution of granitic rocks in the Lesser Xing’an–Zhangguangcai Range (Figure 8b) revealed a westward younging trend in Early Mesozoic magmatism, potentially linked to progressive flattening of the Paleo-Pacific subduction angle during this period.
Figure 12. Tectonic discrimination diagrams for the syenogranite in the study area (Harris et al., 1986; Pearce, 1996). (a) Rb-(Y + Nb) diagram; (b) Rb-(Yb + Ta) diagram; (c) Ta-Yb diagram; (d) Rb/30-Hf-Ta×3 diagram.
6 Conclusion
1. The zircon U-Pb age of the syenogranite in the study area was 194 ± 2 Ma (n = 17, MSWD = 1.15), indicating its emplacement during the Early Jurassic. Combined with the regional chronological data analysis, this suggested that large-scale magmatic activity occurred in the Lesser Xing’an -Zhangguangcai Range during the Early Jurassic.
2. The syenogranite in the northern section of the Zhangguangcai Range was characterized as quasi-aluminous to weakly peraluminous with a high-potassium calc-alkaline affinity, having undergone significant crystallization differentiation during magma evolution, and was classified as a highly differentiated I-type granite.
3. Based on the analysis of geochemical characteristics and zircon Hf isotopic signatures, the magma of the syenogranite within the study area was primarily derived from the partial melting of juvenile amphibolite-facies basic lower crust formed during the Mesoproterozoic to Neoproterozoic.
4. Based on the regional geology, isotopic geochronology, and petrogeochemical characteristics, the syenogranite intrusions within the study area were formed in an active continental margin environment, closely associated with the westward subduction of the Paleo-Pacific Ocean during the Early Jurassic, which may have also been influenced by the superimposed subduction-closure process of the Mudanjiang Ocean, a branch of the Paleo-Pacific Ocean.
Data availability statement
The original contributions presented in the study are included in the article/Supplementary Material, further inquiries can be directed to the corresponding authors.
Author contributions
LL: Conceptualization, Formal Analysis, Investigation, Writing – original draft, Writing – review and editing. MD: Writing – review and editing. JH: Funding acquisition, Writing – review and editing. HS: Investigation, Writing – review and editing. XL: Supervision, Writing – review and editing. YZ: Writing – review and editing.
Funding
The author(s) declare that financial support was received for the research and/or publication of this article. This research was funded by the project of Northeast Geological S&T Innovation Center of China Geological Survey (Grants QCJJ2024-17 and QCJJ 2022-2) and China Geological Survey Project (Grants DD20230508, DD20220852 and DD20242940).
Conflict of interest
The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.
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Supplementary material
The Supplementary Material for this article can be found online at: https://www.frontiersin.org/articles/10.3389/feart.2025.1578301/full#supplementary-material
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Keywords: I-type granite, Zhangguangcai Range, lithogeochemistry, U-Pb age, Hf isotop-ic
Citation: Liu L, Duan M, Huang J, Song H, Lin X and Zhan Y (2025) Petrogenesis and tectonic implications of the Early Jurassic syenogranite in the northern section of Zhangguangcai Range, NE China: insights from geochronology, geochemistry, and Lu-Hf isotopes. Front. Earth Sci. 13:1578301. doi: 10.3389/feart.2025.1578301
Received: 17 February 2025; Accepted: 09 April 2025;
Published: 02 May 2025.
Edited by:
Long Li, University of Alberta, CanadaCopyright © 2025 Liu, Duan, Huang, Song, Lin and Zhan. This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.
*Correspondence: Mingxin Duan, ZG14cGFwMjAxNUAxNjMuY29t; Jimin Huang, aHVhbmdqaW1pbkBtYWlsLmNncy5nb3YuY24=