Petrogenesis and relationship with REE mineralization of the quartz syenite from Chishan and Longbaoshan alkaline complex, southeastern North China Craton: Insights from zircon U–Pb geochronology, element, and Sr–Nd–Pb–Hf isotope geochemistry

Mesozoic alkaline complexes associated with the rare earth element (REE) mineralization are developed in southeastern North China Craton (NCC), and they recorded some important information about the lithospheric thinning and destruction of the NCC. Zircon U–Pb dating results reveal that syenitic rocks from the Chishan and Longbaoshan alkaline complexes were emplaced at ca. 126.2–123.7 Ma. These syenitic rocks have an arc-like affinity with enriched LREEs and LILEs (e.g., Ba and Th) and depleted HFSE (e.g., Nb and Ta). However, they plot within the extensional alkaline–calc-alkaline field in the lg (CaO/(K₂O + Na₂O)) versus SiO₂ discrimination diagram and plot within the fields of the divergent plate and within-plate settings in the Nb_N versus Th_N discrimination diagram, implying an extensional tectonic setting. Thus, we suggest that the syenitic rocks should form in an extensional tectonic settings related to rollback and retreat of the subducting Paleo-Pacific plate. These syenitic rocks have similar Sr–Nd–Pb–Hf isotope compositions ((⁸⁷Sr/⁸⁶Sr)_i = 0.7062 to 0.7101, ε_Nd(t) = −8.2 to −15.0, ε_Hf(t) = −13.5 to −9.6), which are the same as the enriched subcontinental lithospheric mantle (SCLM) of the NCC. Taking into account not only our new data but also previously published data regarding the evolution of NCC in the Mesozoic, we conclude that the syenitic rocks from the Chishan and Longbaoshan complexes are derived from partial melting of the lithospheric mantle triggered by the Paleo-Pacific plate subduction. Moreover, the geochemical and Sr–Nd–Pb isotopic similarity between the Chishan REE ores, Longbaoshan altered rocks, and the syenitic rocks implied that they are homologous products of Early Cretaceous and that the mineralization shows inheritance to the magmatic hydrothermal evolution.

1 Introduction

The North China Craton (NCC) is the largest cratonic area at the easternmost point of Eurasia (Yang et al., 2020). It experienced extensive destruction and lithospheric thinning during the Mesozoic (Fan et al., 2000; Goss et al., 2010; Zhai and Santosh, 2011; Zhu et al., 2011; Li and Santosh, 2017; Yang et al., 2018a; Yang et al., 2018b; Yang and Santosh, 2020). This transformation and destruction disturbed the stability of the coupling between the crust and lithospheric mantle and caused activation of the crust, which led to eruption of large-scale magmatism and mineralization during the Mesozoic (Wu et al., 2005; Chen et al., 2007; Goldfarb and Santosh, 2014). Although controversies about the timing, tectonic setting, and mechanism of the lithospheric thinning remain hotly continued (Gao et al., 2002; Zhang H. F. et al., 2007; Wu et al., 2008; Santosh, 2010; Zhu et al., 2011; Zhang et al., 2013), it is generally accepted that the interaction between the crust and the mantle had an important impact during this process (Wilde, et al., 2003; Xu et al., 2004; Gao et al., 2008). Alkaline rocks, as a kind of mantle-derived intrusions, are generally developed in extensional settings (Tu et al., 1984; Qiu, 1993), for instance, post-collisional extension (Bonin et al., 1998) or along deep faults (Jung et al., 2007). They are considered one of the ideal options to study the crust–mantle interaction and continental crust evolution (Yang et al., 2007; Lan et al., 2011).

There are a large number of magmatic rocks related to NCC destruction during the Mesozoic, especially the widespread late Mesozoic alkaline rocks in the Luxi Block, southeastern NCC (Zhang et al., 2005; Lan et al., 2011). These magmatic rocks recorded some important information about lithospheric thinning and destruction of the NCC (Xu et al., 2004; Zhang et al., 2005; Lan et al., 2011; Yang D. B. et al., 2012; Zhang et al., 2014; Yang et al., 2018a), including the lithospheric architecture, crust–mantle interaction, tectonic reactivation, timing, mechanism, and geodynamic setting (Gao et al., 2002; Wu et al., 2008; Santosh, 2010; Zhu et al., 2011; Deng et al., 2018; Yang et al., 2020). Moreover, alkaline rocks in the Luxi Block have a close relationship with the gold and rare earth element (REE) mineralization. For instance, the Longbaoshan complex, which is relatively larger than other alkaline intrusions in the Luxi Block, is closely associated with the mineralization of gold and REE deposits. The Chishan alkaline complex is considered the ore-forming parent rock of the Chishan REE deposit, which holds the third-largest light REE deposit in China, after the Inner Mongolia Bayan Obo and Sichuan Maoniuping REE deposits. With regard to the Longbaoshan and Chishan complexes, the lithologic assemblage is dominated by syenitic rocks, which are the most closely related to REE mineralization. However, the petrogenesis of these syenitic rocks has not been systematically researched until now (Zhang et al., 2005; Lan et al., 2011). In this study, we carried out detailed fieldwork, petrological and mineralogical observations, and obtained element geochemical, zircon U–Pb–Hf isotopic, and Sr–Nd–Pb isotopic data of the quartz syenite from the Longbaoshan and Chishan complexes to identify the nature and petrogenesis of the syenitic rocks and to understand their significance to the crust–mantle interaction. The final goal, using the results from the Longbaoshan and Chishan complexes, is to further our understanding on how magmatic processes control REE enrichment in alkaline magmas in southeastern NCC.

2 Geological background and sampling

2.1 Geological background

The NCC is China’s oldest and largest craton due to its 2.5–3.8 Ga Archean core (Liu et al., 1992). It is separated from the Yangtze Craton by the Qinling–Dabie–Sulu Orogenic Belt to the south and east and from the Central Asian Orogenic Belt by the Bayan Obo–Chifeng–Kaiyuan fault to the north (Figure 1A) (Li et al., 1993; Zhao et al., 2001). In many popular models, the NCC is divided into the Western Block (WB) and Eastern Block (EB), which were welded along the nearly north–south trending Trans-North China Orogen (TNCO) (Zhao et al., 2001; Zhao and Zhai, 2013). The basement rocks within the EB are primarily dominated by Archean to Paleoproterozoic tonalite–trondhjemite–granodiorite (TTG) (Zhao and Zhai, 2013). The WB was the outcome of amalgamation between the Ordos and Yinshan blocks along the Khondalie Belt at 1.95–1.92 Ga (Santosh, 2010; Yang et al., 2018a). The TNCO is a collision orogenic belt between the EB and WB in the Paleoproterozoic (1.85 Ga), with basement rocks of late Neoarchean–Paleoproterozoic TTG gneisses and granitoids (Zhao et al., 2005).

FIGURE 1

FIGURE 1. (A) Simplified geological map of the North China Craton and the location of the Luxi Block (after Zhao et al., 2001; Zhang et al., 2005). (B) Simplified geological map of the Luxi Block (after Zhang H. F. et al., 2007). (C) Simplified geological map of the Longbaoshan alkaline complex (after Lan et al., 2011). (D) Simplified geological map of the Chishan alkaline complex (Wei et al., 2019). (E–H) Photos of field outcrops where the four kinds of samples were collected in.

The Luxi Block is bordered by the Tan-Lu fault in the east, the Liaocheng–Lankao fault in the west, the Qihe–Guangrao fault in the north, and the Fengpei fault in the south (Figure 1B) (Zhang X. M. et al., 2007). The crystalline basement of the Luxi Block incorporates a suite of Neoarchean metamorphic rocks (e.g., gneiss, amphibolite, and deformed/metamorphosed TTG) and Paleoproterozoic granitoids. The sedimentary cover is mainly composed of Paleozoic carbonates and clastic rocks, Mesozoic to Cenozoic terrigenous clastic rocks, and volcaniclastic rocks. In addition, some intermediate-basic rocks, mafic dikes, and alkaline rocks are also exposed (Figure 1B) (Xu et al., 2015; Wang et al., 2018; Yang et al., 2020). Especially in the Jurassic–Early Cretaceous period, a large number of alkaline rocks were developed as batholiths, stocks, or dykes (Wei et al., 2019). Their lithology was mainly syenite, syenite porphyrite, diorite porphyrite, diabase, and lamprophyre. The representative alkaline rocks are the Tongshi complex, Shagou complex, Chishan alkaline complex, and Longbaoshan alkaline complex. The Longbaoshan alkaline complex, with an area of 3.5 km², is exposed near the Wugou village of the Cangshan county. It is predominantly composed of quartz syenite, syenite, aegirine–augite syenite, and syenodiorite assemblages (Figure 1C). The NW-trending Longhui fault is the major structure in the study area, and its SN-, EW-, and NNE-trending secondary fracture and alteration zone are developed, controlling the distribution of the Longbaoshan complex and REE ore veins (Figures 1E,F). The Chishan alkaline complex covers an area of 0.5 km² and crops out in the Chishan village of the Weishan county. It mainly consists of quartz syenite, alkali granite, and aegirine quartz syenite (Figure 1D). The regional structure mainly comprises the NW-, NE-, SN-, and EW-trending faults. The Chishan complex extends in NE- and SW-trending controlled by the regional faults and contacts with gneiss in irregular branches. The REE ore veins occurred within the quartz and gneiss (Figures 1D,H).

2.2 Samples

In this study, five samples of quartz syenite (18CS-01, −10, −11, −12, and −33) and two samples of REE ore (18CS-05 and 18CS-18) were collected from the −160 m level of the Chishan REE deposit (Figures 1D,G,H). A total of five samples of porphyritic quartz syenite samples (LBS-01, -04, -06, -07, and -09) and two samples of alterated rock (P6D8h1 and P6D8h3) were collected from outcrops (Figures 1C,E,F) of the Longbaoshan alkaline complex. Petrographic observations, whole-rock geochemical, and Sr–Nd–Pb isotopic analyses were performed on all the samples. The zircon U-Pb dating and Hf isotopic analyses were conducted only on samples 18CS-01 and LBS-01.

The quartz syenite of the Chishan alkaline complex, with gray to light pink color, has generally porphyroid or porphyritic textures and a massive structure (Figure 2A). It consists mainly of K-feldspar (53 vol%), plagioclase (25 vol%), quartz (15 vol%), and hornblende (5 vol%). The K-feldspar grains have grain sizes of 1.0–1.5 mm and are subhedral columnar or granular, some of which show Carlsbad twinning (Figure 2B). The porphyritic quartz syenite of the Longbaoshan complex is generally gray to light pink in color and shows a porphyritic texture (Figure 2C). K-feldspar (1.0–2.5 mm), plagioclase (0.3–1.0 mm), and quartz (0.1–0.3 mm) phenocrysts are distributed in the groundmass (Figure 2D), while the matrix is dominated by K-feldspar, plagioclase, and quartz with sizes of 0.01–0.05 mm.

FIGURE 2

FIGURE 2. Photographs of the quartz syenite (A,B) from the Chishan complex and porphyritic quartz syenite (C,D) from the Longbaoshan complex. Abbreviations: Kfs = K-feldspar, Pl = plagioclase, and Qtz = quartz.

3 Analytical methods

3.1 Zircon LA-ICP-MS U–Pb dating

Zircon separation was conducted using standard density and magnetic separation techniques followed by hand-picking at Langfang Fengzeyuan Rock and Mineral Testing Technology Co., Ltd. (Langfang, China). The zircons grains were selected under a stereo-microscope, sealed in an epoxy resin target, and polished until the mid-sections were exposed. Cathodoluminescence (CL) transmitted and reflected images were taken prior to U–Pb dating analysis to identify the internal textures of zircon grains and select target spots with no cracks, no inclusions, and good growth zones for U–Pb dating and Hf isotopic analysis.

Zircon U–Pb dating was conducted at Beijing Createch Testing Technology Co., Ltd. (Beijing, China) using a Neptune multi-collector inductively coupled plasma mass spectrometry (MC-ICP-MS) equipped with a New Wave 193-nm laser sampler. The diameter of the laser beam was 35 μm, and the carrier gas was He. Detailed analytical processes were described by Yuan et al. (2004). The results were corrected with the measured ²⁰⁴Pb for U–Th–Pb isotopic fractionation and the presence of common Pb (from the measured ²⁰⁴Pb). The final data were processed with ICP-MS DataCal software (Liu et al., 2008). Zircon U-Pb concordia diagrams and mean ages were obtained with ISOPLOT 3.0 software (Ludwig, 2003).

3.2 Major and trace elements

The major and trace element concentrations were determined at Beijing Createch Testing Technology Co., Ltd. (Beijing, China). Fresh samples were crushed to less than 200 meshes. Major elements were analyzed by X-ray fluorescence spectrometry (XRF-1800), with an accuracy of better than 1%. Fused glass disks were prepared by mixing the samples with Li₂B₄O₇–LiBO₂ flux, with an automated fusion system. The trace elements were analyzed using the lithium borate melting method and determined by quantitative ICP-MS (Agilent 7500ce), with an accuracy of better than 5%.

3.3 Whole rock Sr–Nd–Pb isotopes

Whole rock Sr, Nd, and Pb isotopes were determined in Beijing Createch Testing Technology Co., Ltd. (Beijing, China) by using a Finnigan MAT 262 multi-channel thermal ionization mass spectrometer (TIMS). Samples were weighted into Teflon capsules along with ⁸⁴Sr, ⁸⁷Rb, ¹⁵⁰Nd, and ¹⁴⁷Sm isotopic spikes and then digested in HClO₄ and HF. The separation of lead was used as the conventional anionic resin-exchange technique with HCl. After ion exchange separation, the Sr–Nd isotope ratios were analyzed using a Finnigan MAT 262 thermal ionization mass spectrometer. The chemical analytical procedures were described by Pin et al. (2014).

The correction of Sr and Nd isotope ratios mass fractionation used were ⁸⁷Sr/⁸⁸Sr = 0.1194 and ¹⁴⁶Nd/¹⁴⁴Nd = 0.7219, respectively. The procedural blanks for Rb and Sr were <100 pg, and for Sm and Nd were <50 pg. The obtained standard results are as follows: NBS-987 ⁸⁷Sr/⁸⁶Sr = 0.710248 ± 13; GSB ¹⁴³Nd/¹⁴⁴Nd = 0.512185 ± 8. Repeated analyses of BCR-2 standard yielded the ratio of ²⁰⁶Pb/²⁰⁴Pb = 18.7477 ± 3, ²⁰⁷Pb/²⁰⁴ Pb = 15.6111 ± 3, and ²⁰⁸Pb/²⁰⁴Pb = 38.6921 ± 7, respectively, and all of them are within the error range (Yang et al., 2010).

3.4 Zircon Lu–Hf isotopes

The zircon Lu–Hf isotope analysis was proceeded on or close to the U-Pb dating spots at Beijing Createch Testing Technology Co., Ltd. (Beijing, China) using a Neptune MC-ICP MS system. The laser and mass spectrometry conditions are the same with the zircon U–Pb dating. Analytical conditions, instrument settings, and procedures were described by Geng et al. (2011). In this study, the adopted ¹⁷⁶Lu decay constant was 1.867×10⁻¹¹year⁻¹ (Söderlund et al., 2004), the ¹⁷⁶Hf/¹⁷⁷Hf ratio value of chondrite was 0.0332, and the ¹⁷⁶Lu/¹⁷⁷Hf ratio value was 0.282772 (Blichert-Toft and Albarède, 1997). Depleted mantle model ages (t_DM1) were calculated based on present-day depleted mantle ¹⁷⁶Lu/¹⁷⁷Hf and ¹⁷⁶Hf/¹⁷⁷Hf ratios (¹⁷⁶Lu/¹⁷⁷Hf = 0.0384, ¹⁷⁶Hf/¹⁷⁷Hf = 0.28325) (Griffin et al., 2000). The ¹⁷⁶Lu/¹⁷⁷Hf ratio of 0.015 (Griffin et al., 2002) was used to calculate the depletedmantlemodelage (t_DM2). The detailed analysis and calculation procedures were described by Wu et al. (2007).

4 Results

4.1 Zircon U–Pb dating

Zircon grains from sample 18CS-01 (quartz syenite) of the Chishan complex are dark in color and euhedral to short columnar in shape, with the sizes of 100–200 μm and aspect ratios from 1:2.5 to 1:1.25. The CL images show that most of the grains have smooth surfaces and oscillatory zoning, indicative of a magmatic origin (Figure 3A). Zircon grains from sample LBS-01 (porphyritic quartz syenite) of the Longbaoshan complex are light black to colorless. They are euhedral to subhedral and range in size from 50 to 150 μm, with aspect ratios of 1:1 to 1:2.5. In the CL images, most zircon grains also display obvious oscillatory zonation (Figure 3B).

FIGURE 3

FIGURE 3. (A,B) Cathodoluminescence (CL) images of representative zircon grains in sample 18CS-01 and LBS-01, showing analytical positions, ²⁰⁶Pb/²³⁸U ages, and ε_Hf(t) values. (C–F) U-Pb concordia diagram and weighted mean ²⁰⁶Pb/²³⁸U ages of zircons from Chishan and Longbaoshan complexes.

A total of 50 spots from two samples were analyzed in this study. In order to ensure the accuracy and reliability of the results, age data having the concordance below 90% in the ²⁰⁷Pb/²³⁵U-²⁰⁶Pb/²³⁸U plot were deleted. The adjusted data are listed in Table 1.

TABLE 1

TABLE 1. LA-ICP-MS zircon U–Pb isotope analyses of the quartz syenite from Chishan and Longbaoshan complexes.

Zircons from Chishan quartz syenite have ²³⁸U contents of 738–1672 ppm, ²³²Th concentrations of 157–1576 ppm, and ²³²Th/²³⁸U ratios of 0.18–1.01. The ²⁰⁶Pb/²³⁸U ages of all the analyzed zircons are concentrated and fall on the concordia line (Figure 3C) and yield a mean age of 126.2 ± 1.1 Ma (MSWD = 1.6) (Figure 3D), which is considered to be the crystallization age of the quartz syenite.

Zircons from Longbaoshan porphyritic quartz syenite have ²³⁸U contents of 194–601 ppm, ²³²Th concentrations of 224–641 ppm, and ²³²Th/²³⁸U ratios of 1.08–1.57. The ²⁰⁶Pb/²³⁸U ages of all the analyzed zircons fall on or near the concordia line (Figure 3E) and yield a mean age of 123.7 ± 0.7 Ma (MSWD = 1.1) (Figure 3F). It is suggested that the porphyritic quartz syenite was emplaced contemporaneous with the quartz syenite (18CS-01) in the Early Cretaceous.

4.2 Major and trace elements

Major and trace element contents and associated parameters of all samples from the Longbaoshan and Chishan complexes are listed in Table 2. The Chishan quartz syenite samples have SiO₂ contents of 69.02–71.72 wt%, A1₂O₃ contents of 13.51–16.12 wt%, and Na₂O, K₂O, and CaO contents of 5.53–7.13 wt%, 3.34–4.43 wt%, and 0.38–1.59 wt%, respectively. These samples are relatively high in SiO₂, total alkali (Na₂O + K₂O) and A1₂O₃ and low in TiO₂ (0.06–0.17 wt%). These samples are mainly classified as belonging to the alkaline series (Figure 4A), with an aluminum saturation index (A/CNK) of 0.83–0.98, showing a metaluminous to peralkaline characteristic (Figure 4B). They plot within the high-K field on the SiO₂ versus K₂O diagram (Figure 4C), mainly in the alkali-calcic field in the SiO₂ versus K₂O + Na₂O—CaO diagram (Figure 4D).

TABLE 2

TABLE 2. Whole-rock major and trace element compositions of the quartz syenite, REE ore samples, and alterated rocks from Chishan and Longbaoshan REE deposits.

FIGURE 4

FIGURE 4. Geochemical diagrams for the (porphyritic) quartz syenite analyzed in this study. (A) SiO₂ versus K₂O (after Middlemost, 1994. The dotted line of alkaline and subalkaline series from Irvine and Baragar, 1971); (B) A/CNK [molar ratio Al₂O₃/(K₂O + Na₂O + CaO)] versus A/NK [molar ratio Al₂O₃/(K₂O + Na₂O)] (after Maniar and Piccoli, 1989); (C) SiO₂ versus K₂O (after Peccerillo and Taylor, 1976); (D) SiO₂ versus K₂O + Na₂O—CaO (after Frost et al., 2001).

The Longbaoshan porphyritic quartz syenite samples have SiO₂ = 62.87–69.01 wt%, A1₂O₃ = 16.77–17.64 wt%, Na₂O = 6.61–6.89 wt%, K₂O = 5.02–5.21 wt%, and CaO = 0.16–1.49 wt%. On the total alkali versus silica (TAS) diagram (Figure 4A), the majority of these sample plots fall within the quartz monzonite field. As shown in the A/CNK versus A/NK diagram, these samples show a peraluminous to metaluminous affinity (Figure 4B). All the samples plot within the shoshonite field on the SiO₂ versus K₂O diagram (Figure 4C), and within the alkalic field on the SiO₂ versus K₂O + Na₂O—CaO diagram (Figure 4D).

The chondrite normalized REE patterns (Figure 5A) show that both the Chishan quartz syenite samples and Longbaoshan porphyritic quartz syenite samples show obvious REE fractionation and have the features of enrichment in light REEs (LREEs) and depletion in heavy REEs (HREEs). Moreover, they have similar REE components with total REE concentrations (ΣREE) of 255.2–1117.8 ppm, LREE/HREE ratios of 17.2–29.4, (La/Yb)_N values of 23.5–77.7, and Eu anomalies (δEu) of 0.77–0.98. On the primitive mantle-normalized trace element spider diagram (Figure 5B), they are characterized by enrichment in large-ion lithophile elements (LILEs, e.g., Rb, Ba, and Sr), depletion in high field strength elements (HFSEs, e.g., Nb and Ta), and positive Pb anomalies and negative Nd and Dy anomalies.

FIGURE 5

FIGURE 5. (A) Chondrite-normalized REE distribution pattern of the Chishan and Longbaoshan complexes (chondrite values after Sun and McDonough, 1989). (B) Primitive mantle-normalized spider diagram of the Chishan and Longbaoshan complexes (primitive mantle values after Sun and McDonough, 1989).

The Chishan REE ores and Longbaoshan altered rocks are highly enriched in REEs (ΣREE = 4067.5–77419.3 ppm), with LREE/HREE ratios of 17.3–121.6 and (La/Yb)_N values of 23.1–603.5. In the chondrite-normalized REE patterns (Figure 5A), these samples exhibit distinct REE fractionation and features of enrichment in LREEs and depletion in HREEs with mild negative Eu (δEu = 0.52–0.88) anomalies. On the primitive mantle-normalized trace element spider diagram (Figure 5B), they are characterized by exceeding enrichment in LILEs (Rb and Ba), depletion in HFSEs (Nb, Ta, Zr, and Hf), and negative Pb and Dy anomalies.

4.3 Whole rock Sr–Nd–Pb isotopes

The Sr–Nd–Pb isotopic analysis results are listed in Table 3. The Chishan quartz syenite samples have uniform initial (⁸⁷Sr/⁸⁶Sr)_i ratios (0.7062–0.7088) and negative ε_Nd(t) values (−12.9 to −9.3), whereas the Longbaoshan porphyritic quartz syenite samples have high initial (⁸⁷Sr/⁸⁶Sr)_i ratios (0.7083–0.7100) and lower ε_Nd(t) values (−14.6 to −13.6). The Chishan REE ore samples have similar initial (⁸⁷Sr/⁸⁶Sr)_i ratios (0.7073–0.7077) and ε_Nd(t) values (−9.3 to −8.8) to the quartz syenite, and the Longbaoshan altered rocks also have similar initial (⁸⁷Sr/⁸⁶Sr)_i ratios (0.7087–0.7089) and ε_Nd(t) values (−13.3 to −13.1) to the porphyritic quartz syenite.

TABLE 3

TABLE 3. Sr-Nd-Pb isotopic compositions of the quartz syenite, REE ore samples, and altered rocks from Chishan and Longbaoshan REE deposits.

The Chishan quartz syenite samples and the Longbaoshan porphyritic quartz syenite samples have coincident Pb isotope compositions with the (²⁰⁶Pb/²⁰⁴Pb)_t, (²⁰⁷Pb/²⁰⁴Pb)_t, and (²⁰⁸Pb/²⁰⁴Pb)_t ratios of 17.25–17.63, 15.41–15.51, and 36.25–37.84, respectively. The Chishan REE ore samples and Longbaoshan altered rocks also have similar Pb isotope compositions to the (porphyritic) quartz syenite samples ((²⁰⁶Pb/²⁰⁴Pb)_t =17.19 to 17.52, (²⁰⁷Pb/²⁰⁴Pb)_t = 15.44 to 15.53, and (²⁰⁸Pb/²⁰⁴Pb)_t =36.99–37.81).

4.4 Zircon Hf isotopes

The in situ Hf isotopic analysis results of the (porphyritic) quartz syenite are listed in Table 4. The results show that they have analogical ε_Hf(t) values. In total, five zircon grains from sample 18CS-01 yield ε_Hf(t) values from −15.8 to −13.2 (mean = −14.4) and Hf model ages (T_DM^C) of 2.07–2.19 Ga (mean = 2.09 Ga). In total, five zircon grains from sample LBS-01 yield ε_Hf(t) values of −17.9 to −13.8 (mean = −15.4) and T_DM^C of 2.06–2.32 Ga (mean = 2.16 Ga).

TABLE 4

TABLE 4. Zircon Hf isotopic compositions of the quartz syenite from Chishan and Longbaoshan complexes.

5 Discussion

5.1 Timing of magmatism

The zircon grains from the (porphyritic) quartz syenite exhibit growing oscillatory zoning (Figures 3A,B), which coupled with relatively high Th/U ratios (>0.2 and 1.0) (Table 1), indicate a magmatic origin. Therefore, the weighted mean ²⁰⁶Pb/²³⁸U ages of 126.2 ± 1.1 Ma and 123.7 ± 0.7 Ma can represent the emplacement ages of the syenitic rocks from the Chishan and Longbaoshan complexes, respectively.

The emplacement age of the Chishan quartz syenite agreed with the previously reported ages (122–126 Ma) of the alkaline complex within the error range (Liang et al., 2017; Wei et al., 2019; Ding et al., 2022). However, the obtained diagenetic age (123.7 ± 0.7 Ma) of the porphyritic quartz syenite is slightly less than the precious reported poorly defined Rb–Sr isochron age (129.3 Ma, Zhang et al., 2005) and LA-ICP-MS zircon U–Pb ages (129.4–131.7 Ma, Lan et al., 2011) of the Longbaoshan complex. The slight difference between the ages of this study and those of predecessors indicates that the Longbaoshan complex was formed in a magmatic activity lasting relatively for a long duration.

Comparing the emplacement ages of the quartz syenite and porphyritic quartz syenite, it is found that they are both formed in the late Early Cretaceous. There is a broad consensus that the NCC has undergone large-scale lithospheric thinning or destruction since the late Paleozoic (Zhai et al., 2002; Deng et al., 2003; Chen, 2010; Yang et al., 2018b), and the peak time of destruction and thinning was the Early Cretaceous (125–120 Ma) (Wu et al., 2005; Zhang et al., 2014; Zheng et al., 2018; Yang et al., 2020; Zhang et al., 2020; Zeng et al., 2022). Thus, the diagenesis time of the Chishan and Longbaoshan complexes is consistent with the peak period of the NCC destruction process.

5.2 Petrogenesis

5.2.1 Magma source

The spatial isolated Chishan quartz syenite and Longbaoshan porphyritic quartz syenite have the similar diagenetic ages, chemical characteristics, Sr–Nd–Pb isotopic and zircon Hf isotopic compositions, and normalized trace element and REE patterns, indicating that they may be of cogenetic origin.

The Chishan quartz syenite samples and Longbaoshan porphyritic quartz syenite samples have similar chemical characteristics of relatively high alkalis (Na₂O + K₂O = 7.62–10.94 wt%), high potassium (Na₂O/K₂O = 0.28–0.89) and metaluminous (A/CNK = 0.75–1.00), and low TiO₂ content (0.06–0.17 wt%). In the SiO₂ versus K₂O diagram (Figure 4C), all the sample plots fall within the high-K and shoshonite fields. The rocks display peraluminous to peralkaline features in the A/CNK versus A/NK diagram (Figure 4B). In the SiO₂ versus K₂O + Na₂O—CaO diagram (Figure 4D), all the sample plots fall within the alkalic and alkali–calcic fields. Therefore, they have the obvious characteristics of alkaline and metaluminous rocks.

The syenitic rocks from the Chishan and Longbaoshan complexes show similar REE and trace element patterns (Figure 5 and Table 2) with the characteristics of enrichment in LREEs and LILEs (Rb, Ba, Pb, and K) and depletion in HFSEs (Ti, Nb, and Ta), along with a slight negative Eu anomaly (Figure 5B). The chondrite-normalized REE patterns also display strongly fractionated LREE/HREE patterns (Figure 5A). Those chemical characteristics are almost the same as the mantle-derived mafic intrusions and volcanics in southeastern NCC during the Early Cretaceous (Zhang et al., 2002; Zhang et al., 2005; Lan et al., 2011).

The Chishan quartz syenite samples and Longbaoshan porphyritic quartz syenite samples have high initial ⁸⁷Sr/⁸⁶Sr ratios and low ε_Nd(t) values ((⁸⁷Sr/⁸⁶Sr)_i = 0.7062 to 0.7100 and ε_Nd(t) = −14.6 to −9.3), which are characteristics of the EM2-like character (Zhang et al., 2005; Lan et al., 2011). In the ε_Nd(t)–(⁸⁷Sr/⁸⁶Sr)_i diagram (Figure 6), all the sample plots fall near the mantle array despite the variations and fall within the subcontinental lithospheric mantle (SCLM), also suggesting a mantle origin. The (porphyritic) quartz syenite samples have low (²⁰⁶Pb/²⁰⁴Pb)_i (17.2–17.6), slightly high (²⁰⁷Pb/²⁰⁴Pb)_i (Δ7/4=15.4–15.5), and very high (²⁰⁸Pb/²⁰⁴Pb)_i (Δ8/4=36.5–37.8) (Table 3 and Figure 7), similar to the I-MORB and EM2-type rocks (Zhang et al., 2002, Zhang et al., 2005). In the Pb isotopic diagrams (Figure 7), majority of sample plots fall within the Mesozoic mafic rock field, suggesting that they have similar characteristics to the Mesozoic basalts and mafic intrusive rocks in the NCC (Zhang et al., 2002, Zhang et al., 2004). In addition, the (porphyritic) quartz syenite samples have similar (¹⁷⁶Hf/¹⁷⁷Hf)_i and ε_Hf(t) values (0.28219 to 0.28232 and −17.9 to −13.2, respectively) (Table 4), and in the Hf isotope diagram (Figure 8), all the sample plots fall above the 2.5 Ga continental crust evolutional line, as well as within the Mesozoic enriched SCLM field. Thus, it is reasonable to deduce that the (porphyritic) quartz syenites were derived predominantly from enriched lithospheric mantle (EM2-type).

FIGURE 6

FIGURE 6. Initial ⁸⁷Sr/⁸⁶Sr versus ε_Nd (t) diagram of the Chishan and Longbaoshan complexes. Isotopic data for ultrahigh pressure metamorphic rocks in the North Dabie (NDB) zone (from Dai et al., 2016), Mesozoic-enriched SCLM of the NCC (from Dai et al., 2016), Paleo-Pacific oceanic crust (from Hauff et al., 2003), Mesozoic alkali-rich intrusive rocks near the TLFZ in northern Yangtze Craton (from Yan et al., 2008), and the EM1-type rocks and EM2-type rocks in the Luxi Block (from Zhang et al., 2004, Zhang et al., 2005; Lan et al., 2011).

FIGURE 7

FIGURE 7. Diagrams of ²⁰⁷Pb/²⁰⁴Pb versus ²⁰⁶Pb/²⁰⁴ Pb (A) and ²⁰⁸Pb/²⁰⁴Pb versus ²⁰⁶Pb/²⁰⁴Pb (B) for the Chishan and Longbaoshan complexes. Data are also plotted for Mesozoic-enriched SCLM of the NCC (from Dai et al., 2016), Dabie-Sulu UHP eclogites and gneisses (from Yang K. F. et al., 2012), Mesozoic mafic rocks in the NCC (from Li and Yang, 2003) and the EM1-type rocks and EM2-type rocks in the Luxi Block (from Zhang et al., 2005; Lan et al., 2011).

FIGURE 8

FIGURE 8. ε_Hf(t) versus U-Pb age diagram of zircons from the quartz syenite at the Chishan and Longbaoshan complexes. (Data for the enriched NCC mantle are from Yang et al., 2006; Lan et al., 2013).

Previous studies have revealed that the mafic intrusions and volcanic rocks that formed in the Early Cretaceous in southeastern NCC were originated from a mantle domain of arc-like and isotopically enriched (Wu et al., 2017; Dai et al., 2019; Ding et al., 2022). The (porphyritic) quartz syenite samples are characterized by low Nb/Th (0.52–1.95), Nb/La (0.09–0.85) ratios, relatively higher La/Nb (1.00–26.76), Th/Ta (12.39–148.65), Ba/Nb (9.90–239.12) ratios, and negative Nb–Ta anomalies, which are similar to the sub-continental mantle-derived magma contaminated with crustal material (Santosh et al., 2016; Yang et al., 2018b). Moreover, this is also well-demonstrated by the Nd and zircon Hf model ages (t_DM2 of 1633–2048 Ma and T_DM^C from 2060 Ma to 2315 Ma, Tables 3, 4), which indicates variable proportions of the Paleoproterozoic crustal material. The crustal source is predominantly a reworked Paleoproterozoic crustal zone originating from the Yangtze Craton (Deng et al., 2018). In the La/Nb versus Ba/Nb diagram (Figure 9A), most of the syenitic sample plots fall within the arc volcanic field, indicative of the similar mantle source of the subducted mantle wedge (Lan et al., 2011). Furthermore, these samples have high (Hf/Sm)_N and relative low (Ta/La)_N ratios which are identical to the Jinan gabbros in the Luxi Block (Figure 9B), suggesting that this enriched mantle source may be related to subduction metasomatism (Lan et al., 2011). In addition, these isotopic compositions of the (porphyritic) quartz syenite are consistent with the Fangcheng basalts and mafic rocks in this region, which were considered to be originated from a lithospheric mantle highly reformed by subducted crust melts (Zhang et al., 2002; Xu et al., 2004; Yang K. F. et al., 2012). Thus, we propose that the (porphyritic) quartz syenites are also derived from lithospheric mantle, which is reformed by the SCLM melts.

FIGURE 9

FIGURE 9. (A) La/Nb versus Ba/Nb diagram for the Chishan and Longbaoshan complexes. The fields of MORB, PM, OIB, Dupal OIB, continental crust (CC) average, and arc volcanics are referred to Jahn et al. (1999). (B) (Ta/La)_N versus (Hf/Sm)_N diagram for the Chishan and Longbaoshan complexes. The trends of the subduction- and carbonatite-related metasomatism are from La Flèche et al. (1998). (C) SiO₂ versus lg (CaO/(K₂O + Na₂O)) discrimination diagrams of the quartz syenite from the Chishan and Longbaoshan complexes (after Pearce, 1996). (D) Nb_N versus Th_N diagrams for the Chishan and Longbaoshan complex (after Saccani, 2015).

5.2.2 Genetic model and process

Three models have been suggested for the generation of syenitic rocks: 1) partial melting of crustal rocks (Miyazaki et al., 2000; Martin, 2006) or an over-thickened crust (Tchameni et al., 2001); 2) partial melting of the enriched mantle or metasomatized mantle (Litvinovsky et al., 2002) or differential evolution of alkalic basaltic magma (Macdonald and Scaillet, 2006); 3) mixing of silica-undersaturated alkaline or mafic magmas derived from the mantle with granitic magmas derived from the lower crust (Zhao et al., 1995; Jung et al., 2007). Based on the aforementioned discussion, we consider that the origin of the (porphyritic) quartz syenite from the Chishan and Longbaoshan complexes should follow the second model. They derived from the lithospheric mantle converted by SCLM melts.

However, for the rocks formed by partial melting in the mantle source area, two main mechanisms have been proposed to reveal the reformation of lower crust materials: 1) the direct transformation of the magma source area by delaminated continental crust materials; 2) the assimilation or contamination of the crustal materials in the magma ascending process (Yang D. B. et al., 2012). In the ε_Nd(t)-SiO₂ and (⁸⁷Sr/⁸⁶Sr)_i-SiO₂ diagrams (Figure 10), the initial ⁸⁷Sr/⁸⁶Sr ratios and ε_Nd(t) values have no significant changes with the increase of SiO₂ contents, which is consistent with the evolution trend of fractional crystallization, manifesting that the assimilation of continental crust materials may have occurred principally in the magma chamber (Zhang et al., 2005; Lan et al., 2011). Therefore, we conclude that the alkaline magma derived from the enriched lithospheric mantle was unevenly assimilated by melts derived from the continental crust in the magma chamber and then produced the parent magma of the (porphyritic) quartz syenites.

FIGURE 10

FIGURE 10. Diagrams of initial ⁸⁷Sr/⁸⁶Sr ratio versus SiO₂ (A) and ε_Nd(t) value versus SiO₂ (B) for the Chishan and Longbaoshan complexes.

Through the aforementioned discussion, the formation process of the (porphyritic) quartz syenite can be summarized as follows: before 130 Ma, the lithospheric mantle under the southeastern part of the Luxi Block reformed by the SCLM melts and transformed from EM1-type into EM2-type in response to the subduction of the Yangtze continental crust (Figure 11A) (Zhang et al., 2002, Zhang et al., 2004; Lan et al., 2011). At ∼130 Ma, due to subduction of the Paleo-Pacific plate, the converted EM2-type lithospheric mantle was partially melted and produced potassium-rich alkaline magma marked by enrichment of LREEs and LILEs and depletion of HFSEs (Figure 11B) (Zhang et al., 2002; Zhang et al., 2004, Zhang et al., 2005). This magma assimilated the crust-derived melts and were up-invaded with the lithospheric thinning and asthenosphere mantle upwelling, forming the Chishan and Longbaoshan alkaline complexes (Figure 11C).

FIGURE 11

FIGURE 11. Simplified genetic model cross-sections of quartz syenite (modified after Zhu and Xu, 2019; Deng et al., 2020; Ding et al., 2022). (A) Trassic subduction of the Yangtze Craton. (b) Early Cretaceous subduction of the Paleo-Pacific plate. (C) Early Cretaceous lithospheric thinning and destruction of the NCC.

5.3 Tectonic setting

All the studied syenitic rocks from the Chishan and Longbaoshan complexes have an arc-like affinity with enriched LREEs and LILEs (e.g., Ba and Th) and depleted HFSE (e.g., Nb and Ta). This can be further evidenced by the La/Nb versus Ba/Nb diagram (Figure 9A), in which most syenitic samples plot within the arc volcanic field. In addition, the high (Hf/Sm)_N and low (Ta/La)_N ratios (Figure 9B) of these samples suggest that the enriched mantle source may be associated with subduction metasomatism (La Flèche et al., 1998; Lan et al., 2011). Nevertheless, it is noteworthy that the syenitic samples plot within the extensional alkaline-calc-alkaline field in the lg (CaO/(K₂O + Na₂O)) versus SiO₂ discrimination diagram (Figure 9C) and plot within the fields of divergent plate and within-plate settings in the Nb_N versus Th_N discrimination diagram (Figure 9D), implying an extensional tectonic setting (Wei et al., 2019; Ding et al., 2022). Moreover, the paleostress regimes reconstructed results of the Jiaolai Basin based on the effective fault-slip data and fold hinge data inversion showed that it has experienced E–W extension (135–121 Ma) and NW–SE extension (120–93 Ma) since the Cretaceous (Zhang et al., 2020). The study on the structural geology, paleomagnetism, and gravity modeling of Fengjiayu–Xibailianyu and Gubeikou plutons revealed that the NCC was also in a NW–SE trending extensional tectonics during 130–110 Ma with severe extension after ca. 127 Ma (Zeng et al., 2022).

Numerous studies have shown that the NCC was in an extensional tectonic environment during the Mesozoic and underwent craton destruction and extensive lithospheric thinning indicated by intense magmatism (Zhai et al., 2002; Deng et al., 2003; Yang et al., 2007). It has already been confirmed that the Early Cretaceous was a peak period for NCC destruction and lithospheric thinning (Wu et al., 2005; Zheng, 2009; Goss et al., 2010) due to the rollback and retreat of subducting the Paleo-Pacific plate (Santosh, 2010; Zhu et al., 2012). In the early Mesozoic, the Paleo-Pacific plate subducted in a low angle along the continental margin of the eastern NCC and showed an important impact on the destruction and thinning of the latter continental lithosphere (Xu et al., 2012; Zheng et al., 2018; Zhu and Xu, 2019). It has been proposed that the angle of subduction gradually increased with the rollback and retreat of the subduction zone during the Early Cretaceous (Zhu and Xu, 2019). The transition of subduction angle may have occurred at ca. 140 Ma (Wu et al., 2005; Zhang et al., 2014; Zhao et al., 2017). In addition, partial melting of the SCLM as well as the destruction and extension of the lithosphere was also caused during this process (Zhu et al., 2012; Yang et al., 2021).

5.4 Relationship between quartz syenite and REE mineralization

It is widely accepted that REE mineralization is genetically relevant to mantle-derived carbonatite-alkaline magmatism (Goodenough et al., 2016; Smith et al., 2016; Liu et al., 2019; Fan et al., 2020; Xie et al., 2020). At Chishan and Longbaoshan, the REE mineralization generally occurred within quartz syenite and porphyritic quartz syenite, which were under the control of NW- and NE-trending faults and NNE- and NE-trending faults, respectively. Preciously published Rb–Sr isochron ages and ⁴⁰Ar-³⁹Ar and U–Th dating results have yielded ages of 110–124 Ma of the REE mineralization (Tian et al., 2002; Lan et al., 2011; Ding et al., 2022), which are generally consistent with diagenetic ages of the syenitic rocks in this study. Actually, this age difference is basically consistent with the age error for magmatic hydrothermal deposits (Li et al., 1992; Tan et al., 2006). This spatial and temporal distribution consistency of the syenitic rocks and REE indicates that the mineralization has a certain genetic relationship with these alkaline rocks (Tian et al., 2002; Yu et al., 2010, 2014; Lan et al., 2011; Wei et al., 2019).

The aforementioned conclusions are also demonstrated by the geochemical and Sr–Nd–Pb isotopic characteristics of the syenitic rocks, REE ores, and altered rocks. The Chishan REE ores and Longbaoshan altered rocks are characterized by enrichment of LREEs and LILEs and depletion of HFSEs, which is similar to those of the syenitic rocks. From the chondrite-normalized REE patterns (Figure 5A), it can be seen that the REE distribution curve shapes of the Chishan REE ores and Longbaoshan altered rocks are basically similar to those of syenitic rocks. They all show a right-inclined distribution pattern, indicating that they have the characteristics of evolutionary inheritance. Furthermore, the Chishan REE ores and Longbaoshan altered rocks have similar Sr–Nd–Pb isotopic compositions to the syenitic rocks (Table 3; Figures 6, 7), indicating that the Chishan REE ores and Longbaoshan altered rocks have identical material sources with the syenitic rocks which were originated from the enriched mantle. Moreover, the in situ Nd isotopic compositions from single minerals of bastnasite and monazite at the Chishan REE deposit also suggested that the REE was derived from the enriched lithospheric mantle (Lan et al., 2011), which is also identical to that of the syenitic rocks.

Some studies have shown that the sources of ore-forming materials of Bayan Obo and Maoniuping REE deposits are closely related to those of the enriched mantle (Hou et al., 2009; Xie et al., 2009; Yang et al., 2009), indicating that the enriched mantle should be the source area of REE deposits. It has been suggested that melt-enriched LREE were derived from an enriched mantle metasomatized by REE- and CO₂-rich fluids that were released from subducted marine sediments (Walter et al., 2008; Yang et al., 2011; Hou et al., 2015; Liu et al., 2015; Ding et al., 2022).

In summary, based on the similar diagenetic/metallogenic ages, Sr–Nd–Pb isotopic compositions, and direct coexistence in space, we propose that the REE minerals have a genetic relationship with the syenitic rocks and they are homologous products, and the mineralization shows inheritance to the magmatic hydrothermal evolution.

6 Conclusion

1) LA-ICP-MS zircon U-Pb dating indicated that the diagenetic ages of the Chishan quartz syenite and Longbaoshan porphyritic quartz syenite were 126.2 ± 1.1 Ma and 123.7 ± 0.7 Ma, respectively, which belong to the Early Cretaceous and correspond to the peak period for NCC destruction and lithospheric thinning.

2) Geochemical and Sr–Nd–Pb–Hf isotopic characteristics suggest that the Chishan quartz syenite and Longbaoshan porphyritic quartz syenite have the identical material source of an EM-2 type lithospheric mantle that was modified by SCLM melts while the Yangtze block subducted.

3) The Chishan quartz syenite and Longbaoshan porphyritic quartz syenite show an arc affinity, implying in an extensional tectonic setting associated with rollback and retreat of the subducting Paleo-Pacific plate.

4) Based on the similar diagenetic/metallogenic ages, Sr–Nd–Pb isotopic compositions, and direct coexistence in space, we propose that the quartz syenite and the REE ore-forming material are homologous products. The REE mineralization shows inheritance to the magmatic hydrothermal evolution.

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

PW, DL, and ZS conceived this research. PW wrote the manuscript and prepared the figures. DL, ZS, and KG reviewed and edited the draft. QL, KG, YZ, and CD participated in field investigation. ZL, NC, WX, and CZ analyzed the data. All authors finally approved the manuscript and thus agreed to be accountable for this work.

Funding

This study was financially supported by the National Natural Science Foundation of China (Grant Nos. 42272104, 42172094, 41372086, 41672084, and 41772076), Natural Science Foundation of Shandong Province (Grant Nos. ZR2020QD028, ZR2020QD031, ZR2018QD002, and ZR2020MD032), Geological Exploration Project of Shandong Province (Grant Nos. LKZ (2020) 7, LKZ (2021) 7, LKZ (2022) 9), and a special fund for “Taishan scholars” project in the Shandong province.

Acknowledgments

We would like to express our thanks to the reviewers who offered constructive and valuable comments to improve the manuscript.

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.

Publisher’s note

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