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Article

Geochronology, Geochemistry, and Geodynamic Relationship of the Mafic Dykes and Granites in the Qianlishan Complex, South China

by
Zhi-Feng Yu
1,2,
Qi-Ming Peng
1,3,
Zheng Zhao
2,*,
Ping-An Wang
2,
Ying Xia
4,
Yu-Qi Wang
1,2 and
Hao Wang
5
1
School of Earth Sciences and Resources, China University of Geosciences (Beijing), Beijing 100083, China
2
MLR Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing 100037, China
3
China Mining Association, Beijing 100029, China
4
College of Earth Sciences, Chengdu University of Technology, Chengdu 610059, China
5
China Tungsten & Hightech Materials Co., LTD, Zhuzhou 430200, China
*
Author to whom correspondence should be addressed.
Minerals 2020, 10(12), 1069; https://doi.org/10.3390/min10121069
Submission received: 3 November 2020 / Revised: 25 November 2020 / Accepted: 26 November 2020 / Published: 29 November 2020
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Abstract

:
The Qianlishan complex, located in Hunan Province of South China, is closely associated with intense W-dominated polymetallic mineralization. The Qianlishan complex is composed of three phases: the main-phase porphyritic and equigranular granites, granite porphyry, and mafic dykes. Geochronologically, the zircon U-Pb dating results show that the porphyritic and equigranular granites have ages of approximately 159 and 158 Ma, respectively, similar to those of mafic dykes (approximately 158 Ma), while the granite porphyry was formed later at approximately 145 Ma. Geochemically, the mafic dykes are characterized by calc-alkaline high-Mg andesite (HMA) with high MgO, TiO2, Mg#, and CA/TH index. They exhibit significantly depleted εNd(t) and εHf(t) with high Ba/La, La/Nb, and (La/Yb)N, indicating that they formed from mixing melts of depleted asthenospheric mantle and metasomatized subcontinental lithospheric mantle (SCLM). The main-phase granites are peraluminous and are characterized by high SiO2, low (La/Yb)N ratios, and relative depletion in Ba, Sr, Ti, and Eu. They also display negative correlations between La, Ce, Y, and Rb contents, suggesting that they are highly fractionated S-type granites. Furthermore, they show high εNd(t) and εHf(t), CaO/Na2O ratios, HREE, and Y contents, indicating that they were produced by parental melting of ancient basement mixed with mantle-derived components. In contrast, the granite porphyry shows A-type signature granites, with higher εNd(t) and εHf(t) and CaO/Na2O ratios than the main-phase granites but similar Zr/Nb and Zr/Hf ratios to the mafic dykes, suggesting that they are the products of partial melting of a hybrid source with ancient basement and the mafic dykes. We thus infer that the slab roll-back led to generation of Qianlishan back-arc basalt and HMA and further triggered the formation of the Qianlishan granite.

1. Introduction

South China is famous for its extensive and intensive Mesozoic W-dominated polymetallic mineralization [1], which is closely related to Mesozoic granites, and these granites were interpreted as the result of partial melting of crustal anatexis with possible contamination of country rocks [2,3,4]. The tectonic setting of the voluminous granitic activities is a subject of much debate, diversely interpreted as collision of the South China and Indochina Blocks [5,6,7] or subduction of the paleo-Pacific plate beneath the South China Plate [8,9,10]. These models suggest that the extensive magmatism generated bimodal volcanism [11], adakitic rocks [12], mafic and ultramafic rocks [13], and granitoids [7,14] within South China.
Recently, a growing dataset of Mesozoic granites in the Nanling region suggests that mantle-derived components might be involved in their sources [15,16,17,18]. These granites have relatively depleted εNd(t) (−6.7 to −3.3) with Nd model ages (e.g., 1.2–1.5 Ga [19]). Especially, the granites of 160 to 156 Ma age in the Qianlishan complex display a wide range of εHf(t) (e.g., −9.25–+0.13), indicating a hybrid source of crust which involved a mantle-derived component [20]. Therefore, studying the mafic rocks in the Qianlishan complex to manifest the potential relationship between generation of these granites and mafic rocks is an appealing prospect.
The Qianlishan complex shows a close relationship with polymetallic mineralization of the giant Shizhuyuan W–Sn polymetallic deposit, as the ore-body occurs in the contact zone between the Qianlishan granites and the argillaceous banded limestone [21,22,23]. The mafic dykes are also exposed in the Qianlishan complex that hitherto lacked detailed age constraints. Previous studies were mainly focused on the mineralogy, petrology, and geochemistry of the Qianlishan granites [21,22,23,24,25,26]. Therefore, the study of geochemical and geochronological characteristics on Qianlishan mafic dykes and the Qianlishan granites may offer an opportunity to explain the mantle contribution of the granites and the possible deep mantle process that generated the mafic dykes and associated granites. In this study, we report whole rock geochemical and Hf-Nd isotope data along with zircon U-Pb geochronology data of granites and mafic dykes of the Qianlishan complex. These new data, in combination with previously published data for mafic dykes [20], allow for a new interpretation of the petrogenesis and geodynamic setting of the Qianlishan complex.

2. Geological Setting

South China is composed of the Yangtze Block in the northwest and the Cathaysia Block in the southeast (Figure 1), where they are separated by the northeastern part of Jiangshan-Shaoxing suture (J-S suture) [27]. The two blocks were amalgamated during the Neoproterozoic era [13,28]. The Nanling region includes southern Jiangxi, southern Hunan, northern Guangdong, and eastern Guangxi Provinces.
Strata exposed in the Nanling region mainly include weakly metamorphosed Precambrian sandstone. They are overlain by Paleozoic and lower Mesozoic mudstone or sandstone of shallow marine origin [18,29]. The Nanling region has experienced multiple tectonic events (e.g., Indosinian, 251–205 Ma and Yanshanian, 180–67 Ma), resulting in the formation of E-W strike-slip fault systems and N-E thrust fault systems controlling regional-scale magmatic activities (Figure 1). The sedimentary cover and basement have been subjected to strong intracontinental deformation under the influence of the Indosinian orogeny, forming Indosinian granites (251–205 Ma [14,18]). Subsequently, the tectonic environment of the Nanling region was dominated by the Yanshanian orogeny, generating abundant calc-alkaline granites [30,31]. Numerous W-Sn deposits were formed during these orogenic activities in the Nanling region (180–142 Ma [7,32]). Spatially, many of these deposits are associated with widespread Mesozoic granitic intrusions. Tungsten and tin mineralization usually occur along the contact zones between the granitic intrusions and the sedimentary strata and are hosted in both Devonian to Permian sedimentary rocks and in granitic rocks. The field relations suggest that W-Sn deposits in this region are essentially coeval with the host Mesozoic granites [33,34,35].
Moreover, numerous mafic rocks have been recorded in South China. Previous studies suggest natures of these mafic rocks. For example, the Devonian (approximately 365 Ma) and Carboniferous (approximately 340 Ma) basalts mainly derived from an enriched lithospheric mantle and OIB-type asthenosphere, respectively [36], Permian basalt and diabase (260–250 Ma) of South China [37,38], and Mesozoic mafic rocks are high-Mg andesite (HMA) (approximately 159 Ma) and are derived from an ancient metasomatized lithospheric mantle [39].

3. Qianlishan Complex Petrography

The Qianlishan complex is composed of the main-phase granites (porphyritic granites and equigranular granites), the granite porphyry, and the mafic dykes (Figure 2).
The porphyritic granite shows a white or light gray color (Figure 3a) and mainly consists of euhedral quartz (30–35%, 0.5–3 cm), megacrystic perthitic K-feldspar (30–35%, 0.5–5 cm), albite (25–30%), and minor muscovite (0–6%, 0.2–0.5 mm, Figure 4a). Accessory minerals include zircon, apatite, titanite, monazite, and ilmenite [40]. Pegmatite and greisen sometimes occur in the contact zone between these granites and the limestone. Most of the pegmatite form banded pegmatitic edges of 10–30 cm in the contact zone at the top of the granite (Figure 3a), and minor pegmatite is distributed into the granite forming pegmatitic schlieren (Figure 3b), which is composed of coarse-grained feldspar and quartz with associated aplite (Figure 3c). The equigranular granite mainly consists of K-feldspar (40%, 0.5–3 cm), quartz (30%, 0.5–2 cm), albite (25%), and minor muscovite (3%, 0.2–0.5 mm), with accessory topaz, wolframite, and zircon (Figure 4b,c). Skarn is formed in the contact zone of the main-phase granites and limestone. Massive W-Sn-Bi-Mo mineralization is present within skarn and is sometimes accompanied by cryptoexplosive breccia (Figure 3f).
In the south of the Qianlishan granites, there are many NE-trending granite porphyry dykes that intruded into main-phase granite (Figure 2 and Figure 3c). The dykes are approximately 1–4 km long and 0.2 km wide. Phenocrysts are mainly coarse-grained K-feldspar and quartz with minor plagioclase and grain sizes commonly over 3 cm. The groundmass is a fine-grained granitic structure, and accessory minerals include zircon, apatite, titanite, fluorite, and pyrite (Figure 4d,e [40]).
The mafic dykes mostly intrude into granite or Devonian strata and are generally 20 cm to several meters wide (Figure 3d,f). They are gabbroic and show an amygdaloidal structure consisting of phenocryst (10%) and matrix (90%). The phenocryst is composed of plagioclase and augite (Figure 4f). The groundmass is slender tabular plagioclase (55%), augite (25%), amphibole (10%), and minor biotite.

4. Analytical Methods

4.1. In Situ Zircon U–Pb Isotopic Analyses

Three granite samples (SZY1, SZY4, and SZY6) and one mafic dyke (SZY9) sample from the Qianlishan complex were collected for zircon U-Pb dating. Zircons were separated by conventional heavy-liquid and magnetic techniques at the Special Laboratory of the Geological Team in Langfang, Hebei Province, China. Cathodoluminescence (CL) images were taken using a HITACHI S-3000N scanning electron microscope fitted with a Gatan Chroma CL imaging system at the National Research Center for Geoanalysis (NRCG), Chinese Academy of Geological Sciences, Beijing, China.
U-Pb zircon isotopic analyses were perform with use of LA-ICP-MS, using an Agilent 7500a ICP-MS equipped with a UP193SS laser ablation system at the MLR Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing, China. A laser spot of 36 μm was used for analysis, and a Harvard zircon 91500 standard with a recommended 206Pb/238U age of 1065.4 ± 0.6 Ma was used for external standardization [41]; this standard was analyzed after every four unknown zircon analyses. Corrections for common Pb were made following the approach of Andersen [42], and data were processed using the GLITTER and ISOPLOT programs [43]. All reported ages are based on 238U/206Pb calculated as weighted means with errors at the 95% confidence level. More details of the analytical procedure are provided in Black et al. [44].

4.2. In Situ Zircon Hf Isotopic Analyses

In situ zircon Hf-isotope analyses were performed at the same sites or in the same age domains (identified using CL images) as the zircon U-Pb analyses. The analyses were performed using a Neptune MC-ICP-MS equipped with a GeoLas 200M ArF excimer 193-nm laser ablation system at the same laboratory as the zircon U-Pb analyses. The detailed analytical technique is described in Wu et al. [45]. A 44-μm laser spot size was selected during the ablation with a repetition rate of 8 Hz at 15 J/cm2. 175Lu/176Lu of 0.02655 was used for elemental fractionation correction [46]. Isobaric interference of 176Yb on 176Hf was corrected using the mean fractionation index proposed by Iizuka and Hirata [47] and a 176Yb/172Yb ratio of 0.5886 [48]. Repeated measurements on the Mud Tank zircon standard yielded a mean 176Hf/177Hf ratio of 0.282506 ± 11 (2σ, n = 177), which is consistent with the standard reference value of 0.282500 within error [45].

4.3. Whole-Rock Geochemical Analyses

Samples were collected for whole-rock geochemical analyses which were performed at the NRCG, Beijing, China. The major elements were determined by X-ray fluorescence (XRF model PW 4400), with analytical uncertainties ranging from 1% to 3%. Loss on ignition was obtained using about 1 g of sample powder heated at 980 °C for 30 min. The trace elements were analyzed by an Agilent 7500ce inductively coupled plasma mass spectrometer (ICP-MS). About 50 mg of powder was dissolved for about 7 days at approximately 100 °C using HF-HNO3 (10:1) mixtures in screw-top Teflon beakers, followed by evaporation to dryness. The material was dissolved in 7 N HNO3 and taken to incipient dryness again and then was redissolved in 2% HNO3 to a sample/solution weight ratio of 1:1000. The analyses of the international standards (GSR-3) were in good agreement with the recommended values [49]. Trace and rare earth elements were analyzed with analytical uncertainties of 10% for elements with abundances < 10 ppm and approximately 5% for those with >10 ppm. The detailed analytical procedures were similar to those described by Luo et al. [50].
Nd isotopic compositions of the 11 samples (eight granites and three mafic dykes) were measured using an MAT262 mass spectrometer at Nanjing Focus Technology Co. Ltd. For calculation of εNd(t) values, Nd model ages and adopted parameters were as follows: decay constant for 147Sm was 6.54 × 10−12 per year; 147Sm/144Nd ratio of chondritic uniform reservoir (CHUR) was 0.1967; 143Nd/144Nd ratio of CHUR was 0.512638; 147Sm/144Nd and 143Nd/144Nd ratios for depleted mantle (DM) were 0.2136 and 0.513151, respectively; and a 147Sm/144Nd ratio of 0.12 was used for average continental crust. The measurement procedures were the same as described by Zhu et al. [51].

5. Results

5.1. Zircon U-Pb Geochronology

Three granite samples from the Qianlishan granites and one mafic dyke sample were selected for zircon U-Pb dating (sampling positions are shown in Figure 2), and the data are listed in Supplementary Table S1.
Zircons from the main-phase granites are typically euhedral to subhedral with varying crystal length (80–150 μm) and an aspect ratio of 1:1 to 3:1 (Figure 5a,b). They show clearly homogeneous oscillatory zoning patterns, indicating that they are magmatic in origin [52]. The concentrations of Th and U are 92–600 and 178–2353 ppm, respectively, and the Th/U ratios are 0.27–0.65 (Supplementary Table S1). Analyses for 20 zircons from SZY1 samples yielded zircon U–Pb weighted mean ages of 158.9 ± 1.1 Ma (MSWD = 0.45) and 15 zircons from the SZY4 sample yielded zircon U–Pb weighted mean ages of 157.8 ± 1.4 Ma (MSWD = 0.77) (Figure 5a,b).
Zircons from the granite porphyry (SZY6) can be distinguished from those of the main-phase granites by their smaller sizes (60–120 μm) and show weak luminescence in CL images (Figure 5c). The concentrations of Th and U are 121–986 and 238–1773 ppm, and the Th/U ratios are 0.33–0.60 (Supplementary Table S1). Analyses for 20 zircons from SZY6 samples yielded zircon U–Pb weighted mean ages of 144.5 ± 1.0 Ma (MSWD = 1.24).
Zircons of SZY9 samples are from the mafic dykes. They are mostly up to 50–100 μm in size and have length to width ratios of between 1:1 and 2:1 (Figure 5d). Most zircons are clear, simple prismatic crystals without obvious zoning on CL images. The concentrations of Th and U are 100–282 and 137–428 ppm, and the Th/U ratios are 0.51–0.98 (Supplementary Table S1). Analyses for nine zircons from SZY9 samples yielded zircon U-Pb weighted mean ages of 157.6 ± 1.8 Ma (MSWD = 0.78).

5.2. Zircon Hf Isotopes

The zircon Hf isotopic data are listed in Supplementary Table S2. The Hf isotopic analyses for 20 zircon grains from the main-phase porphyritic granites yielded εHf(t) values from −8.3 to +0.7. Analyses of 12 zircons from the main-phase equigranular granites resulted in εHf(t) values in the range of −7.4 to −0.3. Analyses of 20 zircons from the granite porphyry yielded εHf(t) values in the range of −6.3 to +3.9, higher than those of the main-phase granites. Analyses of eight zircons from the mafic dykes gave εHf(t) values in the range of −4.4 to +4.3 (Figure 6).

5.3. Whole-Rock Geochemical Results

The rocks have varying loss on ignition (LOI) contents that range from 0.84 to 4.80 wt.%. These results, in combination with field and petrographic observations, suggest that these rocks underwent varying degrees of alteration. However, large ion lithophile elements (LILE; e.g., Rb and La) are correlated with high field strength element (HFSE; e.g., Th and Nb) in these samples, indicating that these elements were not disturbed significantly by alteration. The whole-rock geochemical data are listed in Supplementary Table S3.
The main-phase porphyritic granites are characterized by high SiO2 (72.16–75.63 wt.%), low MgO (0.09–0.32 wt.%), and P2O5 (0.02–0.05 wt.%). In addition, these samples are high-K highly fractionated calc-alkalic series (K2O = 5.68–6.41 wt.%) and belong to peraluminous granites as indicated by the aluminum saturation index (A/CNK = 1.31–1.38; Figure 7). These granites show flat rare earth element (REE) patterns with (La/Yb)N = 1.21–1.36 and are enriched in LILE, exhibiting significantly negative Sr, Ba, Eu, and high field strength element (HFSE) anomalies (Figure 8). The main-phase equigranular granites display similar geochemical characteristics to the porphyritic granites, including SiO2 (74.67–75.45 wt.%), MgO (0.01–0.02 wt.%), P2O5 (0.02–0.03 wt.%), K2O (3.33–4.85 wt.%), and A/CNK (1.43–1.93) of major elements. They also belong to high-K highly fractionated calc-alkalic and peraluminous granites (Figure 7). Moreover, They also show flat REE patterns with (La/Yb)N = 1.67–1.87 and display more significantly negative Sr, Ba, Eu, and HFSE anomalies (Figure 8). In summary, the main-phase granites of the Qianlishan complex are peraluminous high-K highly fractionated calc-alkalic granites.
The granite porphyry exhibits similar geochemical characteristics to major elements as main-phase granites, suggesting that it is high-K and peraluminous granite (Figure 7). However, they show lower Na2O + K2O (4.59–7.53 wt.%) contents and higher MgO + FeO + TiO2 (2.21–16.25 wt.%) contents than those in main-phase granite, suggesting that they belong to Alkalic granite but not the highly fractionated granite (Figure 7). In addition, the geochemical characteristics of trace elements of the granite porphyry are enriched in LREE, with (La/Yb)N = 2.85–16.10, and show indistinct Sr, Ba, Eu, and HFSE anomalies compared to the main-phase granites (Figure 8). Therefore, the granite porphyry in Qianlishan granites consist of peraluminous high-Kalkalic granites.
The mafic dykes are characterized by high MgO (8.28–9.13 wt.%), Cr (527.09–791.36 ppm), and Ni (113.98–224.98 ppm) contents and Mg# (>60), which shows affinity to primitive andesite [58]. They are enriched in LREE with (La/Yb)N = 8.43–13.28 (Figure 8). They exhibit relative depletion of Sr and HFSE (e.g., Nb, Zr, and Ti; Figure 8), with high MgO > 8 wt.%, TiO2 > 0.5 wt.%, and Mg# > 60 . Therefore, the mafic dykes at Qianlishan belong to calc-alkaline high-Mg andesite (HMA; [59]).
The Nd isotope composition of 11 samples was analyzed (Supplementary Table S4). Whole-rock εNd(t) values of the main-phase granites and the granite porphyry are −8.04 to −7.10 and −8.58 to −8.08, respectively. The values of the mafic dykes are −2.08 to 0.73.

6. Discussion

6.1. Ages of Qianlishan Granites and Mafic Dykes

In this study, the main-phase porphyritic and equigranular granites yielded zircon U-Pb ages of 158.9 ± 1.1 and 157.8 ± 1.4 Ma, respectively. These ages are higher than the ages of 153 ± 2 and 152 ± 2 Ma obtained by the method of SHRIMP (Supplementary Table S5; [24,61]). They do, however, show concordance with the mineralization age of 159.8 ± 2.9 Ma by molybdenite Re-Os isochron date [62]. As the mineralization is closely related to the Qianlishan main-phase granites, we thus conclude that the age in this study is accurate and that the difference may be due to multiple magmatic pulses because of different sample locations [40]. The granite porphyry exhibits a zircon U-Pb age of 144.5 ± 1.0 Ma. The mafic dykes sample displays a zircon U-Pb age of 157.6 ± 1.8 Ma. Although we observed that the mafic dykes intrude into the main-phase granite (Figure 3e), their zircon U-Pb age within error (1.14%) cannot be distinguished by the method of LA-ICP-MS [63], and the age results indicate that they might be generated contemporaneously. However, we observed that the mafic dykes are cutting through the main-phase granites in the field (Figure 3f), so the mafic dykes are later than the main-phase granites. Therefore, the geochronological characteristics of the Qianlishan complex suggest that the main-phase granites and mafic dykes have contemporaneous emplacement ages and are significantly older than the granite porphyry.

6.2. Genesis Type of the Qianlishan Complex

The main-phase granites are characterized by high SiO2 (72.16–75.63 wt.%); differentiation index values; low (La/Yb)N ratios (1.21–1.87); and distinct Ba, Sr, Ti, and Eu depletions (Figure 8), suggesting an affinity of A-type granites (Figure 9a–c [64]). However, it is difficult to identify the genetic type of such highly fractionated granites because the compositions of such rocks tend to be close to the near minimum-temperature melt [65]. The low abundances of HFSE (Nb = 17.5–74.9 ppm and Y = 34.2–102.2 ppm, Supplementary Table S3) especially indicate that these samples cannot be simply considered A-type granites, which are characterized by high abundances of HFSE (>350 ppm [64,66]). It has been well accepted that the content of REE in I-type and S-type granitic melts could be used as an effective indicator to distinguish the genetic type of granite [67,68]. This is because highly fractionated S-type granites generally have low La, Ce, and Y contents and have a negative correlation of Rb (Figure 9; [67]). The peraluminous and highly fractionated signatures in combination with the negative arrays involving REEs vs. Rb (Figure 9d–f), suggest an S-type affinity for all of the main phase Qianlishan granites [69]. Moreover, in Eu/Eu* vs. SiO2 and Zr/Hf vs. Nb/Ta plots (Figure 10), these samples reveal an increasing degrees of magma differentiation, which causes the rise in content of Ga and further results in the abnormally high 10,000*Ga/Al ratios, which show A-type affinity in Figure 9b,c.
In contrast, the geochemical characteristics of the granite porphyry samples show high ratios of 10,000*Ga/Al, high content of Nb + Ce + Y + Zr (>350 ppm) and are enriched in Nb, Ce, Y, and Ga. Therefore, they can be seen in the A-type granite zone in the discrimination diagrams of A-type granite (Figure 9a–c), consistent with Chen et al. [20] and Chen et al. [40] but different from the views on S-type granites of Guo et al. [24]. In fact, the granite porphyry showed extremely low P2O5 content (<0.25%), obviously differing from the abundance of P2O5 found in fractionated S-type granite [67]. Thus, the granite porphyry is A-type granite.
The mafic dykes are represented by sub-alkaline andesite in the SiO2 vs. Zr/TiO2*10,000 and SiO2 vs. Nb/Y diagram (Figure 11a,c). Furthermore, the CA/TH index of the mafic dykes is >1, and the high Th content indicates that they are calc-alkaline (Figure 11b,d; [71]). The calc-alkaline andesite has high MgO > 8 wt.%, TiO2 > 0.5 wt.%, and Mg# > 60, showing geochemical affinity to Setouchi high-Mg andesite (HMA; Figure 11e,f [72]). This HMA exhibits slightly enriched LREE and depleted Nb–Ta–Ti (Figure 8). In addition, it is characterized by low SiO2 (51.1–54.6 wt.%), Sr (270–383 ppm), and Sr/Y ratios (12.0–14.9) with high Y (20.6–28.7 ppm), Yb (2.61–3.88 ppm), and K2O/Na2O. Such characteristics are distinct from those of typical adakites [73] but similar to Sanukitic HMA (Figure 11f and Figure 15b; [72]).

6.3. The Relationship between Qianlishan Mafic Dykes and Granites

In situ zircon Hf isotopic analysis is an effective tool in determining the nature of magma sources and the mixing process during the formation of magmas [78]. Though the main-phase granites are highly evolved S-type granites and they preserve little evidence of the composition of the parental magmas and show different Nd isotopes and HFSE ratios (e.g., Zr/Nb and Zr/Hf in Figure 12) from the contemporaneous mafic dykes, the isotopic results still provide us a chance to explore the nature of their origin [79]. The diagram of age versus εNd(t) shows low and homogeneous εNd(t) values of the main-phase granites plotted in the zone of the Precambrian crust of the South China Block (SCB) and mantle (Figure 6a,b). In contrast, the zircon Hf isotopes exhibit a much wider range of εHf(t) values from −8.3 to 0.7 (Figure 6c,d), indicating that the mantle-derived component was indeed involved in their genesis. Therefore, the main-phase granites may be the products of parental melting of ancient basement with highly negative εHf(t) values mixed with mantle-derived components with εHf(t) values around zero. However, compared to the Qianlishan mafic dykes, the main-phase granite samples display high HREE (Yb = 6.12–13.1 ppm) and Y (34.2–102 ppm) contents and flat HREE patterns, precluding a residual phase within the crustal source [80]. Moreover, these samples have significant negative anomalies of Eu and Sr, enrichment in LILE, and the trace element patterns requiring partial melting of source rocks within the stability field of plagioclase [73]. Hence, they should have a relatively shallow source (approximately 30 km). Therefore, we propose that the main-phase granites were derived from partial melting of crustal rocks at a shallow depth caused by underplating of the basaltic magmas and mixed parts of a lateral underplating magma.
Different from the main-phase granites, the granite porphyry is A-type granite. However, the εNd(t) values of these samples are similar as those of main-phase granites and are plotted mainly close to the Precambrian crust of the SCB (Figure 6a,b). However, they show high ratios of CaO/Na2O (>17), suggesting that they originated from the partial melting of the ancient basement [81]. However, compared to the zircon εHf(t) of the ancient basement in subterranean south Hunan (−17.9 to −14.2 [82]) and the main-phase granites (−8.3 to 0.7), the values of the granite porphyry samples (−6.3 to 3.9) are much higher (Figure 6c,d). This indicates that the source of the granite porphyry has more contributions of mantle components than the main-phase granites. Therefore, the granite porphyry may also be a product of parental melting of the ancient basement mixed with mantle-derived components. The granite porphyry has positive correlations between Zr and Ce/Y, suggesting insignificant influence of fractional crystallization. Thus, the negative anomalies of Eu and Sr require partial melting of source rocks within the stability field of plagioclase. Although the granite porphyry exhibits high La/Yb and Dy/Yb, the Yb content of granite porphyry (3.9–8.5 ppm) do not exhibit significant differences in the main phase granite (6.12–13.1 ppm). Therefore, we prefer that the high La/Yb and Dy/Yb of granite porphyry mainly inherit from the source [80]. Thus, we conclude that the source of the mantle-derived components of the granite porphyry is the Qianlishan mafic dykes, which display similar Zr/Nb and Zr/Hf ratios to the granite porphyry (Figure 12) and conform to the chronology results above. In addition, one sample of the granite porphyry shows significantly similar geochemical characteristics of high La/Yb and LREE enrichment to the Qianlishan mafic dykes, as seen in Chondrite-normalized REE patterns (Figure 8). Therefore, we propose that granite porphyry is the product of partial melting of a hybrid source with the ancient basement and the Qianlishan mafic dykes.

6.4. Tectonic Implications

Previous studies have shown that HMA is common in the subduction zones, such as Japan and the Aleutian Islands, which are frequently considered products of partial melting of hydrous mantle peridotite or metasomatized lithospheric mantle [83,84,85,86]. Moreover, typical HMA is also observed within cratons, which are diversely interpreted as interactions between partial melts of eclogite and mantle peridotite (e.g., North China Craton [87]) and/or interactions of slab-derived components with an overlying mantle wedge [88,89,90].
The Qianlishan HMA in this study does not show adakitic affinity (Figure 11f) and is unlikely to be derived from interaction between partial melts of eclogite and mantle peridotite by lower foundering of the thick lower crust or dehydration of slabs [87,89]. A previous study of HMA in the Youjiang Basin suggested that its enriched εNd(t) (−7.8 to −4.3) and zircon εHf(t) (−14.0 to −9.2) are similar to early Paleozoic high-Mg rocks originating from ancient metasomatized SCLM associated with Neoproterozoic subduction along the Jiangnan Orogen [39]. In fact, some geochemical data of whole rock in this study are similar to those for HMA in the Youjiang Basin, e.g., Th/Sm (1.33–1.77), Th/Ce (0.14–0.18), Th/Yb (3.73–5.12), Ba/La (12.8–20.5), Th/Nb (0.59–0.74), and Nb/Yb (5.17–6.44) ratios (Figure 13 and Figure 14), suggesting the addition of subducted sediment-derived components [39,91]. However, the HMA in this study is different from early Paleozoic high-Mg rocks and HMA in the Youjiang Basin due to its significantly depleted whole-rock εNd(t) (−2.08 to 0.73) and zircon εHf(t) (−4.4 to 4.3; Figure 6). Moreover, the Qianlishan HMA consists of HMA and enriched mid-ocean ridge basalts (EMORB)-like tholeiitic dolerites (Figure 14a,b [92]). The EMORB-like tholeiitic dolerites exhibit depleted εNd(t) with high Ba/La (12.8–20.5) and arc-like Nb-Ta-Ti anomalies, suggesting an affinity to back-arc basalt (Figure 8 and Figure 14c [93]). The diagram of εNd(t) vs. La/Nb further suggests that the Qianlishan HMA could be the result of mixing melts of depleted asthenospheric mantle and metasomatized SCLM (Figure 15). Based on such signatures, we thus infer the following processes to explain genesis of the Qianlishan complex: (1) the slab roll-back may have led to generation of Qianlishan back-arc basalt and HMA, and the HMA further formed the Qianlishan mafic dykes in the Late Jurassic; (2) asthenospheric underplating led to mantle and crust interaction, and lithospheric mantle in the SCB melted, resulting in the formation of Qianlishan granites during the Late Jurassic (Figure 16).

7. Conclusions

1. The Qianlishan complex consists of the main-phase porphyritic and equigranular granites, granite porphyry, and mafic dykes with emplacement ages at 158.9 ± 1.1, 157.8 ± 1.4, 144.5 ± 1.0, and 157.6 ± 1.8 Ma, respectively.
2. The main-phase granites are high-K, calc-alkaline, and highly fractionated S-type granites. The granite porphyry is A-type granite. The mafic dykes are characterized by high-Mg andesite (HMA).
3. The main-phase granites are derived from a hybrid source of crust which involved a mantle-derived component. The granite porphyry is the product of partial melting of a hybrid source with Qianlishan mafic rocks and ancient basement. The Qianlishan mafic dykes are derived from mixing melts of depleted asthenospheric mantle and metasomatized SCLM.

Supplementary Materials

The following are available online at https://www.mdpi.com/2075-163X/10/12/1069/s1, Table S1: LA-ICP-MS U-Pb isotopic data of zircon of the Qianlishan complex, Table S2: Hf isotopic data of zircons separated from the Qianlishan complex, Table S3: Major and trace elements of the Qianlishan complex, Table S4: Whole-rock Nd isotopic data of the Qianlishan complex, Table S5: Synthesis of the ages of the Qianlishan complex.

Author Contributions

Conceptualization, Z.-F.Y. and Z.Z.; methodology, Z.-F.Y. and Y.X.; investigation, Z.-F.Y., Y.-Q.W. and H.W.; writing—original draft preparation, Z.-F.Y.; writing—review and editing, Z.-F.Y., Q.-M.P. and Z.Z.; project administration, P.-A.W.; funding acquisition, Z.Z. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the National Key Research and Development Plan (No. 2016YFC0600208), by the National Nonprofit Institute Research Grant of Chinese Academy of Geological Sciences (No. JYYWF20180502), and by the National Science Foundation of China (No. 41973046).

Acknowledgments

We express our acknowledgement for reviews by Winston Wen Zhao and Xin-You Zhu. Yu Mu and Yan-Lin Zhu are thanked for support for the figures.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. Geological map of the Nanling Region, South China modified from Chen et al. [40].
Figure 1. Geological map of the Nanling Region, South China modified from Chen et al. [40].
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Figure 2. Sketch map of the Qianlishan granites modified from Chen et al. [40] and Chen et al. [20]. Data cited: (1) this paper, (2) Chen et al. [20], and (3) Chen et al. [40].
Figure 2. Sketch map of the Qianlishan granites modified from Chen et al. [40] and Chen et al. [20]. Data cited: (1) this paper, (2) Chen et al. [20], and (3) Chen et al. [40].
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Figure 3. Photographs of the Qianlishan complex: (a) porphyritic granite and banded pegmatitic edge; (b) pegmatitic schlieren in porphyritic granite; (c) granite porphyry; (d) mafic dyke intruded into porphyritic granite; (e) cryptoexplosive breccia in equigranular granite; and (f) mafic dyke cut through the main-phase granite. Abbreviations: PG: porphyritic granite; EG: equigranular granite; GP: granite porphyry; MD: mafic dykes; Sk: skarn; Pe: pegmatite; and Cb: cryptoexplosive breccia.
Figure 3. Photographs of the Qianlishan complex: (a) porphyritic granite and banded pegmatitic edge; (b) pegmatitic schlieren in porphyritic granite; (c) granite porphyry; (d) mafic dyke intruded into porphyritic granite; (e) cryptoexplosive breccia in equigranular granite; and (f) mafic dyke cut through the main-phase granite. Abbreviations: PG: porphyritic granite; EG: equigranular granite; GP: granite porphyry; MD: mafic dykes; Sk: skarn; Pe: pegmatite; and Cb: cryptoexplosive breccia.
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Figure 4. Microphotographs of rocks of the Qianlishan complex: (a) porphyritic granite; (b,c) equigranular granite; (d,e) granite porphyry; and (f) mafic dyke. Abbreviations: Pl: plagioclase; Q: Quartz; Mus: Muscovite; Kf: K-feldspar; Toz: topaz; Wf: Wolframite; F: Fluorite; Sch: scheelite; Py: pyrite; and Aug: augite.
Figure 4. Microphotographs of rocks of the Qianlishan complex: (a) porphyritic granite; (b,c) equigranular granite; (d,e) granite porphyry; and (f) mafic dyke. Abbreviations: Pl: plagioclase; Q: Quartz; Mus: Muscovite; Kf: K-feldspar; Toz: topaz; Wf: Wolframite; F: Fluorite; Sch: scheelite; Py: pyrite; and Aug: augite.
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Figure 5. U–Pb concordia diagrams of zircon data and representative cathodoluminescence images of zircons from the Qianlishan complex: (a) main-phase porphyritic granites; (b) main-phase equigranular granites; (c) granite porphyry; and (d) mafic dykes. MSWD—mean square of weighted deviates.
Figure 5. U–Pb concordia diagrams of zircon data and representative cathodoluminescence images of zircons from the Qianlishan complex: (a) main-phase porphyritic granites; (b) main-phase equigranular granites; (c) granite porphyry; and (d) mafic dykes. MSWD—mean square of weighted deviates.
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Figure 6. Plots of εNd(t) versus t (a,b) and εHf(t) versus t diagrams (c,d) for the granites and mafic dykes of the Qianlishan complex: the εNd isotopic evolution fields for Proterozoic crust in South China are cited from Shen et al. [53]. Data cited from Chen et al. [20].
Figure 6. Plots of εNd(t) versus t (a,b) and εHf(t) versus t diagrams (c,d) for the granites and mafic dykes of the Qianlishan complex: the εNd isotopic evolution fields for Proterozoic crust in South China are cited from Shen et al. [53]. Data cited from Chen et al. [20].
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Figure 7. Geochemical classification of the Qianlishan granites: (a) total alkali vs. silica (TAS) diagram for classification [54]; (b) diagram of A/NK vs. A/CNK [55], A/NK = molar ratio of [Al2O3/(Na2O + K2O)], A/CNK = molar ratio of [Al2O3/(CaO + Na2O + K2O)]; (c) K2O vs. SiO2 diagram [56]; and (d) (Al2O3 + CaO)/(FeO + Na2O + K2O) vs. 100 * [(MgO + FeO + TiO2)/SiO2] classification diagram [57]. Data cited from Chen et al. [20].
Figure 7. Geochemical classification of the Qianlishan granites: (a) total alkali vs. silica (TAS) diagram for classification [54]; (b) diagram of A/NK vs. A/CNK [55], A/NK = molar ratio of [Al2O3/(Na2O + K2O)], A/CNK = molar ratio of [Al2O3/(CaO + Na2O + K2O)]; (c) K2O vs. SiO2 diagram [56]; and (d) (Al2O3 + CaO)/(FeO + Na2O + K2O) vs. 100 * [(MgO + FeO + TiO2)/SiO2] classification diagram [57]. Data cited from Chen et al. [20].
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Figure 8. (a) Chondrite-normalized rare earth element (REE) patterns of main-phase granites, granite porphyry, and mafic dykes of Qianlishan and (b) primitive mantle-normalized trace element diagrams for main-phase granites, granite porphyry, and mafic dykes of Qianlishan (main-phase granites in black, granite porphyry in red, and mafic dykes in blue): the values of chondrite and primitive mantle are from [60].
Figure 8. (a) Chondrite-normalized rare earth element (REE) patterns of main-phase granites, granite porphyry, and mafic dykes of Qianlishan and (b) primitive mantle-normalized trace element diagrams for main-phase granites, granite porphyry, and mafic dykes of Qianlishan (main-phase granites in black, granite porphyry in red, and mafic dykes in blue): the values of chondrite and primitive mantle are from [60].
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Figure 9. Selected plots of trace element concentrations from I-, S-, and A-type granitoids: (a) (Na2O + K2O)/CaO vs. Zr + Nb + Ce + Y, (b) Nb vs. 10,000*Ga/Al, and (c) Y vs. 10,000*Ga/Al classification diagrams [64]. (d–f) Selected plots for distinguishing I-type and S-type magmas indicate that the granite samples are most likely fractionated from S-type magmas [67]. Data cited from Chen et al. [20].
Figure 9. Selected plots of trace element concentrations from I-, S-, and A-type granitoids: (a) (Na2O + K2O)/CaO vs. Zr + Nb + Ce + Y, (b) Nb vs. 10,000*Ga/Al, and (c) Y vs. 10,000*Ga/Al classification diagrams [64]. (d–f) Selected plots for distinguishing I-type and S-type magmas indicate that the granite samples are most likely fractionated from S-type magmas [67]. Data cited from Chen et al. [20].
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Figure 10. Diagrams of (a) SiO2 vs. Eu/Eu* and (b) Nb/Ta vs. Zr/Hf in which the common range of granites is as reported by Jahn et al. [70]. Data cited from Chen et al. [20].
Figure 10. Diagrams of (a) SiO2 vs. Eu/Eu* and (b) Nb/Ta vs. Zr/Hf in which the common range of granites is as reported by Jahn et al. [70]. Data cited from Chen et al. [20].
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Figure 11. Plots of (a) SiO2 vs. Zr/TiO2 [74], (b) FeO/MgO vs. SiO2 [71], (c) SiO2 vs. Nb/Y [74], (d) Th vs. Co [75], (e) Mg# vs. SiO2 [72], and (f) Sr/Y vs. Y [72] for the Qianlishan and the South China Block (SCB) mafic rocks: data for the SCB mafic rocks are from Cen et al. [76], Chen et al. [20], Gan et al. [39], and Zhao et al. [77].
Figure 11. Plots of (a) SiO2 vs. Zr/TiO2 [74], (b) FeO/MgO vs. SiO2 [71], (c) SiO2 vs. Nb/Y [74], (d) Th vs. Co [75], (e) Mg# vs. SiO2 [72], and (f) Sr/Y vs. Y [72] for the Qianlishan and the South China Block (SCB) mafic rocks: data for the SCB mafic rocks are from Cen et al. [76], Chen et al. [20], Gan et al. [39], and Zhao et al. [77].
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Figure 12. Plots of (a) Zr/Hf vs. εNd(t) and (b) Zr/Nb vs. εNd(t) showing the magmatic differentiation model.
Figure 12. Plots of (a) Zr/Hf vs. εNd(t) and (b) Zr/Nb vs. εNd(t) showing the magmatic differentiation model.
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Figure 13. Plots of (a) La vs. La/Yb, (b) Nb/La vs. Zr/Nb, (c) εNd(t) vs. SiO2, and (d) Ni vs. Cr [39] for the Qianlishan and the SCB mafic rocks: cited data are the same as in Figure 11. The DM in (c) is marked by SiO2 = 45 wt.%, Nd = 4.0 ppm, εNd(t) = +8.0, and Nb/La = 0.75; its derivation is marked by SiO2 = 48 wt.%, Nd = 20 ppm, εNd(t) = +8.0, and Nb/La = 0.75; and the SCB crustal rock is marked by SiO2 = 70 wt.%, Nd = 26.3 ppm, εNd(t) = −15.0, and Nb/La = 0.32. The fields for different rocks in (d) are from Zhang et al. [86] and the references therein.
Figure 13. Plots of (a) La vs. La/Yb, (b) Nb/La vs. Zr/Nb, (c) εNd(t) vs. SiO2, and (d) Ni vs. Cr [39] for the Qianlishan and the SCB mafic rocks: cited data are the same as in Figure 11. The DM in (c) is marked by SiO2 = 45 wt.%, Nd = 4.0 ppm, εNd(t) = +8.0, and Nb/La = 0.75; its derivation is marked by SiO2 = 48 wt.%, Nd = 20 ppm, εNd(t) = +8.0, and Nb/La = 0.75; and the SCB crustal rock is marked by SiO2 = 70 wt.%, Nd = 26.3 ppm, εNd(t) = −15.0, and Nb/La = 0.32. The fields for different rocks in (d) are from Zhang et al. [86] and the references therein.
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Figure 14. Plots of (a) TiO2/Yb vs. Nb/Yb, (b) Th/Yb vs. Nb/Yb [94], (c) Ba/La vs. Th/Yb, (d) U/Th vs. Yh/Nb, (e) Sm/Yb vs. Sm, and (f) εNd(t) vs. Nb/La [39] for the Qianlishan and the SCB mafic rocks: cited data are the same as in Figure 11. Normal mid-ocean ridge basalts (N-MORB), enriched mid-ocean ridge basalts (E-MORB), and oceanic island basalts (OIB) of (b) are cited from [94]. The fields of the global subducting sediment (GLOSS) and bulk continental crust (BCC) in (c,d) are from Plank and Langmuir [92]. The dashed and solid lines of (e) are melting trends for the DM (Sm = 0.3 ppm and Sm/Yb = 0.86 [95]) and the SCLM (Sm = 0.6 ppm and Sm/Yb = 0.96 [96]). The DM of (f) is represented by La = 0.4 ppm, Nb = 0.3 ppm, Nd = 4.0 ppm, and εNd(t) = +8 [97]; sediment-derived fluid is represented by La = 37.5 ppm, Nb = 2.25 ppm, Nd = 75 ppm, and εNd(t) = −15; and sediment-derived melt is represented by La = 47.6 ppm, Nb = 17.8 ppm, Nd = 51.4 ppm, and εNd(t) = −15 [98].
Figure 14. Plots of (a) TiO2/Yb vs. Nb/Yb, (b) Th/Yb vs. Nb/Yb [94], (c) Ba/La vs. Th/Yb, (d) U/Th vs. Yh/Nb, (e) Sm/Yb vs. Sm, and (f) εNd(t) vs. Nb/La [39] for the Qianlishan and the SCB mafic rocks: cited data are the same as in Figure 11. Normal mid-ocean ridge basalts (N-MORB), enriched mid-ocean ridge basalts (E-MORB), and oceanic island basalts (OIB) of (b) are cited from [94]. The fields of the global subducting sediment (GLOSS) and bulk continental crust (BCC) in (c,d) are from Plank and Langmuir [92]. The dashed and solid lines of (e) are melting trends for the DM (Sm = 0.3 ppm and Sm/Yb = 0.86 [95]) and the SCLM (Sm = 0.6 ppm and Sm/Yb = 0.96 [96]). The DM of (f) is represented by La = 0.4 ppm, Nb = 0.3 ppm, Nd = 4.0 ppm, and εNd(t) = +8 [97]; sediment-derived fluid is represented by La = 37.5 ppm, Nb = 2.25 ppm, Nd = 75 ppm, and εNd(t) = −15; and sediment-derived melt is represented by La = 47.6 ppm, Nb = 17.8 ppm, Nd = 51.4 ppm, and εNd(t) = −15 [98].
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Figure 15. Plots of (a) εNd(t) vs. La/Nb [39,99] and (b) MgO vs. SiO2 [94] for the Qianlishan and the SCB mafic rocks: cited data are the same as in Figure 11. Early Paleozoic high-Mg rock from Yao et al. [100] and Wang et al. [101]; Jurassic mafic rock in the SCB and SCLM from Gan et al. [39].
Figure 15. Plots of (a) εNd(t) vs. La/Nb [39,99] and (b) MgO vs. SiO2 [94] for the Qianlishan and the SCB mafic rocks: cited data are the same as in Figure 11. Early Paleozoic high-Mg rock from Yao et al. [100] and Wang et al. [101]; Jurassic mafic rock in the SCB and SCLM from Gan et al. [39].
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Figure 16. Schematic illustration of the petrogenetic mechanism of the Qianlishan high-Mg andesite (HMA) and Qianlishan granites.
Figure 16. Schematic illustration of the petrogenetic mechanism of the Qianlishan high-Mg andesite (HMA) and Qianlishan granites.
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Yu, Z.-F.; Peng, Q.-M.; Zhao, Z.; Wang, P.-A.; Xia, Y.; Wang, Y.-Q.; Wang, H. Geochronology, Geochemistry, and Geodynamic Relationship of the Mafic Dykes and Granites in the Qianlishan Complex, South China. Minerals 2020, 10, 1069. https://doi.org/10.3390/min10121069

AMA Style

Yu Z-F, Peng Q-M, Zhao Z, Wang P-A, Xia Y, Wang Y-Q, Wang H. Geochronology, Geochemistry, and Geodynamic Relationship of the Mafic Dykes and Granites in the Qianlishan Complex, South China. Minerals. 2020; 10(12):1069. https://doi.org/10.3390/min10121069

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Yu, Zhi-Feng, Qi-Ming Peng, Zheng Zhao, Ping-An Wang, Ying Xia, Yu-Qi Wang, and Hao Wang. 2020. "Geochronology, Geochemistry, and Geodynamic Relationship of the Mafic Dykes and Granites in the Qianlishan Complex, South China" Minerals 10, no. 12: 1069. https://doi.org/10.3390/min10121069

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