Detrital Zircon Geochronology of Devonian Quartzite from Tectonic Mélange in the Mianlue Suture Zone, Central China: Provenance and Tectonic Implications

International Geology Review

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Detrital zircon geochronology of Devonian quartzite from tectonic mélange in the Mianlue Suture Zone, Central China: provenance and tectonic implications

Xing-Zhong Ji, Li-Qiang Yang, M. Santosh, Nan Li, Chuang Zhang, Zhi-Chao Zhang, Ri Han, Zai-Chun Li & Chun-Jun Wu

To cite this article: Xing-Zhong Ji, Li-Qiang Yang, M. Santosh, Nan Li, Chuang Zhang, Zhi- Chao Zhang, Ri Han, Zai-Chun Li & Chun-Jun Wu (2016) Detrital zircon geochronology of Devonian quartzite from tectonic mélange in the Mianlue Suture Zone, Central China: provenance and tectonic implications, International Geology Review, 58:12, 1510-1527, DOI: 10.1080/00206814.2016.1167635

To link to this article: http://dx.doi.org/10.1080/00206814.2016.1167635

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Download by: [Shanghai Jiaotong University] Date: 17 October 2016, At: 00:27 INTERNATIONAL GEOLOGY REVIEW, 2016 VOL. 58, NO. 12, 1510–1527 http://dx.doi.org/10.1080/00206814.2016.1167635

Detrital zircon geochronology of Devonian quartzite from tectonic mélange in the Mianlue Suture Zone, Central China: provenance and tectonic implications Xing-Zhong Jia, Li-Qiang Yanga, M. Santosha,b, Nan Lia, Chuang Zhangc, Zhi-Chao Zhanga, Ri Hana, Zai-Chun Lia and Chun-Jun Wud aState Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Beijing, PR China; bDepartment of Earth Sciences, University of Adelaide, Adelaide, Australia; cDivision of Geology and Mineral Resources, Beijing Research Institute of Uranium Geology, Beijing, PR China; dTechnology Centre, 12th Gold Mine Detachment of the Chinese Armed Police Force, Chengdu, PR China

ABSTRACT ARTICLE HISTORY Devonian quartzite occurs as blocks within a phyllite matrix in Puziba area of the Mianlue Suture Received 5 January 2016 Zone (MLSZ) in central China. The depositional time of the quartzite is younger than 425 Ma Accepted 15 March 2016 – (mainly Early Devonian), constrained by the zircon U Pb geochronology data from the quartzite, KEYWORDS cross-cutting relationships with granite, and palaeontology evidence. The detrital zircons in the Detrital zircon quartzite show typical magmatic features with four main age peaks at: 2676–2420 Ma (11.6% of geochronology; quartzite; the population), 1791–1606 Ma (4.8%), 997–817 Ma (26.5%), and 597–425 Ma (17.5%). In combi- Mianlue Suture; Qinling nation with the zircon εHf(t) values, we propose that the quartzite in the MLSZ was sourced from Orogen; tectonic evolution Neoproterozoic and Palaeozoic magmatic and sedimentary rocks in the South Qinling Block and the South China Block (particularly from the Bikou Terrane), with minor contributions from Archaean and Palaeoproterozoic magmatic units from both of the South and North China blocks. The blocks of quartzite, slate, marble, metasandstone, and chert blocks in the phyllite matrix in the Puziba area show a typical block-in-matrix texture in a tectonic mélange, and provide significant evidence from sedimentary rock blocks rather than ophiolite or volcanic rock for the existence of the MLSZ.

1. Introduction The lithostratigraphic compositions of the different tectonic units in the Qinling Orogen are complex. The S- The Qinling Orogen, the central orogenic belt in China, NCB is mainly composed of ancient basements (Ar – which separates the North and the South China blocks 3 Pt ), volcanic rocks (Pt ), clastic and carbonate sequence [Figure 1(A) and (B)], is bounded by the Lingbao– 1 2 (Pt –Pt ), tillite (Pt ), and passive continental margin Lushan–Wuyang Fault (LWF) in the north and the 2 3 3 successions (Є–O) (Dong and Santosh 2015). The NQB Mianlue–Bashan–Xiangguang Fault (MBXF) in the consists of the Kuanping Group (Pt –Pt ophiolite, Pt south (Dong and Santosh 2015). The Orogen itself can 1 2 3 sedimentary units), Erlangping Group (Palaeozoic ophio- be divided into the Southern North China Block (S-NCB), lite), Qinling Group (Precambrian basement of gneiss, the North Qinling Block (NQB), and the South Qinling amphibolite and marble, Neoproterozoic, and Block (SQB) by the Luonan–Luanchuan Fault (LLF), the Palaeozoic plutons), Songshugou Complex (Pt –Pt Shangdan Suture Zone (SDSZ), and the Mianlue Suture 1 2 ophiolite), and Danfeng Group (ophiolite) (Zhang et al. Zone (MLSZ) from north to south [Figure 1(B)], respec- 2003). The Shangdan Suture comprises Palaeozoic tively. The Shangdan and the Mianlue Sutures contain ophiolitic assemblages, subduction-related volcanic, magmatic and sedimentary rocks and structures that and sedimentary rocks (530–470 Ma). The SQB could can be used to reconstruct the continental rifting, open- be divided into the Northern and the Southern SQB ing and closing of the oceanic basin, and the subduc- because of the different lithostratigraphic units, and tion and collision processes between the North and the the boundary is near the E–W trend fault from South China Blocks (Zhang et al. 2003; Dong and Mianxian to Shangnan [Figure 1(B)] (Dong and Santosh Santosh 2015). 2015). The Northern SQB is primarily composed of

CONTACT Li-Qiang Yang [email protected] State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, No. 29 Xueyuan Road, Beijing 100083, PR China Supplemental data for this article can be accessed here. © 2016 Informa UK Limited, trading as Taylor & Francis Group INTERNATIONAL GEOLOGY REVIEW 1511

Figure 1. (A) Simplified geological map showing the central Qinling–Dabie Orogen separating the North and the South China blocks. (B) The geological map of the Qinling Orogenic Belt, showing the Mianlue and the Shangdan suture zones (modified from Zhang et al. 2003; Dong and Santosh 2015). QL, Qilian Orogen; DB, Dabie Terrane; SL, Sulu orogenic belt.

gneiss and amphibolite (Pt3), pelagic turbidite (D2–D3) Carboniferous to late Permian, and the large scale of and clastic rocks (C, P, T); while the Southern SQB mainly subduction occurred from Early–Middle Triassic), with consist of granitic gneiss, amphibolite and marble (Ar3), the final closure of the Mianlue Ocean and the conse- clastic and volcanic rocks (Pt3), clastic and carbonate quent continent–continent collision between the South rocks (Pt3), limestone (Є–O), shale (S), and minor clastic China Block and the SQB occurring in the Middle–Late rocks (D, C, P, T) (Dong and Santosh 2015). To the south, Triassic, which also represents the final collision of the the Mianlue Suture comprises Neoproterozoic and North and South China blocks (Zhang et al. 2003; Dong Palaeozoic ophiolite and volcanic rocks, and continental and Santosh 2015). The region subsequently trans-

margin sedimentary rocks (Palaeozoic-T2) (Zhang et al. formed into an intra-continental tectonic setting in the 2003). The Bikou Terrane is mainly composed of Late Triassic (Zhang et al. 2003). Several important sedi- Neoarchaean Yudongzi Group (gneiss, amphibolite, mentary–metamorphic quartzite and hydrothermal gold greenschist, and quartzite), Neoproterozoic volcanic– deposits (Li et al. 2007, 2014; Liang et al. 2014; Zhou sedimentary rock, and turbidite (Wei 1994; Yan et al. et al. 2014), located within or near the MLSZ, have been 2004). The Dabie Terrane is an ultra-high pressure meta- correlated to the tectonic evolution of the Mianlue morphic terrane, and it consists of granitic and pelitic Suture and the SQB. Hence, research on the rock asso- gneisses, with minor eclogite, garnet–peridotite, pyrox- ciations in the MLSZ is significant not only to clarify the enite, marble, and jadeite–quartzite (Zhang et al. 2009). tectonic evolution of the Qinling Orogen but also pro- The MLSZ, separating the SQB and the South China vide information on the genesis of the ore deposits and Block [Figure 1(B)], is the boundary fault zone of the the ore-forming processes (Deng et al. 2014a, 2014b; southern margin of the central orogenic belt in China. Yang et al. 2016a, 2016b). Previous studies of the ophiolite complex, volcanic and In recent years, with the development of analytical intrusive rock suites, and sedimentary units within the facilities using laser ablation inductively coupled plasma MLSZ have shown that the suture formed during the mass spectrometry (LA-ICP-MS) for zircon geochronol- late Palaeozoic to early Mesozoic (Li et al. 2002; Zhang ogy, detrital zircons in clastic sedimentary rocks have et al. 2003; Wu and Zheng 2013). The rifting and open- been extensively used to constrain the maximum age of ing of the initial Mianlue oceanic basin occurred during deposition, provide source information of the sedi- the early Silurian to early Carboniferous (Li et al.(2002) ments, and unravel the tectono-sedimentary evolution suggested the rifting existed from the Early Devonian to of continental realms (Burrett et al. 2014; Spencer et al. early Carboniferous), with the ocean reaching its largest 2014; Wang et al. 2014; Henrique-Pinto et al. 2015). In extent during the early Carboniferous to mid-Permian addition, the Lu–Hf isotopic composition of detrital zir- (Zhang et al. 2003). Subduction of the Mianlue Ocean cons can provide important clues on crustal growth took place during the late Permian to Middle Triassic (Li (Roberts and Spencer 2015). et al.(2002) thought the subduction and expansion of In this paper, we report LA-ICP-MS U–Pb ages and the Mianlue Ocean were coexisted from early Lu–Hf isotopic compositions of detrital zircons in the 1512 X.-Z. JI ET AL.

Devonian quartzite from the Puziba area of the MLSZ. (Zhang et al. 2003). Therefore, our research has focused Our results provide new constraints on the depositional on this segment. time and provenance of the Devonian quartzite, and The Mianxian–Wenxian–Maqu segment of the throw light on the tectonic evolution of the Mianlue MLSZ is located between the SQB and the Bikou Suture. Terrane, and its northern and southern boundaries are the Songbai–Liping–Zhuangyuanbei Fault and the Wenxian–Lianghekou–Lueyang Fault, respectively 2. Geological setting and sampling (Figure 2;Laiet al. 1997). The main strata in this area The MLSZ is marked by a series of thrust faults and later are widespread Devonian metamorphic mudstone, left-lateral strike-slip fault systems (Figures 1(B) and 2: sandstone and carbonate rocks. Besides, Sinian meta- Zhang et al. 2003; Chen et al. 2010), and these deep morphic volcanic, clastic and carbonate rocks outcrop structures, which reached down to the crust–mantle in Wenxian–Lianghekou and Mianxian, and few boundary, can provided pathways for ore-forming fluids Carboniferous carbonate and clastic rocks are also and thus lead to the formation of important gold found in the west (Figure 2;YangandHu1990). In deposits (Yang et al. 2014; Deng et al. 2015a, 2015b). addition, ophiolites, ocean-island basalts, island-arc The WNW–ESE-trending curvilinear suture extends for volcanic rocks, and bimodal volcanic rock units are ~1500 km from the Dabie Terrane in the east to the discontinuously distributed in the area (Figure 2): all Qilian Orogen in the west [Figure 1(A)], and it is mainly of these ophiolites and related volcanic rocks outcrop made up of three arcuate thrust nappe structures from as tectonic slices in the Devonian strata (Li et al. 1996; east to west, called the southern Dabie Terrane, Lai et al. 1997, 2003a, 2003b), and their geology and Southern Daba Mountains, and Mianxian–Wenxian– geochemistry indicate that there was an oceanic basin Maqu segment, respectively. The Mianxian–Wenxian– that had opened, spread, and subsequently closed Maqu segment (Figures 1(B) and 2) is the most impor- (Zhang et al. 2003). tant thrust nappe structure and has attracted attention There are two periods of ophiolites and related vol- for its widespread ophiolites, volcanic and sedimentary canic rocks displaying features of a tectonic and ophio- rock associations, which could indicate the presence of lite mélange (Figure 2; Table 1). The first group formed the Mianlue Suture and contribute to our understand- in the Neoproterozoic. Li et al.(2009) reported zircon U– ing of the tectonic evolution of the Qinling Orogen Pb ages of 783–754 Ma for the Pipasi mafic volcanic

Figure 2. The geological map of Mianxian–Wenxian–Maqu segment of the Mianlue Suture Zone (MLSZ) (modified from Zhang et al. 2003; Yang et al. 2015a, 2015b), showing the widespread Neoproterozoic ophiolite, volcanic, intrusive rocks and their U–Pb zircon ages in the MLSZ and the Bikou Terrane. INTERNATIONAL GEOLOGY REVIEW 1513 rock near Lianghekou; Yan et al.(2007) published evolution of the MLSZ, and a detailed study of the Neoproterozoic ages for the ophiolites and mafic–ultra- quartzite, which is the dominant unit, is important for mafic rocks from Kangxian to Mianxian (Figure 2); and understanding the subduction and collision associated Lin et al.(2013) found basalts and dacite with ages of with the amalgamation of the two major continental ~800 Ma in the west of Lueyang. These Neoproterozoic blocks (Hsü et al. 1987; Collins and Robertson 1997; Shi rock associations are similar in age to the magmatic et al. 2004; Huang et al. 2015). rocks in the Bikou Terrane (Figure 2; Table 1). Another Quartzite samples from three different blocks of group of ophiolites and related volcanic rocks formed in metasandstone with quartzite intercalation were col- the late Palaeozoic (Figure 2; Xu and Han 1996). These lected around Puziba [Figure 3(A)], 15 km away from are the Late Devonian marine volcanic rocks in Wenxian in the Gansu Province. In outcrop, the quart- Longkang–Tazang (Yang et al. 1995), ocean-island zite occurs as blocks in the phyllite matrix and loose basalts in Kangxian with ocean-island tholeiite and alka- blocks that have weathered out of the phyllite matrix line basalts (Lai et al. 2003a, 2003b), ophiolites in [Figure 4(A)–(C)]. The quartzite blocks are often massive, Sanchazi with the main rock association of ultrabasic slightly deformed and fragmented [Figure 4(A)–(C)], and rocks, cumulate gabbro, dolerite dikes and mid-oceanic it commonly consists of quartz (98%) and minor acces- ridge basalt (Li et al. 2003), island-arc volcanic rocks sory minerals, such as zircon and apatite. Some of the (mainly tholeiite) in Sanchazi and Wuliba (Lai et al. quartzite with a thickness of 10–30 cm is interlayered 2000, 2003a), and bimodal volcanic rocks with basalt with the phyllite [Figure 4(C) and (D)]. These thin quart- and rhyolite in Heigouxia (Li et al. 1996). These late zite layers are deformed and sheared, and can occur as Palaeozoic rock associations provide critical evidence lenticular bodies or elongated boudins [Figure 4(C) and for the tectonic evolution of the MLSZ. (D)]. The deformation and elongation of quartz crystals, The Devonian Sanhekou Group is one of the wide- together with recrystallization with jagged grain mar- spread sedimentary rock units in the Mianxian– gins [Figure 4(E) and (F)] are due to the sinistral shearing Wenxian–Maqu segment of the MLSZ, especially in event in the MLSZ that occurred after the terminal Puziba (Figure 2) in Gansu province. This region experi- collision between the North and the South China enced regional metamorphism under lower greenschist Blocks (Chen et al. 2010). The original rock of the quart- facies (Wei 1994), and the major rock types are phyllite, zite is quartz sandstone rather than chert, for medium- quartzite, slate, marble, metasandstone, and chert coarse quartz instead of microcrystalline quartz in the (Figure 3(A); Dong 2004) but lack ophiolite or volcanic quartzite (Yang et al. 2015a). It did not look like quartz rocks. Previous studies suggested that these different veins for the existence of widespread argillaceous mate- rock types have either conformable or faulted contacts rials in the rock [Figure 4(E) and (F)]. As to silicon and that deposition was continuous (Yang 1991; Dong replacement, no obvious structural channels for trans- 2004), which is not in accord with the geological fea- portation of hydrothermal fluid developed near the tures of tectonic mélanges or sutures. In contrast, our quartzite, and the mineral compositions seem similar detailed field work has revealed that the strata in the among the wall-rocks which located near or far from MLSZ at Puziba correspond to a tectonic mélange. The the quartzite. matrix of the mélange in the Puziba area consists mainly of plastic mudstone that has been transformed into phyllite. Within this matrix there are blocks of quartzite, 3. Analytical methods slate, marble, metasandstone and chert [Figure 3(A)], 3.1. LA-ICP-MS U–Pb zircon dating defining a typical ‘block-in-matrix’ texture [Figure 3(B)]. In the field, these blocks often show clear boundary Zircons were separated from three quartzite samples with the phyllite matrix, and sometimes they form (SDP-1, SDP-5, and MLH-3) by crushing, sieving, mag- obvious hills in the topography [Figure 4(A) and (B)]. netic, and heavy-liquid separation methods at Langfang The chert formed in the bathyal to abyssal basin in the Geological Service Limited Corporation, Langfang, continental margin (Yang et al. 2015a), while the origi- Hebei, China. More than 250 single zircon crystals from nal rock of quartzite, slate, metasandstone, and marble each sample were handpicked and mounted in an mainly formed in shallow sea environment (Dong 2004). epoxy resin, and then, at Beijing GeoAnalysis Limited Thus, it shows these rock blocks forming in different Corporation, Beijing, polished to expose grain centres. sedimentary setting were involved into the phyllite Subsequently, transmitted and reflected light photomi- matrix as tectonic slices and constituted a tectonic crographs and cathodoluminescence (CL) images of zir- mélange. This tectonic mélange provides new data on con were taken to reveal the external and inner the convergent margin processes associated with the structure for further selection of spot locations

1514 .Z IE AL. ET JI X.-Z.

Table 1. A summary of the tectonic blocks and magmatic rocks in the Mianlue Suture Zone (MLSZ) and Bikou Terrane. Number Lithology Geographical position Tectonic location Rock property Ages and analytic methods References 1 Mafic volcanic rocks Pipasi, Lianghekou MLSZ Tectonic block 783 ± 15 Ma, 754 ± 14 Ma, zircon LA-ICP-MS U–Pb Li et al.(2009) 2 Metamorphic mafic rocks Dabao, northwestern Kangxian MLSZ Tectonic block 812 ± 11 Ma, zircon SHRIMP U–Pb Yan et al.(2007) 3 Metamorphic mafic rocks Xiangziba, northwestern Kangxian MLSZ Tectonic block 841 ± 16 Ma, zircon SHRIMP U–Pb Yan et al.(2007) 4 Metamorphic mafic rocks Shuiquangou, southeastern Kangxian MLSZ Tectonic block 826 ± 19 Ma, zircon SHRIMP U–Pb Yan et al.(2007) 5 Basalt and tuff Huachanggou, western Lueyang MLSZ Tectonic block 802 ± 5 Ma, zircon LA-ICP-MS U–Pb Lin et al.(2013) 6 Plagioclase granite, gabbro Sanchazi, western Lueyang MLSZ Tectonic block 923 ± 13 Ma, 808 ± 10 Ma, zircon SHRIMP U–Pb Yan et al.(2007) 7 Gabbro Xiakouyi, eastern Lueyang MLSZ Tectonic block 815 ± 24 Ma, zircon SHRIMP U–Pb Yan et al.(2007) 8 Quartz diorite, granodiorite Tongchang, southeastern Lueyang Bikou Terrane Intrusive pluton 824, 840, and 879 Ma, zircon SHRIMP U–Pb Wang et al.(2012) 9 Acidic volcanic rocks Tongqianba, southern Kangxian Bikou Terrane Volcanic rocks 790 ± 15 Ma, zircon SHRIMP U–Pb Yan et al.(2003) 10 Basic volcanic rocks Yangba, southern Kangxian Bikou Terrane Volcanic rocks 840 ± 10 Ma, zircon SHRIMP U–Pb Yan et al.(2003) 11 Diorite Guankouya, western Yangpingguan Bikou Terrane Intrusive pluton 884 ± 14 Ma, zircon SHRIMP U–Pb Xiao et al.(2007) 12 Diorite Liujiaping, Yangpingguan Bikou Terrane Intrusive pluton 877 ± 13 Ma, zircon SHRIMP U–Pb Xiao et al.(2007) 13 Gabbro Pingtoushan, southern Bikou Bikou Terrane Intrusive pluton 844 ± 6 Ma, zircon SHRIMP U–Pb Xiao et al.(2007) 14 Acidic volcanic rocks Northern Pingwu Bikou Terrane Volcanic rocks 776 ± 13 Ma, zircon SHRIMP U–Pb Yan et al.(2003) 15 Marine volcanic rocks Longkang-Tazang, western Wenxian MLSZ Tectonic block Late Devonian Yang et al.(1995) 16 Ocean-island basalts Northern Kangxian MLSZ Tectonic block Late Palaeozoic Lai et al.(2003a, 2003b) 17 Ophiolite Sanchazi, western Lueyang MLSZ Tectonic block Late Palaeozoic Li et al.(2003) 18 Island-arc volcanic rocks Sanchazi-Wuliba, western Lueyang MLSZ Tectonic block Late Palaeozoic Lai et al.(2000, 2003a) 19 Bimodal volcanic rocks Heigouxia, western Lueyang MLSZ Tectonic block Late Palaeozoic Li et al.(1996, 2003) 20 Quartzite (metamorphic quartz sandstone) Puziba, northern Wenxian MLSZ Tectonic block Early Devonian This study INTERNATIONAL GEOLOGY REVIEW 1515

Figure 3. (A) Geological map and (B) cross sections of the Puziba area in the MLSZ in the Qinling Orogen (modified from Li et al. 2014; Yang et al. 2015c). Sample locations are shown with blue stars.

Figure 4. Outcrops of metasandstone, marble, and quartzite blocks with phyllite matrix in the MLSZ in the Puziba area. (A and B) Metasandstone and marble blocks fell into the phyllite matrix, and have weathered out as small hills. (C) Shearing of lenticular blocks of quartzite in the phyllite matrix. (D) Quartzite occurs as interlayers in phyllite matrix, showing elongated boudins and shearing. (E and F) Photomicrographs (crossed polarizers) of quartz in the deformed quartzite showing elongated and recrystallized quartz. 1516 X.-Z. JI ET AL.

Figure 5. Cathodoluminescence images (A–C), laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS) zircon U–Pb concordia diagrams (D–F) and histograms of age distribution of detrital zircons (G–I) from quartzite samples collected along the MLSZ. Red circles are the locations of LA-ICP-MS dating, the numbers are ages of the zircons; yellow circles are the spots of Lu–Hf isotopes analyses, the numbers are εHf(t) values of zircons; analytical uncertainties are presented as 1σ.

[Figure 5(A)–(C)]. CL images were obtained on a JXA– et al.(2009). The analytical uncertainties are presented 880 electronic microscope and image analysis software as 1σ. Uncertainties in mean ages are quoted at the 95% under operating conditions of 20 kV and 20 nA at confidence level. Peking University, Beijing. In view of the greater imprecision of 207Pb analysis, The zircons from the three quartzite samples were which will lead to greater imprecision to the 207Pb/206Pb analysed for U, Th, and Pb using the LA-ICP-MS facility age for younger zircons (Spencer et al. 2015), while the at the Hefei University of Technology, Hefei, Anhui, 207Pb/206Pb ages are less sensitive to Pb loss which is China. Laser sampling was performed using a New more common in older system (Gehrels et al. 2008), Wave Research UP 213 laser ablation system. All ana- 207Pb/206Pb ages were taken for old zircons that ages lyses were conducted with a beam diameter of 30 μm, a are more than 1200 Ma, while for younger zircons, we 10-Hz repetition rate, and energy of 2.5 J cm‒2.A used the 206Pb/238Pb ages as their crystallization ages. Thermo Finnigan Neptune MC-ICP-MS instrument was The data discussed in this work are from analyses used to acquire the ion-signal intensities. Reference that displayed <10% discordance (discor. = 100 − 100 × materials 91500 (Wiedenbeck et al. 1995), Plešovice (206Pb/238U ages/207Pb/206Pb ages)0.5, where the age is (Sláma et al. 2008) and SRM610 (Woodhead and Hergt >1000 Ma, and discor. = 100 – 100 × (206Pb/238Pb 2001; Jochum et al. 2011) were used during the ana- ages/207Pb/235U ages)0.5 for ages <1000 Ma), thus avoid- lyses, and they were assessed in two out of every 5–10 ing grains that experienced significant Pb loss during analyses (Liu et al. 2010). The data were evaluated using later events. ICP-MS Data Cal 3.4 (Liu et al. 2010). Concordia diagrams and weighted mean calculations were made using – Isoplot 3 (Ludwig 2003). The detailed operating condi- 3.2. In situ zircon Lu Hf isotopic analyses tions of the laser ablation system and the MC-ICP-MS In situ zircon Hf isotopic analyses were performed on instrument and data reduction are as described by Hou the same zircon grains where U–Pb age determinations INTERNATIONAL GEOLOGY REVIEW 1517 were made using a Nepture MC-ICP-MS equipped with a insignificant age peaks were recognized: one from New Wave UP 193 nm laser ablation system at the 1766 to 1606 Ma (9.7%) and one from 2555 to Laboratory of Isotope Geology, Tianjin Institute of 2420 Ma (6.5%). Geology and Mineral Resources, Tianjin, China. Details Most of the Th/U ratios of zircons from SDP-1 are of the instrumental conditions and analytical proce- >0.1 (0.13–5.20) except for three grains (Supplementary dures for Lu–Hf isotope analyses have been described Table 1), and nearly 80% of the population is >0.4 which by Geng et al.(2011). Energy density of 15–20 J cm‒2, is characteristic of magmatic zircons (Wu and Zheng 10-Hz laser repetition rate, and 55 μm spot sizes were 2004;Li2009). The first group of zircons with ages used during laser ablation. The zircon standard GJ-1 ranging from 597 to 452 Ma show significant oscillatory (Elhlou et al. 2006) was used as the external standard zoning with subangular grain shape [Figure 5(A)], which for in situ Lu–Hf isotopic analyses to check the instru- suggests that the original magmatic zircons were sub- ment reliability and stability (Geng et al. 2011); we used jected to minor erosion and transportation before the 176Lu decay constant of 1.865 ± 0.015 × 10–5 my−1 deposition. The second group of zircons with ages vary- (Scherer et al. 2001), and adopted the chondritic values ing from 1100 to 722 Ma display similar features under of 176Hf/177Hf and 176Lu/177Hf derived by Blichert-Toft CL, although they differ from the first group in the and Albarede (1997). Single-stage model ages were roundness of the grains and oscillatory zoning calculated relative to the depleted mantle with a pre- [Figure 5(A)]. The other two groups of zircons with 176 177 176 177 sent-day ratio ( Lu/ Hf)DM = 0.0384 and ( Hf/ Hf) ages varying from 1766 to 1606 and 2555 to 2420 Ma DM = 0.28325 (Griffin et al. 2000), and the two-stage are more spherical with pitting and are unzoned. The model ages were calculated assuming the 176Lu/177Hf morphology, internal structure, and Th/U ratios of these ratio of average crust is 0.015 (Griffin et al. 2004). zircons are generally compatible with magmatic sources, while the diverse textures are due to differen- tial erosion, transportation and deposition. In general, 4. Analytical results the younger zircons preserve more original magmatic features, whereas the older ones show typical features 4.1. Morphology of detrital zircons in the quartzite of detrital zircons.

Zircon grains from the three quartzite samples were observed under an optical microscope and CL images. 4.2.2. Sample SDP-5 The detrital zircons show length to width ratios ranging Fifty-nine age determinations with absolute concor- from 1:1 to 4:1, and possess low to high degree of dance >90% were obtained on zircons from sample sphericity with subangular to smooth grain contours SDP-5, from which two major age clusters were recog- [Figure 5(A)–(C)]. Most of the zircons show relatively nized [Figure 5(B), (E), and (H)]: (i) a group comprising clear and long columnar crystals and clear oscillatory 10.2% of the total population with ages of 586–543 Ma, zoning, which suggest a magmatic origin [Figure 5(A)– and (ii) a group constituting 25.4% population with ages (C)] (Wu and Zheng 2004;Li2009; Nallusamy 2015). A of 994–907 Ma. Two minor groups, comprising 11.9% few zircon grains are round with pitting and inconspic- population, have ages varying from 1791 to 1609 Ma uous zoning. and 2461 to 2420 Ma. Most of the Th/U ratios of zircons from SDP-5 are >0.1 (0.12–1.96) (Supplementary Table 1), showing fea- 4.2. LA-ICP-MS U–Pb zircon geochronology tures of magmatic zircon (Wu and Zheng 2004;Li 4.2.1. Sample SDP-1 2009). These ratios combined with the clear oscillatory Excluding the detrital zircon grains that show >10% zoning of inner domains [Figure 5(B)] in the two major discordance, 62 age determinations were obtained groups, suggest that these zircons are of magmatic from the quartzite sample SDP-1 [Supplementary data origin. The two minor, older groups of zircons show – Table 1; Figure 5(A), (D), and (G)]. The results fall into moderate to high degrees of rounding and unclear two main groups [Figure 5(D) and (G)]: (i) a group oscillatory zoning, which suggest that the original comprising 12.9% of the population with ages ranging magmatic zircons were transported and eroded before from 597 to 452 Ma and age peaks at 473–452 Ma, and deposition. In summary, most of the detrital zircons (ii) a group comprising 43.6% of the population with from SDP-5 are magmatic in origin, with the older ages ranging from 1100 to 722 Ma and an age cluster at populations showing higher intensities of erosion and 994–830 Ma. In addition, two more age groups with transportation. 1518 X.-Z. JI ET AL.

4.2.3. Sample MLH-3 In contrast to the zircons from sample SDP-1 and SDP-5, the zircon grains from sample MLH-3 can be divided into three groups based on the 68 age determinations [Figure 5(C), (F) and (I)]. The first and most significant group of zircons make up 22.1% of the population and have ages ranging from 469 to 425 Ma, suggesting a different source to the zircons in samples MLH-3, SDP-1, and SDP-5. The second group, constituting 17.6%, has ages ranging from 997 to 830 Ma, while the third group (8.8%) has ages ranging from 2676 to 2611 Ma, and the oldest zircon in this sample has an age of 3513 Ma. Most of the zircons from MLH-3 have Th/U ratios >0.1 (0.1–2.8) (Supplementary Table 1), which suggests a magmatic origin. The internal texture of zircons displays clear oscillatory zoning even though different degrees of rounding are presented from the youngest zircon Figure 6. Histograms of U–Pb ages for (A) zircons from quart- group (469–425 Ma) to the oldest zircon group (2676– zite in the MLSZ in the Puziba area, and detrital zircons from 2611 Ma) [Figure 5(C)]. The grain morphology, internal Devonian sandstones in (B) the South China, and (C) the South Qinling. Data sources: the South Qinling and the South China texture and geochemical features of the zircons indicate Block from Duan (2010), and Duan et al.(2011, 2012). that they are all magmatic in origin, and experienced different degrees of erosion and transportation before deposition. anomalies and negative Eu-anomalies that are typical feature of magmatic zircons (Scharer et al. 2011;Lei 4.2.4. General characteristics of zircon et al. 2013). However, some zircons with low Th/U ratios geochronology (<0.1) also show similar REE patterns to the magmatic

The zircon geochronology of the three samples shows a zircons (Supplementary Figure 1; Supplementary Tables 1 broad similarity in age distribution, and shows similar and 2), indicating that Th/U values or REE patterns are pattern with detrital zircons from Donghe Group in the not conclusive proxies. Besides, there are also several Mianlue Suture (Mao et al. 2013), except those which zircons which show minor differences in their relatively are younger than 400 Ma. In general, the zircons from flat REE distribution pattern and absence of Ce- or Eu- the quartzites possess two primary and two secondary anomalies (Supplementary Figure 1, red marked lines). age peaks (Figure 6). The significant age peaks appear in One of these shows an extremely low Th/U value (0.01; the range of 997–817 Ma (26.5% population) and 597– Supplementary Figure 1B), which may indicate that it is 425 Ma (17.5%), while the other age peaks are at 1791– metamorphic zircons, but the inconspicuous zoning of 1606 Ma (4.8%) and 2676–2420 Ma (11.6%). Overall, the spotting area make it difficult to tell the genesis of the zircon grain morphology, internal structure, and Th/U zircon. In contrast, others show relatively high Th/U ratios (Figure 5(A)–(C); Supplementary Table 1), suggest values comparable to those of magmatic zircons (Wu most of the detrital zircons are magmatic in origin, and and Zheng 2004;Leiet al. 2013). Based on these geo- zircons of different ages underwent different degrees of chemical features in conjunction with grain morphology erosion and transportation prior to deposition. and internal textures, most of the detrital zircons are inferred to be magmatic in origin. 4.3. Trace-element features of zircons 4.4. Zircon Lu–Hf isotopic composition Although the majority of the detrital zircons from the quartzite are of magmatic origin, some grains show the Ninety-two zircons on which LA-ICP-MS U–Pb geochro- effects of metamorphism with metamorphic rims nology has been performed were selected for Lu–Hf around older cores. Here, we use trace elements to isotopic analysis, and the results are listed in distinguish the different types of zircon. Supplementary Table 3. Plots of εHf(t) vs. corresponding Most of the zircons in the three samples display a spot ages [Figure 7(A)] show that the zircons in the similar chondrite normalized rare earth element (REE) three quartzite samples share similar Hf isotopic char- pattern (Supplementary Figure 1), with slight heavy rare acteristic, with a wide range of εHf(t) values from −28.9 earth element enrichment, and strong positive Ce- to 13.0. INTERNATIONAL GEOLOGY REVIEW 1519

C stage model ages (TDM )of3.4–1.8 Ga, indicative of reworked older crust. The data suggest multiple pro- venances for the Neoproterozoic zircons in the quartzite. The zircon cluster with ages from 1791 to 1606 Ma has mostly negative εHf(t) values indicating a reworked older crust (3.0–2.7 Ga). The oldest zircon group (2676–2420 Ma) shows positive and negative εHf(t) values, suggesting derivation from Palaeoarchaean to Mesoarchaean (3.4–3.0 Ga) juvenile sources and reworked crustal components.

5. Discussion 5.1. Depositional time The quartzite blocks in the Sanhekou Group are metamorphosed quartz sandstones that are composed of grains from a variety of sources. Among these, zircon is an extremely robust mineral (Hawkesworth and Kemp 2006) and has been used as an indicator of depositional timing and sedimentary provenance, based on the age distribution and Hf isotopic composition of detrital zircons and the magmatic zircons from source regions (Augustsson et al. 2006; Veevers Figure 7. εHf(t) versus U–Pb age diagram (A) and TDM2 versus et al. 2006). The youngest zircon from the quartzite U–Pb age diagram (B) for detrital zircons from quartzite in the shows relatively high Th/U ratio (0.34) and typical REE MLSZ in the Puziba area. Data sources: the South China Block

patterns of magmatic zircon (Supplementary Tables 1 from Liu et al.(2008), Zeng et al.(2008), Sun et al.(2009), Wang et al.(2010), Zhang et al.(2010), Duan et al.(2011), Nong et al. and 2; Supplementary Figure 1), and has a crystal- (2012), Ping et al.(2014), Wang et al.(2012); the North China lization age of 425 ± 10 Ma. Additionally, the young- Block from Geng et al.(2012), Wu (2014) and references therein; est group of zircons possess ages ranging from 469 to the Qinling Block from Wang et al.(2009a), (2009b), Liu et al. 425 Ma (discordances vary from 1% to 10%), and it (2013). takes up 10.1% of the total detrital zircons in the quartzite. Therefore, it suggests that the sediments should be deposited younger than this age. In addi- Zircon populations in the different age peaks tion, the crystallization age of zircons from granitoid show distinct Hf isotopic characteristics (Figure 7(A) dikes intruded into the metamorphosed sandstones in and (B); Supplementary Table 3). The youngest age this region is estimated as ~215 Ma (Yang et al. peak with ages ranging from 597 to 425 Ma mainly 2015b, 2015c). Furthermore, previous studies of shows negative εHf(t)valuesfrom−0.22 to −28.94 palaeontology (Favosites, Squameofavosites, Icriodus C costatus darbyensis Klapper with two-stage model ages (TDM )of2.4–1.4 Ga, ) define the depositional suggesting a reworked older crust as the magma time of the chert, sandstone and limestone of source. Three exceptions occur with positive εHf(t) Sanhekou Group as Early Devonian (Sheng et al. values from 2.93 to 10.08 and two-stage model ages 1997;Dong2004), which is in accord with our results. C (TDM )of1.3–0.8 Ga, indicative of minor Therefore, we defined the depositional time of the Mesoproterozoic and Neoproterozoic juvenile com- quartz sandstone (protolith of the quartzite) in ponents. The most significant age peak with ages Puziba area as Early Devonian. ranging from 997 to 817 Ma displays relatively complex Hf isotopic features. One-third of the zircons show positive εHf(t) values from 0.2 to 13.04 with 5.2. Source of the quartzite C – two-stage model ages (TDM )of1.5 1.0 Ga, suggest- Zircons have relative high resistance to weathering, ing Mesoproterozoic juvenile components. However, transportation, erosion, and even moderate degrees of more than half of the Neoproterozoic zircons possess metamorphism. Therefore, the detrital zircons from negative εHf(t)valuesfrom−0.7 to −26.9 with two- quartzites can be used to obtain information of the 1520 X.-Z. JI ET AL. source region (Duan et al. 2011; Nallusamy 2015). The marked correlation with the Neoproterozoic zircons quartzite from the MLSZ is near the Qinling, the South from the magmatic and sedimentary rocks in the and North China blocks, thus materials from these three Bikou Terrane belonging to the South China Block. We blocks may be potential contributions to the quartzite. therefore infer that the Neoproterozoic granitoids, vol- More than one quarter of the 997–817 Ma detrital canic and sedimentary rocks of the Bikou Terrane in the zircons of the quartzites in the MLSZ (Figures 5 and 6; northwest of the South China Block provided an impor- Supplementary Table 1) show a wide range in εHf(t) tant depositional source for the quartzite. ratios from −26.9 to 13.04 [Figure 7(A)]. Previous studies The zircon grains with youngest age peak (597– have documented widespread Neoproterozoic mag- 425 Ma) have a wide range of negative εHf(t) values matic events in the Bikou Terrane which has significant from −28.94 to −0.22 which suggests a reworked older affinities with the South China Block (Yan et al. 2003, crust, that could be part of the South Qinling, the North 2004; Xiao et al. 2007; Sun et al. 2009; Wang et al. 2012). China or the South China Blocks. It is more likely that These include volcanic rocks of the Bikou Group (840– the reworked older crust was part of the South China 776 Ma; Yan et al. 2003; Wang et al. 2008), and the Block and the SQB (Zeng et al. 2008; Wang et al. 2010; Dongjiahe ophiolite in the Bikou Terrane Zhang et al. 2010; Nong et al. 2012) because of the (839.2 ± 8.2 Ma; Lai et al. 2007). Furthermore, U–Pb much lower εHf(t) values from the North China Block SHRIMP data on detrital zircons in a volcaniclastic turbi- (Figure 7(A); Wang et al. 2009a , 2009b). Moreover, detri- dite sequence of the Hengdan Group show that sub- tal zircons with ages ranging from 495 to 425 Ma show duction-related magmatism persisted from 850 to good accordance with that from the SQB, while the 700 Ma in the Bikou Terrane (Druschke et al. 2006). others (597–509 Ma) show consistency with detrital The Neoproterozoic age spectra of detrital zircons zircons from the South China Block [Figure 6(A)–(C)]. from the Mianlue quartzites correlate with the ages in Thus, we propose that early Palaeozoic intrusions in the Bikou Terrane and the South China Block (and are the South China Block and the SQB also played an different from the North China Block) [Figure 7(A)], sug- important role in supplying detritus for quartzite in gesting that the zircons were potentially sourced from the MLSZ. magmatic and sedimentary suites (turbidite) in the The Palaeoproterozoic and Archaean detrital zircons

Bikou Terrane and the South China Block. from the quartzite have affinities with both the South The wide variation of εHf(t)(−26.9 to 13.04) in the and North China blocks, indicating a possibly mixed Neoproterozoic detrital zircons from the Mianlue Suture source for the quartzite (Figure 7(A); Liu et al. 2008; quartzites are comparable with the data from previous Geng et al. 2011;Wu2014). However, the negative εHf studies [Figure 7(A)]. Sun et al.(2009) reported ages of (t) values of the zircons mainly show concordance with detrital zircons from the volcaniclastic turbidite those from the South China Block, whereas others show sequence of the Hengdan Group in the Bikou Terrane affinity to those from the North China Block, which has ranging from 910 to 745 Ma with mostly positive εHf(t) mainly positive εHf(t) values [Figure 7(A)]. values suggesting a major event of juvenile magmatism In summary, we propose that the main source of the 2(Figure ), whereas minor zircons with negative εHf(t) quartzite in the MLSZ was Neoproterozoic and values indicate contamination by continental crustal Palaeozoic magmatic and sedimentary rocks in the material. Wang et al.(2012) reported εHf(t) ratios SQB and the South China Block (especially the Bikou (−12.1 to +3.3) from the Neoproterozoic Tongchang Terrane in the northwest of the South China Block), dioritic pluton (Figure 2) at the northeastern margin of whereas mixed sources of Palaeoproterozoic and the Bikou Terrane, and suggested that the pluton Archaean intrusions from both the South and North formed by mixing of magma derived from the depleted China blocks made minor contributions. mantle and the lower continental crust. Ping et al. (2014) reported Hf isotopes from the Neoproterozoic 5.3. Tectonic attribute of the rock associations in Baiquesi and Da’an granitic plutons at the northeastern the Puziba area margin of the Bikou Terrane, and suggested a Mesoproterozoic juvenile crustal source for the Ophiolites, ocean-island basalts, island-arc volcanic rocks, Baiquesi pluton with εHf(t) ratios ranging from 2.0 to and bimodal volcanic rocks are widespread in the MLSZ, 10.4, whereas the Da’an pluton with εHf(t) values of and are potential evidence for an ophiolite mélange and −12.6 to 11.4 was produced by partial melting of the the existence of a former Mianlue Ocean (Yan et al. 2003, mixed Mesoproterozoic juvenile crust and Neoarchaean 2007;Zhanget al. 2003, 2006). Moreover, the strata and crust. Thus, the U–Pb ages and Hf isotope data of the sedimentary systems in the MLSZ also provide important Neoproterozoic detrital zircons from the quartzite show clues in evaluating the tectono-sedimentary evolution of INTERNATIONAL GEOLOGY REVIEW 1521 the suture. Zhang et al.(2003) defined two tectono-sedi- foreland basin, indicating the terminal collision of the mentary systems in the MLSZ: ancient continental margin South and North China blocks. system (S-T1-2) and foreland basin system (T2-K). The The sandstone, chert, limestone and mudstone in the ancient continental margin system includes two evolu- Puziba region were deposited during the Early tionary stages. The first stage is a continental rifting to Devonian as inferred from the geochronology of detrital oceanic basin tectono-sedimentary system (S-C), as indi- zircons (Yang et al. 2015a) and the palaeontology (Dong cated by the Silurian initial rifting and the development 2004). These units belong to the first stage of ancient of an oceanic basin with coarse clastic sedimentary units, continental margin tectonic–sedimentary system, which as well as later fan sedimentary system in the continental is characterized by sedimentation in a continental rifting margin followed by turbidite systems (Yang 1991;Feng setting or oceanic basin (Zhang et al. 2003; Yang et al. et al. 1996;Xue1997;Yanget al. 2015a). According to 2015a). However, our field observations in Puziba sug- QFL (Q, quartzose grains; F, monocrystalline feldspar gest a different scenario. The phyllite matrix (protolith grains; L, unstable polycrystalline lithic fragments) plot of mudstone) in the Puziba area (Figures 3 and 4)is for sandstone (Dickinson et al. 1983), Devonian quartz quite thick, and the quartzite, slate, marble and metasandstone (protolith of the quartzites in this study) is sandstone within phyllite matrix outcrop as blocks and made up of more than 98% quartz from the mineralogi- the strata lack bedding, indicating that these sedimen- cal data under a microscope, indicating the provenance tary rocks which formed in a continental margin system of a craton interior (Figure 8) and a continental margin subjected to later tectonism. Furthermore, in addition to sedimentary setting, thus we inferred that Devonian these blocks, chert blocks, which represent the marine quartzites and chert in Puziba (Ji et al. 2014;Yanget al. rocks of an ophiolite suite, are also found in the phyllite 2015a) and Devonian chert with conodont fossils of matrix in the Puziba area (Figure 3;Yanget al. 2015a). Icriodus costatus darbyensis Klapper in Lueyang (Sheng These field observations indicate that the rocks in the et al. 1997) were deposited during this stage. The second Puziba area belong to a tectonic mélange rather than a stage is a passive continental margin sedimentary (P-T1-2) normal bedded sequence and were formed at a conver- sequence, represented by a shallow–marine argillaceous gent margin associated with ocean–continent subduc- to lime–mud sedimentary basin and carbonate system tion and later continent–continent collision (Collins and on a continental slope and carbonate platform, found Robertson 1997;Raymond2015). They represent the mainly in the west of the MLSZ (Figure 2), suggesting the existence of the MLSZ in the Puziba area, even though shrinking of the ancient Mianlue Ocean (Liu and Zhang no ophiolites or volcanic rocks were found there. 1999). The overlying foreland basin tectono-sedimentary system (T -K) is divided into a marine (Middle-Late 2 5.4. Tectono-sedimentary evolution of the MLSZ Triassic) and continental (Jurassic to Early Cretaceous) Based on this study of the quartzites and previous studies of ophiolites and related volcanic rocks in the MLSZ, the tectono-sedimentary evolution of the MLSZ can be described as follows. The initial opening of the Mianlue Ocean occurred in the early Silurian on the northern margin of the South China Block [Figure 9(A)], as demonstrated by the bimodal volcanic rocks of metabasalts and rhyolites at Heigouxia in the Mianlue Suture (Li et al. 1996) and the widely exposed Silurian alkaline basalts and dikes that were derived from a continental rift in the northern Daba Mountains (Xia et al. 1994;Xuet al. 1997; Zhang et al. 2003), these magmatic rocks were located in both sides of the rift [Figure 9(A)]. The Mianlue Ocean was floored by a mature oceanic crust from the Devonian to mid-Permian [Figure 9(B)], as shown by the typical N-MORB ophiolites at Lianghekou, Kangxian, and Lueyang (Li et al. 1996; Lai et al. 1997;Xuet al. 2000a, Figure 8. QFL plots for framework modes of terrigenous sand- 2000b). Meanwhile, detritus from the Neoproterozoic stones showing provisional subdivisions according to inferred magmatic rocks in the Bikou Terrane and detritus from provenance type (Dickinson et al. 1983). early Palaeozoic magmatic rocks at the northern margin 1522 X.-Z. JI ET AL.

Figure 9. Block diagram showing the tectono-sedimentary evolution of the MLSZ. (A) Rifting took place on the northern margin of the South China Block, leading to the Silurian magmatic event in the Heigouxia and Daba Mountain. (B) The Mianlue Ocean was spreading and became a mature ocean during the Devonian to mid-Permian, while the detritus of Neoproterozoic and Palaeozoic magmatic rocks from the South China Block (mainly the Bikou Terrane) was transported northwards and deposited in the northern continental margin of the South China Block; the chert in the ophiolite suite in the oceanic basin also formed in this period. of the South China Block were transported northwards 6. Conclusion to the northern continental margin of the South China Based on detailed field observations, LA-ICP-MS U–Pb Block during the Devonian and deposited as the mud- geochronology and in situ Lu–Hf isotope data on detri- stone, limestone, sandstone, and quartz sandstone in tal zircons from quartzites, we elucidate the deposi- Puziba, at the same time the chert (the upper layer of tional history and source of the detritus. We also an ophiolite) formed in the deep sea of the Mianlue identify typical block-in-matrix texture of tectonic Ocean [Figure 9(B)]. To the north, the detritus from early mélange sequences in convergent margins. Palaeozoic plutons in the southern margin of the SQB were transported southwards to the southern margin of the block and formed sandstone. Later subduction (1) The quartz sandstone in the Puziba area of the between the Mianlue Ocean and the SQB, and the MLSZ was deposited in the Early Devonian. final collision of the North and the South China Blocks (2) Detrital zircons in the quartzites show typical took place in the Mid–Late Triassic, as witnessed by the magmatic features and four main age peaks at granitoids formed in the subducted, syn-collisional, and 2676–2420 Ma (11.6% of the population), post-collisional processes (Dong and Santosh 2015). As 1791–1606 Ma (4.8%), 997–817 Ma (26.5%), and a result, rock associations of different ages from differ- 597–425 Ma (17.5%). Combined with their zircon ent tectonic blocks (the SQB, the Mianlue Ocean, and εHf(t) values, we propose that the detritus in the the South China Block) were involved in the MLSZ (Yan MLSZ were derived from Neoproterozoic and et al. 2007;Liet al. 2009; Lin et al. 2013), and the main Palaeozoic magmatic and sedimentary rocks in part of the Mianlue tectonic and ophiolite mélange was the SQB and the South China Block (especially formed at this stage. In the Puziba area, the Devonian in the Bikou Terrane, northwest of the South limestone, quartz sandstone and sandstone on the con- China Block), with a subordinate contribution tinental margin of the South China Block and the SQB from Palaeoproterozoic and Archaean intrusions were metamorphosed to marble, quartzite, metasand- in the South and North China blocks. stone and slate blocks, and together with the chert in (3) The association of quartzite, slate, marble, meta- the oceanic basin, were incorporated into the plastic sandstone, and chert blocks within a phyllite phyllite matrix to form the block-in-matrix texture. matrix in the Puziba area constitutes a tectonic Subsequently, the mélange underwent a regional sinis- mélange related to the subduction and collision tral strike-slip event after the terminal collision of the of the South and North China blocks, and is North and the South China Blocks (Chen et al. 2010), critical proof from sedimentary rock blocks rather which reactivated the contact between matrix and than previous ophiolite or volcanic rock blocks and resulted in the shearing and the formation blocks for the existence of the MLSZ in the of lenticular blocks and boudins [Figure 4(C) and (D)]. Puziba area. INTERNATIONAL GEOLOGY REVIEW 1523

Acknowledgements Deng, J., Liu, X.F., Wang, Q.F., and Pan, R.G., 2015a, Origin of the Jiaodong-type Xinli gold deposit, Jiaodong Peninsula, We are grateful to Professor Jun Deng who made constructive China: Constraints from fluid inclusion and C–D–O–S–Sr comments on an early version of our manuscript, Professor isotope compositions: Ore Geology Reviews, v. 65, p. 674– Robert J. Stern who made essential suggestions for improving 686. doi:10.1016/j.oregeorev.2014.04.018. the manuscript, Professor Dilek Yildirim who inspired and dis- Deng, J., Wang, C.M., Bagas, L., Carranza, E.J.M., and Lu, Y.J., cussed with the authors in the field, and Tony Cockbain who 2015b, Cretaceous–Cenozoic tectonic history of the Jiaojia made significant improvement in English. This work was finan- Fault and gold mineralization in the Jiaodong Peninsula, cially supported by the National Basic Research Program of China China: Constraints from zircon U–Pb, illite K–Ar, and apatite (Grant No. 2015CB452605 and 2015CB452606), the National fission track thermochronometry: Mineralium Deposita, v. Natural Science Foundation of China (Grant No. 41030423), the 50, p. 987–1006. doi:10.1007/s00126-015-0584-1. Public Welfare Scientific Research Funding of China (Grant No. Deng, J., Wang, Q.F., Li, G.J., Li, C.S., and Wang, C.M., 2014b, 201411048), the 111 Project under the Ministry of Education and Tethys tectonic evolution and its bearing on the distribu- the State Administration of Foreign Experts Affairs, China (Grant tion of important mineral deposits in the Sanjiang region, No. B07011), and the Geological investigation work project of the SW China: Gondwana Research, v. 26, p. 419–437. China Geological Survey (Grant No. 1212011121090). doi:10.1016/j.gr.2013.08.002. Deng, J., Wang, Q.F., Li, G.J., and Santosh, M., 2014a, Cenozoic tectono-magmatic and metallogenic processes in the Disclosure statement Sanjiang region, southwestern China: Earth-Science Reviews, v. 138, p. 268–299. doi:10.1016/j. No potential conflict of interest was reported by the authors. earscirev.2014.05.015. Dickinson,W.R.,Beard,L.S.,Breakenridge, G.R., Erjavec, J.L., Ferguson,R.C.,Inman,K.F.,Knepp,R.A.,Lindberg,F.A.,and Funding Ryberg, P.T., 1983, Provenance of North American Phanerozoic sandstones in relation to tectonic setting: This work was financially supported by the National Basic North American Phanerozoic Sandstones, v. 94, p. 222– Research Program of China [grant numbers 2015CB452605 235. and 2015CB452606]; the National Natural Science Dong, H., 2004, Disintegration of Sanhekou group of the Foundation of China [grant number 41030423]; the Public Sanhekou area, southern Qinling and its age: Journal of Welfare Scientific Research Funding of China [grant number Stratigraphy, v. 28, p. 59–63. 201411048]; the 111 Project under the Ministry of Education Dong, Y.P., and Santosh, M., 2015, Tectonic architecture

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