| Citation: | Peng Feng, Lu Wang, Xiawen Li, Wenjie Ding, Zhe Chen. SS-LASS Zircon Dating Deciphering Multiple Episodes of Anatexis in a Deeply-Subducted Continental Crust: An Example from Sulu Orogen, China. Journal of Earth Science, 2024, 35(1): 85-98. doi: 10.1007/s12583-022-1797-8
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'Single shot' laser-ablation split-stream (SS-LASS) technique analyzing unpolished zircon grains makes their thin rims tenable for determination, which thus offers great potential in deciphering the timing of multiple and short-lived episodes of anatexis and metamorphism in deeply-subducted continental crusts. Dominated granitic gneisses in the deeply subducted continental crust undergoing considerable fluid-melt activities persist multistage growth of zircon. Therefore, a comparative study of SS-LASS and laser ablation inductively coupled plasma mass spectrometer (LA-ICP-MS) zircon dating was conducted on the granitic gneisses from the Sulu belt in this study. Zircons mostly show a core-mantle-rim structure with CL-bright rims thinner than 5 μm. For LA-ICP-MS dating, relict magmatic zircon cores yield protolith ages of
Anatexis has a remarkable bearing on the evolution of orogenic crusts by heat and mass transfer (Sawyer et al., 2011; Vanderhaeghe, 2009; Brown and Rushmer, 2006). It also plays a pivotal role in influencing crustal deformation and strength (Rosenberg and Handy, 2005; Brown and Solar, 1999), and especially furthers the exhumation of deeply subducted slabs from mantle depth and post-collisional extension of orogenic belts (Ferrero et al., 2015; Sizova et al., 2012; Labrousse et al., 2011; Rey et al., 2009; Brown, 2005; Teyssier and Whitney, 2002). However, it is not effortless to explicitly prove that the incipient anatexis indeed took place in ultrahigh-pressure (UHP) metamorphic rocks, especially for granitic gneiss, because anatectic evidence could be erased by subsequent retrogression and deformation during the long journey of the parent rocks ascending to the shallow crustal depth (Hermann et al., 2013; Holness et al., 2011). Therefore, to decipher the timing and mechanism of anatexis, it is in instant need of robust records preserved in such refractory minerals as zircon.
Peritectic zircons generally present representative trace element features and inner structures (e.g., Chen and Zheng, 2017; Taylor et al., 2016; Rubatto et al., 2006; Nemchin et al., 2001), and likely trap multiphase solid inclusions further demonstrating a partial melting origin (Liu et al., 2020; Cesare et al., 2015; Kawakami et al., 2013). Moreover, because of the extremely high closure temperatures and remarkably low Pb diffusion of the U-Pb isotope system (Cherniak and Watson, 2003), U-Pb dating of peritectic zircon domains obtains the timing of anatexis (Taylor et al., 2016; Korhonen et al., 2013; Wu et al., 2007). Finally, isotope systematics, trace elements and mineral inclusions are well preserved in the robust zircon container from the destruction of later metamorphism or magmatism overprinting (Zheng et al., 2005). Thus, for deeply subducted crusts, the detailed study of inner microstructure, U-Pb dating and trace element compositions is increasingly crucial for deciphering multiple episodes of anatectic events. However, zircon rims due to limited growth in a relatively poor fluid system are too thin to be analyzed by conventional secondary ion mass spectroscopy (SIMS) or laser ablation inductively coupled plasma mass spectrometer (LA-ICP-MS) methods.
The laser-ablation split-stream (LASS) approach was created to avail of the MC-ICP-MS for isotopic ratios and SC/Q-ICP-MS for trace element compositions, respectively (Xie et al., 2008; Yuan et al., 2008). In this study, zircon without polishing was ablated by laser to produce an aerosol stream, which was then split to import part of it to an MC-ICP-MS to determine U-Pb isotopic ratios, and the rest to a Q-ICP-MS to measure elemental concentrations (Kylander-Clark et al., 2013). Compared with the conventional LA-ICP-MS approach, this method considerably enhances the precision of each date and is also maintainable for sampling notably smaller volumes of ablated zircon for subsequent analysis (Kylander-Clark et al., 2013). Therefore, the LASS method with high spatial resolution makes it possible for dating thin zircon rims and has great potential in identifying multiple, short-duration anatectic and metamorphic events in a deeply subducted crust (Viete et al., 2015).
In this contribution, we present SS-LASS and LA-ICP-MS zircon dating results of the UHP granitic gneisses from the Sulu belt, and further recognize three episodes of anatexis in the deeply subducted continental crust. This work is of great help to better understand the thermal evolutional history of the Sulu Orogen from continental collision to orogenic collapse, and also sheds fresh light on SS-LASS petrochronology identifying multiple, short-lived anatectic events in the collisional orogens.
The Qinling-Dabie-Sulu Orogen marks a long-lived polyorogenic intra-continental suture zone in central China (e.g., Wu and Zheng, 2013). In the extreme eastern part of this orogen, the Sulu belt preserves the record of a terminal collision between the Yangtze Craton and the North China Craton (Ernst et al., 2007; Hacker et al., 2000). The Sulu belt comprises high-pressure (HP) and UHP metamorphic zones (Liu et al., 2004; Fig. 1a). The UHP metamorphic zone mainly consists of dominating granitic gneiss with minor eclogite, paragneiss, garnet peridotite, marble and quartzite (Zhang et al., 2009; Hacker et al., 2000). The protoliths of the granitic gneisses were generally generated by the Neoproterozoic magmatism (ca. 800–700 Ma) during the breakup of the Rodinia (Liu and Liou, 2011; Zheng et al., 2004). Coesite-bearing zircon domains within the above metamorphic rocks timing UHP metamorphism of ca. 235–225 Ma (Liu and Liou, 2011).
Abundant geochronology studies on migmatitic UHP rocks cropped out throughout the Sulu UHP zone, demonstrate that this orogenic belt underwent extensive anatexis during exhumation (ca. 225–210 Ma; e.g., Wang S J et al., 2023, 2020a, 2017; Song et al., 2014; Wang L et al., 2014; Chen et al., 2013; Xu et al., 2013a; Liu et al., 2010; Zong et al., 2010) and post-collision (ca. 165–150 Ma; Feng et al., 2020; Li et al., 2013; Liu et al., 2012) stages, respectively. Subsequent to the UHP metamorphism, three episodic magmatism associated with remelting of the subducted Yangtze Craton were reported in the Sulu UHP metamorphic zone (Zhao and Zheng, 2009; Guo et al., 2005), generating: (ⅰ) syn-exhumation felsic-intermediate-mafic intrusions at ca. 225–200 Ma recognized in Rongcheng and Rizhao areas (e.g., Zhao et al., 2017, 2012; Xu et al., 2016; Yang et al., 2005); (ⅱ) post-collisional granite intrusions at ca. 161–141 Ma in the northern Sulu belt (e.g., Zhao et al., 2016; Zhang et al., 2010; Hu et al., 2004); and (ⅲ) post-collisional magmatism throughout the Sulu belt, including scattered intermediate-mafic rocks and widespread granites at ca. 133–110 Ma (e.g., Wang et al., 2020b, c, 2019; Liu et al., 2008; Huang et al., 2006; Guo et al., 2004).
Taohang is located in the north margin of the Sulu UHP zone (Fig. 1a). In the study area around Taohang, outcrops are dominated by granitic gneisses, which host layers, blocks and lenses of eclogite (Fig. 1b). Cretaceous granodiorite dykes crosscut these metamorphic rocks (Fig. 1b). In-situ UHP metamorphism was evidenced by coesite inclusions in zircon from the granitic gneiss (Ye et al., 2000). Yao et al. (2000) applied mineral thermobarometry to constrain the metamorphic peak of P = 3.1 GPa and T = 875–860 ℃; two kinds of omphacite-replacing symplectites representing different retrograde reactions occurring at P-T conditions of 1.7 GPa/820 ℃ and 0.9–0.7 GPa/740–700 ℃, respectively. LA-ICP-MS zircon geochronology together with Ti-in-zircon thermometry indicate the host granitic gneiss reached the metamorphic peak at 236 ± 5 Ma (n = 5) with calculated T of 750–650 ℃ at P of 3.5–3.0 GPa, and partial melting took place at 223 ± 3 Ma (n = 8) with crystallization temperatures of 880–700 ℃; whereas thin CL-bright zircon rims can't be analysed by SIMS or LA-ICP-MS methods (Li et al., 2014). Based on conventional mineral thermobarometry and phase equilibrium modeling, Feng et al. (2021) argued that the eclogite achieved metamorphic peak conditions of 3.6–3.1 GPa and 900–840 ℃. Anatexis of eclogite by omphacite-breakdown produced low-volume melts, which crystallized into leucosome pockets at P = 1.6–1.2 GPa and T = 780–690 ℃. U-Pb ages of ca. 217–214 Ma acquired by SS-LASS dating on the thin rims of zircon were regarded as records of melt crystallization during cooling processes along the P-T path of the host eclogite.
In this study, two granitic gneiss samples including TH173-2 and TH173-3 were collected from Taohang (Figs. 1b and 2) for further petrology and zircon dating studies. In this manuscript, mineral abbreviations were used according to Whitney and Evans (2010).
The granitic gneisses consist of quartz (41 vol.%–45 vol.%) + plagioclase (30 vol.%–37 vol.%) + K-feldspar (12 vol.%–16 vol.%) + phengite (4 vol.%–6 vol.%) + epidote (1 vol.%) + garnet (1 vol.%), with accessory biotite, zircon, titanite, apatite and iron oxide (Figs. 3a–3d). Anatexis of the granitic gneisses was evidenced by the following petrological phenomenas: (ⅰ) fine-grained biotite, K-feldspar and plagioclase located on the corroded boundaries of the phengite (Figs. 3a, 3b, 3d), suggesting the former occurrence of phengite-breakdown melting; (ⅱ) the presence of thin films of K-feldspar + plagioclase ± quartz along grain boundaries between coarse-grained quartz and plagioclase (Figs. 3a–3d, 3h); at triple junctions, these films commonly exhibiting low dihedral angles; (ⅲ) leucosome pools composed of plagioclase and K-feldspar enclosed by coarse-grained quartz and plagioclase grains (Figs. 3a, 3d).
In-situ zircon grains were recognized in the thin sections of the host granitic gneisses (Figs. 3d–3h). The zircons are generally situated in such melt pseudomorphs as leucosome pools and veinlets (Figs. 3d, 3e, 3h). These zircons mostly show subhedral to euhedral shapes and their aspect ratios range from 1 : 1 to 2 : 1 (Figs. 3d–3h). Mineral inclusions including iron oxide, apatite together with multiphase solid inclusion (Kfs + Pl + Ph) are identified in zircon grains (Figs. 3f, 3g). In consideration of the above features, these zircon grains were likely derived from anatectic origin.
In this study, the zircon grains selected from the host granitic gneisses were arrayed in epoxy resin. Unlike traditional dating methods, zircons for SS-LASS analysis were not polished. SS-LASS dating of zircon rims was determined at the University of California Santa Barbara. The LASS system integrates a Photon Machines 193 nm ArF Excimer laser and Hel-Ex ablation cell with a Nu Instruments HR Plasma high-resolution MC-ICP-MS system for collecting U-Pb isotope data, and an Agilent 7700 quadrupole for determining trace element concentrations. Methods used in this study follow those outlined by Kylander-Clark et al. (2013). During single-shot laser ablation, the spot size and frequency of the laser were set to 35 µm and 2 Hz with a laser fluence of ~1 j/cm2, yielding a pit depth of ~8 µm. In this study, zircon rim analyses included between the first 3 seconds (6 shots) up to the entire 40 seconds of the analysis (80 shots in total). For U-Pb isotope compositions, every 6 analyses of unknowns were bracketed by zircon reference materials 91500, GJ-1, NIST612 and Plešovice. 90Zr is used as the internal standard and GJ-1 is used as the reference material for determining trace element concentrations. Raw U-Pb isotope and trace element data were reduced using Iolite v2.5 (Paton et al., 2011) to correct for instrument drift, laser-ablation-induced down-hole elemental fractionation, plasma-induced elemental fractionation, and instrumental mass bias. Only part of the U-Pb isotope signal with best concordance and smooth will be selected for calculating the final age, which represents the date of the certain zircon layer.
X-ray energy dispersive spectroscopy for mineral identification, cathodoluminescence (CL) imaging for zircon inner structures and LA-ICP-MS zircon dating for elemental concentrations and isotope ratios were conducted in this study. The detailed information including operating process and instrument model are described in the supplementary material.
Under plane-polarized light, zircons from the granitic gneisses (TH173-2) are generally colorless and transparent. They exhibit euhedral to subhedral shapes and have lengths of 50–250 μm with aspect ratios ranging from 1 : 1 to 2 : 1. The zircon grains mostly show a core-mantle-rim structure in CL images (Fig. 4). The relict oscillatory-zoned cores have weak to moderate luminescence. The unzoned mantles with dark luminescence exhibit sharp contacts against the cores. In addition, most zircon grains have a thin (< ~5 μm) and CL-bright outer rim (Fig. 4), which is not possible to be analyzed by conventional LA-ICP-MS method. In addition, it's worth noting that several zircon grains have grey domains between dark mantles and bright rims (Fig. 4).
Zircon grains from the granitic gneiss samples were analyzed by LA-ICP-MS and SS-LASS methods for U-Pb dating, with the results shown in Table S1 and Fig. 5.
Nineteen spots on zircon grains from sample TH173-2 were analyzed. The inconcordant curve for all analyzed spots intercepts the Concordia at 197 ± 17 and 730 ± 78 Ma, respectively. Six analyses of relict oscillatory-zoned cores give 206Pb/238U dates varying from 756 ± 10 to 461 ± 14 Ma (Fig. 5a). Three analyses of 756 ± 10 to 747 ± 9 Ma with concordance > 95% acquire a weighted mean age of 752 ± 10 Ma (MSWD = 0.28; Fig. 5a). Zircon mantles with dark luminance yield 206Pb/238U dates of 219 ± 2 to 208 ± 3 Ma, giving a weighted mean age of 214 ± 3 Ma (n = 13, MSWD = 1.2; Fig. 5a).
Twenty and twenty-one analyses were performed by SS-LASS method on zircon grains from granitic gneiss samples TH173-2 and TH173-3, respectively. According to values of the zircon U-Pb ages, the dates can be divided into three distinct groups which are named after Group 1, Group 2 and Group 3. 206Pb/238U dates of Group 1 from sample TH173-2 vary from 229 ± 9 to 210 ± 7 Ma with a weighted mean age of 218 ± 3 Ma (n = 8, MSWD = 1.2; Fig. 5c), whereas 206Pb/238U dates of Group 1 from sample TH173-3 range from 226 ± 3 to 210 ± 3 Ma, giving a weighted mean age of 217 ± 3 Ma (n = 6, MSWD = 3.6) (Fig. 5c; Table S1). By contrast, analyses of Group 2 in the two samples yield a range of 206Pb/238U dates from 201 ± 6 to 188 ± 5 Ma (n = 6) and 193 ± 3 to 189 ± 4 Ma (n = 3), respectively (Table S1). These dates from the sample TH173-2 and TH173-3 yield weighted mean ages of 193 ± 5 Ma (MSWD = 0.91; Fig. 5c) and 191 ± 3 Ma (MSWD = 0.39; Fig. 5e), respectively. In addition, for Group 3, 206Pb/238U dates from sample TH173-2 range from 171 ± 3 to 156 ± 2 Ma with a weighted mean age of 161 ± 8 Ma (n = 6, MSWD = 5.1; Fig. 5c), whereas those from sample TH173-3 yield 206Pb/238U dates of 172 ± 4 to 155 ± 3 Ma with a weighted mean age of 162 ± 3 Ma (n = 12, MSWD = 2.3) (Fig. 5e; Table S1).
The trace element compositions of different zircon domains are summarized in Table S1 and presented in Fig. 5.
For the sample TH173-2, the relict oscillatory-zoned cores have variable Th/U ratios of 0.11–1.22 and Lu/Hf ratios of 0.005–0.013 (Figs. 5b, 6); whereas the CL-dark mantle domains have relatively low Th/U ratios of 0.01–0.05 and Lu/Hf ratios of 0.001–0.004 (Figs. 6a, 6b). Both oscillatory-zoned cores and CL-dark mantles show steep HREE patterns ([Lu/Gd]N of 26.68–157.76; 53.55–312.51) positive Ce and negative Eu anomalies (Figs. 5b, 6c, 6d).
Three groups of analyses from the samples TH173-2 and TH173-3 show similar steep HREE patterns and negative Eu anomalies (Figs. 5d, 5f, 6c, 6d). Analyses of Group 1 have total heavy rare earth element (∑ HREE) contents of 216 ppm–2 246 ppm, Th/U ratios of 0.006–0.15 and Lu/Hf ratios of 0.002–0.014; whereas Group 2 generally contain slightly lower ∑ HREE contents of 214 ppm–449 ppm, Th/U ratios of 0.008–0.03 and Lu/Hf ratios of 0.002–0.004. Group 3 have similar ∑ HREE contents of 176 ppm–583 ppm, Th/U ratios of 0.005–0.03 and Lu/Hf ratios of 0.002–0.006 with those of Group 2. Analyses from Group 1, Group 2 and Group 3 contain Nb contents of 1.90 ppm–68.3 ppm, 1.80 ppm–7.10 ppm and 1.53 ppm–6.07 ppm, respectively.
Crystallization temperatures of different zircon domains were calculated after Ti-in-zircon thermometry of Ferry and Watson (2007); the results are shown in Fig. 7 and Table S2. Due to the granitic gneisses containing quartz and titanite (Fig. 3a), αSiO2 and αTiO2 were set to be 1 and 0.5, respectively (Ferry and Watson, 2007; Hayden and Watson, 2007; Watson et al., 2006). The result is presented in box-and-whisker plots of Fig. 7. For the granitic gneisses, the interquartile ranges of the crystallization temperatures are: CL-dark mantles of TH173-2, 801–746 ℃ (median of 772 ℃); Group 1 of TH173-2, 833–778 ℃ (median of 799 ℃); Group 2 of TH173-2, 739–657 ℃ (median of 678 ℃); Group 3 of TH173-2, 716–669 ℃ (median of 708 ℃); Group 1 of TH173-3, 836–785 ℃ (median of 813 ℃); Group 2 of TH173-3, 740–658 ℃ (median of 667 ℃); Group 3 of TH173-3, 731–687 ℃ (median of 716 ℃).
Oscillatory zoning, high Th/U ratios and steep HREE patterns of the relict zircon cores exhibit indicate their magmatic origin. Besides, the trace element compositions of these cores plot into the field of relict magmatic zircon in the UHP rocks from the Dabie-Sulu belt (Fig 6). Therefore, concordant 206Pb/238U dates of 756 ± 10 to 747 ± 9 Ma yielded by the relict oscillatory-zoned cores approximately constrain the protolith age of the granitic gneisses.
The dark mantles with no zoning, low Th/U ratios and steep HREE patterns plot into a peritectic zircon field in Fig. 6. Combined with the multiphase solid inclusion (Kfs + Pl + Ph) within these zircon domains and high crystallization temperatures of 801–746 ℃, we thus argue these mantles with dark luminance crystallized from the hydrous melt. The weighted mean age of ca. 214 Ma retrieved from the zircon mantle domains is consistent with widely reported timing of syn-exhumation anatexis in the Sulu UHP zone (Fig. 8; Wang S J et al., 2020a, 2017; Song et al., 2014; Wang L et al., 2014; Chen et al., 2013a; Xu et al., 2013a; Liu et al., 2010; Zong et al., 2010).
Group 1 of the zircon analyses from the granitic gneisses have similar trace element compositions, Ti-in-zircon temperatures (836–778 ℃) and ages (ca. 217 Ma) with the spots on the CL-dark zircon mantles analyzed by LA-ICP-MS method (Figs. 5b, 5d, 5f, 6, 7), suggesting both recorded partial melting event of the UHP terrane occurring during exhumation stage.
Zircon analyses of Group 2 and Group 3 generally have extremely low Th/U ratios, steep HREE patterns and negative Eu anomalies (Figs. 5b, 5d, 5f), and fall into the field of peritectic zircon from Dabie-Sulu magmatic UHP rocks in Fig. 6. Compared with zircon domains crystallized from aqueous fluid in the granitic gneisses from Taohang area (e.g., Li et al., 2014, 2013), they have considerably higher Ti-in-zircon temperatures (740–657 ℃; 731–669 ℃) and Nb contents (1.80 ppm–7.10 ppm; 1.53 ppm–6.07 ppm). The above features including crystallization temperatures and trace element compositions indicate these two groups of analyses were derived from anatectic melt.
With the drag of gravity force of heavier subducted oceanic slab, continental slices were deeply subducted into mantle depth and underwent UHP metamorphism, which was followed by decoupling and exhumation (Leech, 2001; Vanderhaeghe and Teyssier, 2001). Anatexis of UHP metamorphic rocks commonly took place during exhumation stage when the P-T path crosses the solidus curve of the felsic crust. During the post-collisional stage, the reworking of collisional orogens commonly leads to lithosphere thinning that was accompanied by large-scale crustal remelting (Chen et al., 2015). Correspondingly, multiple episodes of anatexis have been identified in several collisional orogens by dating a large number of migmatite samples, including the central Alps, Himalaya, North Qaidam and Dabie-Sulu belt (e.g., Feng et al., 2020; Li et al., 2016; Chen et al., 2015; Zhang et al., 2014; Imayama et al., 2012; Liu et al., 2012; Rubatto et al., 2009). However, multiple episodes of anatexis in the same UHP rock were rarely reported because of the impossibility of dating thin (< 5 μm) anatectic overgrowth of zircon by conventional analysis methods of geochronology. Here we give a shot at recognizing multiple episodes of anatexis in the deeply subducted continental crust by using the approach of SS-LASS zircon dating.
A three-dimensional model in Fig. 9a is provided to more clearly show the tectonic setting and evolution of Dabie-Sulu Orogen related to the three episodes of anatexis identified in this study. Previous studies show that during the exhumation stage the granitic gneisses in the Sulu belt underwent considerable anatexis and form extensive migmatites (Fig. 8; e.g., Wang et al., 2017; Chen et al., 2013a; Xu et al., 2013a; Liu et al., 2010). Zircon mantles analyzed by LA-ICP-MS and Group 1 analyzed by SS-LASS record an episode of anatexis in the deeply subducted crust during the exhumation stage at ca. 218–214 Ma (Fig. 9b). Experimental petrology has demonstrated that phengite is a critical hydrate in UHP metamorphic rocks and plays a crucial role in melting reaction during exhumation (Auzanneau et al., 2006; Labrousse et al., 2002; Hermann and Green, 2001). Based on petrological observation on the granitic gneisses, phengite-breakdown melting was inferred by the identification of fine-grained biotite, K-feldspar located on the corroded boundaries of the phengite (Figs. 3a, 3b, 3d), which produced felsic melt during decompression according to the reaction of Ph + Qz ± Ep + Pl → Bt ± Grt + felsic melt. Moreover, multiphase solid inclusion of Kfs + Pl + Ph included by the mantle domain (Figs. 3f, 3g) is also a product of phengite-breakdown melting. In addition, crystallization temperatures of 836–746 ℃ (Fig. 7) recorded by the zircon mantles could lead to phengite-breakdown melting of the felsic crust during the exhumation stage (Zheng et al., 2011; Auzanneau et al., 2006). Therefore, we argue that the first episode of anatexis in this study was induced by phengite-breakdown melting during "hot" exhumation at ca. 218–214 Ma (Fig. 9b). Though several models have been developed to illustrate the exhumation of deeply-subducted crustal slices (Hacker et al., 2013), the melting activity is considered as one of the most crucial factors (e.g., Labrousse et al., 2015; Sizova et al., 2012). Extensive anatexis of the slab generated considerable melts and likely promoted the exhumation of the UHP slice from mantle depth in the Dabie-Sulu Orogen.
Anatectic event occurring at ca. 193–191 Ma is recorded by zircon analyses of Group 2 (Figs. 4c, 4e). Taking the whole Dabie-Sulu belt into account, comparable ages were not documented in the Sulu belt but primarily reported in the north Dabie zone. Wang et al. (2002) yielded a biotite 40Ar/39Ar plateau age of 195 ± 2 Ma for a felsic granulite at Huangtuling, and regarded it as the minimum age for granulite-facies metamorphism. Chen et al. (2015) identified a group of zircon dates ranging from 200 to 192 Ma in the felsic migmatite in the Yuexi dome and further attributed them to partial melting related to overprinting of granulite-facies during the late exhumation. In this study, zircon dates of ca. 193–191 Ma with relatively high crystallization temperatures of 740–657 ℃, reveal similar conditions with the anatectic event documented by the granulite in the north Dabie zone, which indicates part of the northern Dabie-Sulu belt was still "hot" in this period. Differential subduction and exhumation of crustal slices in the Dabie-Sulu Orogen were proposed by a systematic study on their P-T-t path (Liu Y C et al., 2011; Liu F L et al., 2009). For the Dabie-Sulu belt, the northern part of the UHP zone was considered as the slice which subducted to the deepest depth and exhumated latest, thus recording retrograde metamorphism with higher temperatures and younger ages during exhumation (Shi et al., 2013; Liu et al., 2009a). The northern Sulu UHP zone was overprinted by granulite-facies at P-T conditions of 700–620 ℃ and 0.8–0.5 GPa at 203–201 Ma (Liu et al., 2009a; Yao et al., 2000; Wang et al., 1993). Therefore, after the granulite overprinting, the occurrence of the second anatectic event at ca. 193–191 Ma could be interpreted as the successive heating of Taohang terrane which was buried in the thickened orogenic crust because of collisional processes.
Large-scale post-collisional magmatism in the Sulu belt has taken place during the Late Jurassic to Early Cretaceous (ca. 161–141 Ma; e.g., Zhang et al., 2010; Guo et al., 2005, 2004; Hu et al., 2004). Moreover, geophysical data suggest that the current Sulu belt lost its lower crust (e.g., Gao et al., 1998). Therefore, the extensional collapse of the thickened Sulu orogenic crust formed by the Triassic collision is commonly inferred. Nevertheless, when and how this process happened is highly controversial due to different study methods and relatively complicated tectonic settings (e.g., Ni et al., 2016; Zhao and Zheng, 2009; Liu et al., 2008; Guo et al., 2005). The initial stage of the extensional process for post-collisional orogens is generally related to an increased heat flow, and further generates extensive crustal anatexis and granitoid intrusions (Brown, 2001; Vanderhaeghe and Teyssier, 2001). Thus, the earliest age for crustal anatexis during the post-collisional stage is commonly considered as the lower time limit reaching an apogee of the extension (Wu et al., 2007; Whitney et al., 2003; Foster et al., 2001; Keay et al., 2001). The third episode of anatexis (ca. 162–161 Ma) derived from the zircon rims in the granitic gneisses by SS-LASS method is consistent with the intrusion timing of the Late Jurassic granitoids cropping out in the northern part of the Sulu belt and post-collisional crustal partial melting (ca. 165–150 Ma; Fig. 8) throughout the Sulu belt (Feng et al., 2020; Zhao et al., 2016; Liu et al., 2012; Zhang et al., 2010; Guo et al., 2005, 2001; Hu et al., 2004). We thus argue that the onset of the post-collisional collapse for the orogenic root of the Sulu belt occurred at ca. 162 Ma (Fig. 9d). Abundant evidence including subduction-related structures, accretion complexes and widely distributed Jurassic magmatism preserved in the eastern margin of the North China Craton demonstrates that the Izanagi Plate initially moved beneath the margin of Eastern Asia with low-angle subduction at ca. 165 Ma (reviewed by Zhu et al., 2017; Fig. 9a), which likely caused heat disturbance and trigger destabilization of the orogenic root, and further facilitate an initial collapse of Sulu Orogen at ca. 162 Ma. The zircon grains within Taohang granitic gneisses record anatexis occurring at ca. 193–191 Ma. Consequently, it is inferred that the Sulu orogenic belt has stayed stable for ca. 30 Ma before the initial collapse.
This study provides new insights into SS-LASS zircon petrochronology deciphering multiple anatectic events in the deeply-subducted continental crust and helps us to better understand the evolution of the Dabie-Sulu belt. Three distinct episodes of anatexis were identified in the UHP gneisses from the Sulu Orogen. The first episode of anatexis took place at ca. 218–214 Ma during the syn-exhumation stage, which was dominated by phengite-breakdown melting. The second episode of anatexis occurring at ca. 193–191 Ma indicates part of the northern Dabie-Sulu belt was still "hot" at that time as a result of deep burying. The third episode of anatexis at ca. 162–161 Ma suggests the initial collapse of the orogenic root of the Sulu belt occurred in the Late Jurassic due to the Izanagi Plate subducting beneath Eastern Asia.
ACKNOWLEDGMENTS: This study is supported by National Natural Science Foundation of China (Nos. 42072228, 42102060, 41902036, 41572182), China Postdoctoral Science Foundation (No. 2021M692983), the Chinese Ministry of Education (No.BP0719022), the Most Special Fund (Nos. MSFGPMR02-3, MSFGPMR30), Open funds from the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences (Nos. GPMR201703, GPMR201704 and GPMR201903), and the Fundamental Research Funds for National University (No. CUG-G1323511572). The final publication is available at Springer via https://doi.org/10.1007/s12583-022-1797-8.| Auzanneau, E., Vielzeuf, D., Schmidt, M. W., 2006. Experimental Evidence of Decompression Melting during Exhumation of Subducted Continental Crust. Contributions to Mineralogy and Petrology, 152(2): 125–148. https://doi.org/10.1007/s00410-006-0104-5 |
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| 1. | Miao-Yan Zhang, Lu-Lu Hao, Yue Qi, et al. Mantle metasomatism by subducted Indian continental crust: Evidence from post-collisional basaltic ultrapotassic rocks in southern Tibetan plateau. Lithos, 2025. doi:10.1016/j.lithos.2025.107966 | |
| 2. | Xing-wei WANG, Jia LIU, Hong-mei LI, et al. Ore fluid characteristics and genesis of the Shuangmiaoguan gold deposit, Dabie orogen. Bulletin of Mineralogy, Petrology and Geochemistry, 2024, 43(3): 579. doi:10.3724/j.issn.1007-2802.20240048 |
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Peng Feng, Lu Wang, Xiawen Li, Wenjie Ding, Zhe Chen. SS-LASS Zircon Dating Deciphering Multiple Episodes of Anatexis in a Deeply-Subducted Continental Crust: An Example from Sulu Orogen, China. Journal of Earth Science, 2024, 35(1): 85-98. doi: 10.1007/s12583-022-1797-8
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