Zircon U-Pb Dating for Paragneiss in the Xinxian Area in the Dabie–Sulu Orogenic Belt and Its Geochemical Characteristics

In order to understand the subduction of the Yangtze block and its collision with the North China Craton, we performed the elements analysis and zircon U-Pb dating on paragneiss from Xinxian area, which located along the west edge of the Dabie-Sulu ultrahigh-pressure (UHP) metamorphic belt. The major elements analysis showed SiO₂, Al₂O₃, and K₂O were enriched and the rare-earth element (REE) analysis showed the paragneiss had a high content of REEs, especially light rare Earth elements (LREEs). The elements analysis suggest that the protolith of paragneiss may be formed by terrestrial materials. As reflected by cathode luminescence (CL), zircon in rocks was metomorphic and had a core-edge microstructure. The edge of zircon was dated by LA-ICP-MS at 233 ± 24 Ma, which suggests that the paragneiss was formed later than the Triassic. The inherited zircon had a large age range of 456–1,727 Ma, mainly in the range of 705–811 Ma. The wide range of ages suggests that the protolith of paragneiss was sedimentary rocks formed no earlier than the Paleozoic. And the paragneiss from Xinxian area were generated in the Dabie-Sulu ocean basin or abortive ocean basin in the Paleozoic era.

Introduction

As one of the largest UHP metamorphic belts in the world, the Dabie-Sulu belt, located between the northern margin of the Yangtze Craton and the southern margin of the North China Craton, has received much attention. It has been widely investigated since the discovery of coesite and microgranular diamond in its eclogite (Okay et al., 1989; Wang et al., 1989; Shutong et al., 1992; Shu-tong et al., 2003). Many geochronological researches have shown that the Dabie-Sulu UHP metamorphic belt was formed by the subduction of the Yangtze block and its collision with the North China Craton during the Triassic (Liu et al., 2003; Shu-tian and You, 2005). The tectonic evolution of the subduction-collision was recorded by the rock assemblies in this metamorphic belt.

The metamorphic belt is mainly composed of eclogite, gneiss and jadeitite quartzite, among which gneiss is the dominant rock and accounts for a larger proportion than any other rock (Dao-gong et al., 2000; Wang et al., 2000; Zheng et al., 2000; Liu et al., 2004). Some geochronological and geochemical studies showed that the protolith of gneiss was related to the Neoproterozoic rift magmatism on the northern edge of the Yangtze block (Zheng et al., 2003; Zheng et al., 2006). Besides, other studies found that the protolith also contained Paleoproterozoic and Archean metamorphic rocks and some Neoproterozoic and Paleozoic granites (Chen et al., 2013). Geochronological and geochemical analysis of gneiss is helpful for the determination of the characteristics of the protolith and understanding of the magmatic activities of the Yangtze Plate during different ages. Meanwhile, it also helps to understand the subduction of the Yangtze block and its collision with the North China Craton.

Although several geochronological and isotopic studies on metamorphic rocks in the Dabie-Sulu UHP metamorphic belt were carried out in the 1990s, most of them only focused on the northern Dabie area in the east of the metamorphic belt (Wu et al., 2001). The researches of the Xinxian area at the western edge of the metamorphic were largely limited to eclogite and gneiss (Wang et al., 1993; Xue-xie et al., 1993), while paragneiss was less studied (Yang et al., 2009; Yang et al., 2009). Based on these previous studies, we investigated the paragneiss and ages of zircon in paragneiss and further discussed the protolith of paragneiss.

Regional Geology

The paragneiss in the Xinxian area is distributed in the west edge of the Dabie-Sulu UHP metamorphic belt and is classified into the quartz andesite gneiss assemblage as shown on the 1:500,000 geological map of the Dabieshan orogenic belt (Figure 1): The assemblage refers to mica plagioclase gneiss with lenticles of marble, jadeitite, and eclogite (YG₁) and mica plagioclase gneiss with lenticles of eclogite (YG₂) (Shu-tong et al., 2005). Outcropping strata in the Xinxian area mainly include the Lower Paleozoic Erlangping Group (Pz₁er), Middle Proterozoic Huwan Formation (Pt₂h), Middle Proterozoic Guishan Formation-Complex (Pt₂g), Sinian to Ordovician Xiaojiamiao Formation (Z-O₁x), Devonian Nanwan Formation (Dn), Lower Cretaceous Chenpeng Formation (Kc), and Quaternary (Q).

FIGURE 1

FIGURE 1. Geological map of the Xinxian area in the Dabie orogenic belt (modified after Kun-guang et al., 2009; Dong-xing et al., 2011). J-K, Jurassic–Cretaceous volcanic rocks and volcano-sedimentary rocks; Kc, Lower Cretaceous Chenpeng Formation; Dn, Devonian Nanwan Formation; Pz₁er, Lower Paleozoic Erlangping Group; Z-O₁, Sinian–Lower Ordovician Xiaojiamiao Formation-Complex; Pt₂h, Middle Proterozoic Huwan Formation-Complex; Pt₂g, Middle Proterozoic Guishan Formation-Complex; Ar₃db, Neoarchean Dabie Formation-Complex; $\eta {\gamma }_5^3$, Late Yanshanian monzonitic granite; $\gamma {\pi }_5^3$, Yanshanian granite porphyry; $h{g}_5^3$, Yanshanian quartz diorite; Pt₃T $\eta \gamma$, Neoproterozoic Tianpu Sequence granite paragneiss.

The paragneiss in the Xinxian area was earlier classified into the Archean Dabie Group (Ar₃db) and Neoproterozoic Tianpu Sequence granite paragneiss (Pt₃T $\eta \gamma$). It is dominated by the Dabie gneissic complex composed of metamorphic supracrustal rocks and metamorphic plutonic rocks. Metamorphic supracrustal rocks consisted of biotite monzonite paragneiss, plagioclase hornblende paragneiss, dolomite quartz schist and magnetite quartzite, among others. Metamorphic plutonic rocks were composed of monzonite granite gneiss, muscovite diorite paragneiss and biotite plagioclase paragneiss (Liu et al., 2004). The Archean Dabie Group (Ar₃db) is distributed in the Tongbai-Dabieshan subzone of the Qinling Stratigraphic Zone and is the oldest strata of the Qinling Fold System. It mainly outcrops in the mountainous area at the junction of the three provinces of Henan, Hubei, and Anhui, and its main body is located in the territories of Hubei and Anhui provinces. This group was composed of quartz schist, biotite schist, dolomite plagioclase paragneiss, dolomite monzonite paragneiss, biotite plagioclase paragneiss, hornblende diorite paragneiss and banded migmatite, etc. It is in unconformable contact with the underlying Archean Dabie Group.

Paragneiss samples were collected for subsequent analysis from the Xinxian Qianhe quarry and the north of Xinxian county (the No. 1 and 2 sampling points marked by black stars in Figure 1). Samples QH-1, QH1A, and QH-2 were collected from the quarry (N 31°41.551′, E 114°56.921′) located on the east side of the road to the south of Qianhe village. Samples XX4-1 and XX4-2 were collected from a hill behind the coach station in the north of Xinxian county (N 31°41.329′, E 114°54.262′) (Figure 2). These rocks are off-white and medium to fine-grained and have black and white strips. They are composed of potassium feldspar, plagioclase, quartz, biotite, etc. Samples XX4-1 and XX4-2 were obtained from thick-layered and thin-layered paragneiss, respectively.

FIGURE 2

FIGURE 2. Outcrops of paragneiss in the north of Xinxian county (A) and in the Xinxian Qianhe quarry (B).

Analytical Methods

Petrochemical Analysis

Petrochemical tests were conducted on 5 samples from Qianhe and the north of Xinxian county for major and trace elements analyses. Experiments were carried out at the State Key Laboratory of Isotope Geochemistry, Guangzhou Institute of Geochemistry, Chinese Academy of Sciences. Major elements were determined by the Varian Vista-PRO ICP-AES (CCD full-spectrum direct reading ICP-AES), with an analytical error (RSD) of less than 5%. Detailed procedures can be found in (Goto and Tatsumi, 1994). Trace elements were determined by the PE-Elan 6000 ICP-MS in the ultra-purification laboratory of the Guangzhou Institute of Geochemistry, Chinese Academy of Sciences, with a RSD of less than 10%. Detailed procedures can be found in (Liu et al., 1996).

Zircon U-Pb Dating

Zircon samples were processed before U-Pb dating to get rid of mixtures. First, ca. 500 g of rock sample was weighed out and crushed into 1 cm³ grains. Then these grains were put into a 20 cm-size stainless steel bowl and were ground repetitively for 3–5 s each time in an XZW100 vibrating mill until they were broken into 60 mesh. Dust was removed and an aluminum-made batea was used to concentrate heavy minerals. Then through magnetic and electromagnetic processing, magnetic minerals were removed and refined zircon was obtained. Finally, zircon grains with good crystals were hand picked under binocular for dating (Zhang et al., 2004).

LA-ICP-MS zircon U-Pb dating was conducted at the Key Laboratory of Isotope Geochronology and Geochemistry, Guangzhou Institute of Geochemistry, Chinese Academy of Sciences. Zircon grains were fixed by epoxy resin and made into laser ablation sample targets. The sample targets were ground and polished until the central surface of the zircon was exposed. Carbon dust was sprayed on zircon for CL imaging and then was wiped off for LA-ICP-MS U-Pb analysis (single spot laser ablation was used with a diameter of the laser spot of 31 μm and at a firing frequency of 8 Hz). Detailed analytical procedures can be found in (Tu et al., 2011). ²⁰⁴Pb data were used to correct Pb data in zircon. The errors of single data points were within 1σ. The ²⁰⁶Pb/²³⁸U age was obtained, whose weighted averages were at the 95% confidence level. Experimental results were plotted into concordia diagrams using the software of Isoplot 3.0 (Ludwig, 2012).

Experimental Results

Characteristics of Major Elements

As shown in Table 1, results were obtained through the geochemical analysis of major elements. It can be seen that the paragneiss in the Qianhe area has a high content of silicon (SiO₂ = 76.10–76.42%), aluminum (Al₂O₃ = 11.58–11.91%), and alkali elements (Na₂O + K₂O = 8.35–8.50%) but shows a deficiency in titanium (TiO₂ = 0.09–0.10%) and calcium (CaO = 0.13–0.26%). Its potassium content is comparatively high (Na₂O/K₂O = 0.57–0.76) and Aluminous Saturation Index (A/CNK) is in the range of 1.35–1.38, suggesting that the rock is peraluminous.

TABLE 1

TABLE 1. Analytical results of major (%) and trace elements (μg/g) for the Xinxian paragneisses.

The paragneiss in the north of Xinxian county is consistent with the one in the Qianhe area in terms of chemical composition, as it is rich in silicon (SiO₂ = 68.29–75.93%), aluminum (Al₂O₃ = 12.58–16.06%) and alkali elements (Na₂O + K₂O = 8.14–8.63%) but poor in titanium and calcium (CaO = 0.14–0.53%). By comparison, its content of potassium (Na₂O/K₂O = 0.79–1.19) is lower than that of the paragneiss in the Qianhe area. As the A/CNK is in the range of 1.43–1.85, it is evident that the rock is peraluminous.

Characteristics of Trace and Rare Earth Elements

The results of trace element analysis are shown in Table 1. The total amount of REE was high in the Qianhe paragneiss (QH-1, QH-2, and QH-3), up to 117.55–216.89 μg/g. As shown in the chondrite-normalized REE diagram (Figure 3), LREEs were enriched as La/Yb was between 4.27 and 4.86 and the negative Eu anomaly was evident (δEu is 0.12–0.13) (Sun and McDonough, 1989). Besides, its pattern curve was skewed to the right and had an obvious V valley. As shown in the primitive mantle-normalized trace element spider diagram (Figure 4), elements such as Rb, K, Th, and U were enriched in the paragneiss in the Qianhe area whereas elements such as Ba, Nb, Sr, and Ti were depleted.

FIGURE 3

FIGURE 3. Primitive mantle-normalized trace-elements spider diagram.

FIGURE 4

FIGURE 4. Chondrite-normalized REE plot of paragneiss.

The total amount of REEs was also high in the Xinxian paragneiss (XX4-1, XX4-2), up to 122.97–240.37 μg/g. Its chondrite-normalized REE plot was similar to that of the paragneiss of the Qianhe area; however, the content of heavy rare Earth elements (HREE) was higher with La/Yb in the range of 4.00–11.71. Besides, the negative Eu anomaly was relatively indistinct with δEu of 0.53–0.73. As shown in the spider diagram (Figure 4), elements such as Rb, K, Ba, Th, and U were enriched in the paragneiss in the north of Xinxian county whereas elements such as Nb, Sr, and Ti were depleted.

Results of Zircon Dating

Zircon U-Pb dating was conducted on Samples QH-1 and QH-1-A from the Qianhe area and Samples XX4-1 and XX4-2 from the north of Xixian county. The CL image (Figure 5) shows that zircon grains were of similar sizes with a length to width ratio of about 1:2. All zircons contained detrital zircon and most of them had a clear core-edge double structure. Detrital zircon in the core of zircons had oscillatory zoning. For most zircons, the edge was darker than the core (Table 2).

FIGURE 5

FIGURE 5. CL images of zircon in paragneiss ((A) Qianhe QH-1 sample, (B) Qianhe QH-1-A sample, (C) XX4-1 thick-layered paragneiss sample and XX4-2 thin-layered paragneiss sample from the north of Xinxian county).

TABLE 2

TABLE 2. Zircon LA ICP MS U-Pb age data of Qianhe and Chengbei paragneisses in Xinxian.

Five points on the detrital zircon of the metamorphic composite zircon sample QH-1 were selected for the determination of Th and U concentrations (Figure 5A). The ratio of Th/U suggests that these zircons were formed during the Proterozoic at the ages of 801, 793, 756, 743, and 727 Ma, respectively. Five points on the edge of the metamorphic composite zircon were dated at 251, 228, 226, and 211 Ma, respectively (Figure 6).

FIGURE 6

FIGURE 6. Zircon U-Pb concordia diagram for paragneisses (A); zircon U-Pb concordant ages in the range of 705–811 Ma (B).

A total of 17 points on the detrital zircon of the metamorphic composite zircon sample QH-1-A were selected for the determination of Th and U concentrations (Figure 5B). Four age ranges were obtained: 913, 811-803, 784-724, and 684 Ma. One point on the edge of the metamorphic zircon was dated at 352 Ma.

A total of 24 points on the detrital zircon of Xinxian metamorphic composite zircon samples were selected for the determination of Th and U concentrations (Figure 5C). These points have a wide age range: 456–1,727 Ma. One point on the edge of the metamorphic zircon was dated at 256 Ma.

U-Pb dating results for the edge of the metamorphic zircon and the metamorphic composite zircon were more concentrated, with ages ranging from 211 to 352 Ma and concordant ages of 233 ± 24 Ma. Besides, the Th/U ratios of these seven points are in the range of 0.08–0.37 while three of them are below 0.1, significantly smaller than the Th/U ratio of magmatic zircon (generally greater than 0.4) and closer to that of metamorphic zircon (Bryant et al., 2002). As suggested by the U-Pb dating results, the detrital zircons in the samples were mainly formed during the Neoproterozoic (564–884 Ma), with their ages mainly in the range of 705-811 Ma. However, some detrital zircons were formed in the Paleozoic and Middle Proterozoic as shown by dating results.

Discussion

Analysis of Zircon U-Pb Dating Results

Two results were obtained from zircon U-Pb dating. The first one was about the edge of metamorphic zircon, whose age was in the range of 211–352 Ma and concordant age was 233 ± 24 Ma. The other result was about detrital zircon in metamorphic zircon, whose age ranged from 456 to 1,727 Ma, mostly between 705 and 811 Ma.

The edge of the metamorphic zircon in samples was dated to the Triassic, suggesting that paragneiss in Xinxian county experienced high-pressure metamorphism during the Triassic. It was consistent with a large amount of previous research on the metamorphic age of the Dabie-Sulu UHP metamorphic belt which confined the age to the Triassic. Hacker et al. (1998) suggested that the metamorphism of the Dabie-Sulu UHP metamorphic belt reached its peak at 245 Ma through zircon dating for paragneiss. Liu et al. (2006) found through U-Pb dating for the edge of metamorphic zircon with coesite that the metamorphic event of the Dabie-Sulu UHP metamorphic belt took place during 240–225 Ma. Our work suggests that the edge of metamorphic zircon is consistent with the data reported by previous researchers, providing further evidence that paragneiss in Xinxian county experienced ultrahigh-pressure metamorphic events during the Triassic.

The dating results of detrital zircon showed that many samples were dated to the middle of the Neoproterozoic, which accounted for about 72% of the total number of samples. Their age range of 700–800 Ma was consistent with the characteristic zircon age of rocks in the Yangtze block (Rowley et al., 1997; Hacker et al., 1998). Considering no large-scale magmatic activity was recorded in the Middle Neoproterozoic in the North China craton, the protolith of the paragneiss in Xinxian county was hence supposed to originate from the Yangtze block. As the magmatic activity was caused by the breakdown of the Rodinia supercontinent, the protolith of the paragneiss of Xinxian county may contain granite formed in the Middle Neoproterozoic in the Yangtze block. In addition, part of detrital zircon in Sample XX4-2 was dated to the Paleozoic (456–532 Ma), which was consistent with data obtained by previous researches of the paragneiss of the UHP belt (Hacker et al., 1998; Liu et al., 2004). However, such age data were in small amount in previous researches and were considered to be the result of the loss of Pb, or due to the fact that the core and edge of zircon were not separated. Hence, these data were not widely discussed or constraining the age by the fugacity state of the paragneiss and orthogneiss (Fu-lai and Xue, 2007). Additionally, (Yuan et al., 2015) found that the core of metamorphic zircon in paragneiss in Luotian of Hubei province was mostly dated to the Paleozoic. No signs of Pb loss could be found, and the boundary between the margin and core was also clear on CL images. Further, considering parts of zircon were dated to the Paleozoic in our work and they had the Th/U ratio close to the ratio range of zircon of magmatic origin (Dao-gong et al., 2001), part of the protolith of the paragneiss was supposed to form later than 456 Ma. As some detrital zircon in the samples was dated to the Middle Proterozoic, the source material of the protolith could possibly come from the crustal residual of the Middle Proterozoic in the Yangtze block rather than from the Paleozoic sedimentary cover.

Protolith Analysis

With regard to the protolith of the paragneiss of the Dabie-Sulu UHP metamorphic belt, it was considered in previous research to be mainly granite formed by the magma coming from the Rodinia rift in the Neoproterozoic at the north edge of the Yangtze block (Zheng et al., 2003). Based on geochemical analysis of the paragneiss in the Dabie belt and Cretaceous granite, the source materials were likely to come from the north edge of the subducting Yangtze block (Frost and Frost, 2011). Therefore, some researchers proposed that the paragneiss in the Dabie belt and Cretaceous granite were produced at different horizons of the Yangtze block (Shu-guang et al., 1997).

The samples of paragneiss from Xinxian had a high SiO₂ content, up to 68.29–76.42%, and their A/CNK reached 1.35–1.85, indicating they are peraluminous. The alkali content ranged between 8.14 and 8.63%, in which the content of potassium is relatively high as the ratio of Na₂O/K₂O is between 0.57 and 1.19. The content of calcium was low and in the range of 0.13–0.53% (Wong et al., 2009; Frost and Frost, 2011). Light rare Earth elements (LREEs) were enriched in the samples and negative Eu anomaly was distinct. Elements such as Rb, K, Th, and U were enriched whereas elements such as Nb, Sr, and Ti were depleted. This distribution pattern suggests that the protolith was formed by the materials of the continental crust (Chen et al., 2006). Felsic magma generated by partial melting of felsic rock under high pressure can extract Si, K, Na, LILEs, and LREEs (Hermann and Green, 2001), and hence, the magma can become enriched in silicon, alkali, aluminum and LREEs while depleted in calcium and magnesium and iron. As Gu found LILEs and LREEs were depleted in eclogite (Gu et al., 2013), it suggests that the paragneiss in Xinxian county might be partially melted, like the felsic magma formed under high pressure. The continuous process from sub-solidus dehydration to partial melting within the UHP gneissic rocks is also evidenced by experimental and petrological observations in Shuanghe paragneiss (Liu and Wu, 2013). According to the geochemical characteristics of the samples, the protolith is likely to be sedimentary rock that has been partially melted during the subduction and retreat of the Yangtze block (Wallis et al., 2005).

Tectonic Setting of the Shuanghe UHP Metamorphic Protolith

By volume, the gneiss occupies between 70 and 80% of the Dabie-Sulu complex (e.g., Dao-gong et al., 2000; Wang et al., 2000; Hui-fen et al., 2001). Of these, 40–60% comprise foliated, garnet-bearing, A-type granitic rock (Shu-tian and You, 2005). These rocks are associated with jadeite-quartzites and marbles that formed from quartz sandstone and limestone respectively. According to the zircon U-Pb dating results, the protoliths of these rocks are controlled by Paleozoic Dabie - Sulu basin. Distributions of the major-elements of these rocks are high SiO₂, alkali-rich, high Na₂O and low Al₂O₃. The mineral component is more rich in alkaline ferromagnesian. The sedimentary origins of these protoliths appear to be neritic facies, some of which are clastic sediments (quartz sandstone to arkoses) and chemical sediments (limestone). These are characteristic of the continental slope environment. The Dabie-Sulu ocean basin was not a mature ocean; it lacked deep-water sedimentation, such as siliceous deposits and turbidites. It evidently lacked contemporaneous pillow lavas and cumulates of ophiolite rock assemblages which is why we have not found remnants of ophiolitic melanges (Wang and Cong Bo-lin, 1998). As the Dabie-Sulu ocean basin was an aborted oceanic basin, it narrowed, with a resultant increase in salinity. This ultimately led to the oceanic basin sediments becoming increasingly alkaline. This provided the necessary material conditions for the formation of alkaline mafic minerals (sodic pyroxenes and amphiboles) during the Late Triassic metamorphism of these rocks.

Conclusion

1) Paragneiss in the Qianhe and Chengbei areas of Xinxian county experienced a metamorphic event during 233 ± 24 Ma, suggesting that the rock was formed later than the Permian.

2) Paragneiss in Xixian county is enriched in silicon, alkali, aluminum and LREEs while depleted in calcium, magnesium and iron. Besides, negative Eu anomalies are evident. It suggests that the protolith may be formed by terrestrial materials.

3) Detrital zircon in paragneiss in the Qianhe area and north of Xinxian county was dated to 456–1727 Ma, mainly in the range of 705–811 Ma. It suggests that the protolith should be formed no earlier than 456 Ma. And they were generated in the Dabie-Sulu ocean basin or abortive ocean basin in the Paleozoic era.

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

LY was responsible for most of the experimental analysis and paper writing; ZY was responsible for sampling and experimental processing; LZ was responsible for the experimental design and the paper revision.

Conflict of Interest

Author ZS was employed by the company The 2nd Oil Production Plant of Daqing Oilfield Limited Company.

The remaining 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

All claims expressed in this article are solely those of the authors and do not necessarily represent those of their affiliated organizations, or those of the publisher, the editors, and the reviewers. Any product that may be evaluated in this article, or claim that may be made by its manufacturer, is not guaranteed or endorsed by the publisher.

Acknowledgments

Researcher Xianglin Tu, Key Laboratory of Isotope Dating and Geochemistry, Guangzhou Institute of Geochemistry, Chinese Academy of Sciences, and others assisted in U-Pb age determination and provided many valuable comments, and we would like to express our sincere gratitude.

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