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Yan Guo-chuan, Wang Bao-di, Liu Han, He Juan, Peng Zhi-min. 2023. Determination of the early Paleozoic accretionary complex in Southwestern Yunnan, China: Implications for the tectonic evolution of the Proto-Tethys Ocean. China Geology, 6(2), 322‒337. doi: 10.31035/cg2023019.
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Lancang rock group may be Early Paleozoic accretionary complex
The magmatic rocks formed during tectonic activities of the Pan-African and Rodinia supercontinent may provide material for the Langcang rock group
Lancang rock group formed by the eastward subduction of the Changning-Menglian Proto-Tethys Ocean
The Sanjiang Tethys tectonic domain, was formed by the breakup of Gondwana and the subsequent splice of landmass, mainly represented by the remnants of the Changning-Menglian Proto-Paleo Tethys Ocean basin (Pan GT et al., 1996, 2020; Mo XX et al., 1993; Metcalfe I, 2002, 2013; Deng J et al., 2014; Wang BD et al., 2018, 2021; Wang LQ et al., 2021; Sun ZB et al., 2020). The accretionary complex has been paid much attention, because it is the direct product of subduction and collision between plates (Hsü K, 1968; Hamilton W, 1978; Karig DE., 1983; Hsü KJ et al., 1995), which is helpful to explore the oceanic lithospheric subduction and the formation and evolution of continental margin arc-basin system at the plate convergent margin (Isozaki Y et al., 1990; Kusky TM et al., 1999, 2013; Kroner A., 2016; Li J et al., 2016; Zhang KX et al., 2016, 2017; Ren F et al., 2017; Feng YM et al., 2018; Pan GT et al., 2019). The accretionary complex records the evolution of ocean basin, ocean-continent transition and continental crust in orogenic belt (Li JL et al., 2004; Feng YM et al., 2018). The Lancang Group, located between the Changning-Menglian suture zone and Simao block, is an important part of the Sanjiang Tethyan tectonic domain. Recent studies have shown that the Lancang Group is an Early Paleozoic accretionary complex formed by the eastward subduction of the Changning-Menglian Tethyan Ocean (Wang BD et al., 2018; Peng ZM et al., 2022). Due to the complexity of the material composition and structure of the Lancang Group, researchers have been concerned more about its tectonic property.
The Lancang Group, located in the Sanjiang region, is a shallow metamorphic rock interlaced with metamorphic basic volcanic rocks. At present, there are still many disputes about Lancang Group, such as the stratigraphic age, material source, and structural attribute. The stratigraphic age of Lancang Group has been reported from Early to Mesoproterozoic to Devonian (Zhai MG et al., 1990; Zhong DL et al., 1998; Wang F et al., 2017; Peng ZM et al., 2022; Hu JF et al., 2020; Han WW et al., 2020). The provenance of clastic rocks in the Lancang Group is also controversial. Some hold the view that they come from the Simao block (Bureau of Geology and Mineral Resources of Yunnan Province., 1990), while others believe that they come from the Baoshan block (Zhao TY et al., 2017, 2019; Zhou ML et al., 2020; Liu BB et al., 2020; Bai XR et al., 2021; Wei YH et al., 2022), and some think they originated from the North India (Xing XW et al., 2016; Wu GH et al., 2022), and even some scholars express the opinion that they originated from the North India and Austrilia (Xing XW et al., 2016; Wu GH et al., 2022). The tectonic properties are also controversial. Lancang Group is regarded as a continental arc of the Simao Block during the Early Paleozoic by some researchers (Bureau of Geology and Mineral Resources of Yunnan Province, 1990) or as part of the Yangtze basement on the basis of whole-rock Sm-Nd isochron age of 1982 ± 41 Ma from the Huimin volcanic rocks (Zhong DL et al., 1998). Some believe that Lancang Group is a tiny landmass and contains old basement materials (Wang DD et al., 2014; Zhao TY et al., 2019; Wu GH et al., 2022; Wei YH et al., 2022; Liu YM et al., 2019). In recent years, according to the materials in Lancang Group, some scholars have obtained the stratigraphic age of Lancang Group, and think it was formed in the Early Paleozoic, belonging to Proto-Tethys Ocean subduction-accretion orogenic materials (Xing XW et al., 2016; Wang BD et al., 2018; Peng ZM et al., 2022; Hu JF et al., 2020; Han WW et al., 2020; Bai XR et al., 2021). These discrepancies largely reflect the complexities of tectonic history in the region and also highlight the lack of consensus with regard to the age and nature of the Lancang Group.
To address these issues, this study preliminarily determined the Lancang Group material composition by field geological survey, and identified the deformation of the Lancang Group. Meanwhile, we defined the sedimentary age and main material sources of the Lancang Group and analyze their tectonic nature by U‒Pb geochronology, which may provide a basis for elucidating the Tethys tectonic evolution in Sanjiang area.
The Sanjiang area in Southwest China, located in the East Tethyan tectonic domain, is an important region for studying the Tethyan evolution (Liu BP et al., 1993,2002; Zi JW et al., 2012, 2013; Metcalfe I, 2013; Metcalfe CM et al., 2017; Wang BD et al., 2018; Li J et al., 2017; Pan GT et al., 1996, 2012, 2016, 2020; He J et al., 2020; Wang BD et al., 2021; Wang LQ et al., 2021), The region experienced Proto-Paleo Tethys tectonic evolution and accretive orogeny, and later suffered from the Cenozoic Indo-Eurasian plate collision orogeny superposition and transformation (Deng J et al., 2014, 2016; Fig. 1a). Several metamorphic complex belts developed, most of which are distributed north-south along the orogenic belt and have undergone multi-stage metamorphism. The complex belt is adjacent to Lincang-Menghai magmatic arc belt in the east and Changning-Menglian suture belt in the west, which are partially covered by Sanchahe Formation (T3sc) and Huakaizuo Formation (J2h).
The Changning-Menglian Suture Zone runs from Tongchangjie to Yunxian in the North via Shuangjiang and Lancang to Menglian in the south and into Myanmar (Wang BD et al., 2021). There are relatively few complete ophiolite mélanges in the Suture Zone, long considered the location of the Paleo-Tethys Ocean, which opened during the Devonian and closed at least during the Late Triassic. The Changning-Menglian Suture Zone contains ophiolites from Devonian to Carboniferous. MORB-type basalts dated at ca. 385–272 Ma developed in the Suture Zone, along with OIB-Type basalt dated at ca. 307–323 Ma, and the associated siliceous rocks include pelagic assemblages of non-compensatory basin siliceous rocks, which contain radiolaria (Zhang RY et al., 1990; Cong BL et al., 1994; Wang F et al., 2017; Duan XD et al., 2006; Yang WQ et al., 2007; Jian P et al., 2009a, b; Deng J et al., 2014).
The Lincang-Menghai magmatic arc belt lies to its east. This magmatic arc is dominated by Middle-to-Late Triassic magmatic activity (ca. 238–212 Ma), which was formed by continent-continental or arc-continental collision after the closure of the Paleo-Tethys Ocean (Yu SY et al., 2003; Peng TP et al., 2006; Kong HL et al., 2012).
The Lancang Group, located between the Changning-Mengshan zone and the Lincang-Menghai magma arc, starts from Fengqing County in the north, passes through Yunxian County, Lincang County, Shuangjiang County and Lancang County, and reaches Xishuangbanna Prefecture in the south. It is about 400 km long and 25–50 km wide, and extends to Myanmar (Fig. 1b). The east of Lancang Group is in fault and intrusive contact with Lincang compound granites, and is partially covered Sanchahe Formation (T3sc) and Huakaizuo Formation (J2h), the western is in fault contact with Nanduan Formation (D-Cn) (Fig. 2).
In this paper, we selected the northern region of Lancang Group as the research area, and focused on Yunxian County, Yunnan (Fig. 1b). Detailed field geological survey was conducted in Xingfu Town and Nanmei Town (Fig. 2). And nine representative samples were selected for study, including meta-feldspar quartz sandstone (17LC-1, 17LC-2), two mica quartz schist (17-LC-3) and quartz schist (17LC-4) in the Xingfu Town, meta-feldspar quartz sandstone (17LC-6, 17LC-10),Two mica quartz schist (17LC-7, 17LC-9), quartz schist (17LC-5) in the Nanmei Town (Fig. 2). Some typical rocks are as follows.
Meta-feldspar quartz sandstone (17LC-1), green gray, quartz veins are commonly developed in rocks, which are crumpled and strongly displaced by late activity. Quartz veins are mostly extruded to form structural lenses and form “pudding” structure, with uneven size and sand-like structure, massive structure and weak bedding (Figs. 3a, b). Under the microscope, the main minerals are are quartz, feldspar, and biotite. The particle size of quartz debris varies, with a total content of 60%−70% (Fig. 4a).
Two mica quartz schist (17LC-3), gray black, quartz veins are also found in the rock, which are sheared to a structural lenticular body (Figs. 3c, d). Microscopically, the mica was arranged in a directional way. The main minerals were quartz (about 70%), and the secondary minerals were biotite (about 5%–10%) and muscovite (about 15%−20%; Fig. 4b).
Quartz schist (17LC-4), gray and black, quartz veins developed in the rock, which were sheared by later tectonic shear to structural lenticular body with different sizes, generally 5–10 cm. Green schist (metamorphic basalt) was also found, which was produced in structural lenticular body with a long axis of about 2.5 m and a short axis of about 1m, reflecting the metamorphic basalt blocks development in Lancang Group (Figs. 3e, f). Microscopically, the structure was medium to fine granular and massive. It is mainly composed of quartz, muscovite, plagioclase (Figs. 4c, d). The main minerals were quartz (about 40%), and the secondary minerals were biotite and plagioclase muscovite (about 40%).
Zircon was separated at the Geological Laboratory of Langfang Institute of Regional Geological Survey in Hebei Province, China. Zircon U‒Pb isotope results were determined using LA-inductively-coupled plasma mass spectrometry (LA-ICP-MS) at the Experimental Center of Chengdu Geological Survey Center, China Geological Survey (Chengdu, China). LA-ICP-MS zircon U‒Pb analyses were conducted on an Agilent 7500 ICP-MS, equipped with a GeoLas 2005 laser system. Temporal analysis included interpretation of blank signals of 20–30 s and sample signals of 50 s. The detected spot diameter was 32 µm. Detailed instrument operating conditions and data processing methods can be found in Liu YS et al. (2008, 2010), and the results are summarized in Supplementary Table S1.
Zircons older than 1000 Ma were selected as 207Pb/206Pb age, while zircons younger than 1000 Ma were selected as 206Pb/238U age. The results of 8 samples are shown in Supplementary Table S1. The uniformity of zircon particles involved in the age calculation is higher than 90%. The major axis is 200–300 μm, and the minor axis is 100‒150 μm. The length/width of zircon grains is mostly 2∶1. Cathodoluminescence images show that some zircons have clear magmatic rings, some have clear core-edge structures, and some have uniform gray unzoned inner structures (Fig. 5). The U‒Pb ages of the three detrital zircons mainly range from 590–550 Ma, 980–910 Ma, and 1150–1490 Ma, with the youngest detrital zircons having a peak age of about 560 Ma. These zircon grains exhibit a wide range of Th (10×10−6–2125×10−6) and U (26×10−6–2143×10−6) contents, with Th/U ratios generally >0.1. The U‒Pb ages of the six detrital zircons mainly range from 440–460 Ma and 980–910 Ma, and the youngest detrital zircon has a peak age of about 445 Ma, These zircon grains exhibit a wide range of Th (10×10−6–1338×10−6) and U (23×10−6–1627 ×10−6) contents, with Th/U ratios generally > 0.1 (Fig. 6; Supplementary Table S1).
There has been a great dispute about the structural attribute of Lancang Group. It is traditionally believed that the Lancang Group was a part of the Simao block during Paleozoic, representing a continental arc (Bureau of Geology and Mineral Resources of Yunnan Province, 1990; Metcalfe I, 2013; Metcalfe CM et al., 2017; Wu HR et al., 1994) or an allochthonous microcontinent accreted to the latter during the Late Permian (Feng QL et al., 1996; Jia HR, 1994; Liu BP et al., 1993; Zeng WT et al., 2017). But recent studies believe that the Lancang Group is a geological record of the subduction and extinction of the Proto-Paleo Tethys Ocean, with the characteristics of accretionary complex (Wang BD et al., 2018; Pan GT et al., 2019; Hu JF et al., 2020; Peng ZM et al., 2022; Han WW et al., 2020). Generally speaking, the accretionary complex and ophiolites coexist closely in the orogenic belt, which is considered to be the final location of subduction and extinction of the oceanic basin (Isozaki Y et al., 1990; Shervais JW, 2006), and are composed of different types and ages rocks intermingled by many secondary deformations and metamorphic processes. In the Lancang Group, strongly deformed basalt, greenschist and other rocks develop as block (Fig. 2), with oceanic crust and magmatic arc characteristic. Due to multiple periods tectonic action, it is difficult to recognize the boundary between most blocks and surrounding rocks, but overall with “matric+block” feature (Fig. 2). The accretionary complex is associated with high-pressure metamorphic rocks (blue schist, eclogite), and the space-time distribution of blue schist and eclogite is an important symbol of plate convergence boundary, ocean subduction and continental collision, recording the entire process of subduction and reentry (Zhang LD et al., 2008). More and more blueschist and eclogite have been found in the Lancang Group. The protolith of blueschist has the arc volcanic rocks characteristics, and eclogite has E-MORB and OIB properties (Fan WM et al., 2015; Wang F et al., 2016; Wang HN et al., 2018). And for high-pressure metamorphic rocks, the protolith forms in different ages, the eclogite formed at different time, including 801 Ma, 451 Ma, 429–463 Ma (Li J et al., 2017; Sun ZB et al., 2017a, b; Wang HN et al., 2018; Wang HN et al., 2018), which is consistent with the age of the oceanic crust in the Changning-Menglian Suture Zone (Wang BD et al., 2013, 2018; Wang F et al., 2016; Sun ZB et al., 2017a, b; Liu GC et al., 2017,2021; Peng ZM et al., 2018, 2019).The results indicate that the protoliths of the high pressure metamorphic rocks in this zone are complex and diverse, which represent the subduction, extinction and accretion orogenic processes of the Changing-Menglian ocean, and the Lancang Group has undergone deep subduction, and the blue schist and eclogite have returned to their positions by arc-continental and continent-continental collision.
In addition, in terms of deformation, previous studies on the accretionary complex have found that it generally has the structure form of mutual shear between matrix and block, as well as dual structure and thrust imbriculate assemblage structure, thus forming a series of structural zones, including thrust faults and different types folds (von Huene R et al., 1994; Taira A, 2001; Niitsuma N, 2004). Some imbricate thrust nappe faults with a tendency to the west are mainly developed on the west side of Lancang Group, and there are shear deformation and detachment deformation structures in the thrust fault zones, and some different types of folds can be seen (Fig. 2). And in its east, the main structure is imbricate thrust nappe with east tendency, and the thrust slices are dominated by broad and gentle structures (Fig. 7). Due to the superposition of multi-stage metamorphism and deformation, a series of asymmetric shear rheological quartz veins can be seen (Fig. 8).
In conclusion, according to the material and deformation characteristics of the Lancang Group, it is believed that the material composition of the Lancang Group is complex and diverse, and the rocks with different properties and ages have undergone late metamorphic deformation and transformation, and the present thrust faults from east to west are developed, and the overall performance is characterized by thrust-nappe and accretive structure. We believe that it has similar characteristics to accretionary complex belt, and its primary structure and sedimentary characteristics have been changed by the later tectonic activities, and it is composed of different lithologic fragments by collage and accumulation. Based on the above and features in the zone, we hold the opinion that Lancang Group is an Early Paleozoic accretionary complex, formed by Changing-Menglian Proto-Tethys Ocean eastward subduction, collision, orogenic, instead of basement rock series or continental blocks, and some basement rock series are likely to be involved in the Changing-Menglian Proto-Tethys Ocean evolution process and mixed into the Lancang Group by the late tectonic movement.
There are many studies on Lancang Group material, mainly including sericite quartz schist, dolomite quartz schist, sericite microcrystalline schist, phyllite and slate, with local iron, phosphorus and siliceous rocks in the Lancang Group. The protolith is feldspar-bearing quartz sandstone, feldspar-quartz sandstone, argillaceous sandstone, siltstone, shale and carbonaceous shale, with flysite characteristics. It is considered as basement metamorphic rocks (Bureau of Geology and Mineral Resources of Yunnan Province, 1990; Zhang RY et al., 1990; Zhai MG et al., 1990; Zhong DL et al., 1998; Wang Q et al., 2014; Zhao TY et al., 2019; Wu GH et al., 2022; Wei YH et al., 2022; Liu YM et al., 2019). However, as intensive study grows in recent years, some new rocks such as blueschist and eclogite have been discovered in the zone (Peng ZM et al., 2019, 2022), and a new understanding of the material composition of the Lancang Group has been gained. Based on previous data and field surveys, this study suggest that: The Lancang Group is an intermediate and shallow metamorphic rock with different lithologic assemblages. The metamorphism grade is proved to be low greenschist facies, low amphibolite facies, blue schist facies and eclogite facies. The material composition of Lancang Group is diverse and complex, covering shallow metamorphic rock series with metamorphic basic volcanic rocks. The main types include mica quartz schist, two mica schist and other metasandstone (Fig. 3); The chlorite albite schist, chlorite two-mica schist and other metamorphic medium acid volcanic rock (Xu YF et al., 2018); green schist, albite schist, amphibolite and other metamorphic mafic-medium volcanic rocks; locally developed metamorphic intermediate-acid intrusive rocks such as granitic gneiss and albite shallow granulite (Han WW et al., 2020; Hu JF et al., 2020), low temperature and high pressure metamorphic rocks such as blue schist and eclogite, and a small amount of marble and carbonaceous quartz schist (Peng ZM et al., 2019, 2022). Metamorphic acidic volcanic rock, basic volcanic rocks, intermediate-acid intrusive rocks and high-pressure metamorphic rocks are exposed in the form of tectonic lens in schist, rendering melange typical structure characteristics of the “block + matrix”. Matrix in our study area includes various types of schist, and block mainly includes metabasalt (Fig. 3).
Compared with Lincang granite chronology, the study on the sedimentary age of Lancang Group is relatively weak. The Lancang Group was named by the survey team of Yunnan Geological Bureau, belonging to Cambrian or Early Cambrian. Later, some researchers classified it as Paleoproterozoic or Mesoproterozoic (Bureau of Geology and Mineral Resources of Yunnan Province, 1990). Wei GY et al. (1984) also believed that the Lancang Group belonged to the Paleoproterozoic, possibly partly to the Cambrian, on the grounds of paleo-algae and micropaleo-plant fossils. In the recent years, some think the depositional time of the Lancang Group should be Early Paleozoic according to the detrital zircons and metavolcanite age in the Lancang Group (Wang F et al., 2017; Wang HN et al., 2018; Xu YF et al., 2018; Peng ZM et al., 2022; Hu JF et al., 2020; Han WW et al., 2020; Wei YH et al., 2022).
In this research, we obtained the ages of detrital zircons of nine rocks in the Lancang Group. In general, the youngest detrital zircon ages of sedimentary strata can represent the oldest ages of sedimentary strata (Andersen T, 2005). The U‒Pb ages of the three detrital zircons mainly range from 590–550 Ma, 980–910 Ma, and 1150‒1490 Ma, with the youngest detrital zircons having a peak age of about 560 Ma. The U‒Pb ages of the six detrital zircons mainly range from 440–460 Ma and 980–910 Ma, and the youngest detrital zircon has a peak age of about 445 Ma (Fig. 6). This is consistent with recent findings (Wang F et al., 2017; Xu YF et al., 2018; Peng ZM et al., 2022; Wei YH et al., 2022). This is in line with recent findings by Nie XM et al (2015), LA-ICPMS U‒Pb chronology of zircons in three metamorphic volcanic rocks from Huimin formation of Lancang Group was conducted, and the ages of 456 ± 3 Ma, 456 ± 7 Ma and 459 ± 14 Ma were obtained, respectively. Xing XW (2016) also conducted a chronological study on two metamorphic volcanic rocks in the Lancang Group, and obtained U‒Pb ages of 462 ± 6 Ma and 454 ± 27 Ma, respectively. Han WW (2020) obtained an age-weighted average age of 476.5±1.6 Ma for the formation of Albite shallow granulite from Lancang Group by zircon U‒Pb dating, and Hu JF (2020) obtained an age of 474.1 ± 1.7 Ma for the formation of albite-actinolite-schist from Lancang Group. The metavolcanic rocks samples (about 495 Ma) in the Manlai Formation, five metavolcanic samples from the Huimin Formation yielded zircon U‒Pb ages between 478±5 Ma and 442 ± 5 Ma (Wei YH et al., 2022), and Liu BB (2020) obtained the age of volcanic rocks in Manlai Formation of Lancang Group was 494‒495 Ma (Fig. 1). Combined with previous research results, the Lancang Group was inferred to formed in the Late Ordovician, or Early Paleozoic.
The distribution patterns of U‒Pb ages recorded in detrital zircon grains are helpful for seeking for the source regions and are widely used to probe sediment provenance (DeCelles PG et al., 2000; Chen FK et al., 2021; Zhu DC et al., 2011a; Nebel O et al., 2014). And detrital zircons clustered mainly around 520‒550 Ma in the Lancang Group (Fig. 9). Zircon grains with U‒Pb ages <500 Ma largely retain oscillatory zoning and show euhedral to subhedral shape (Fig. 5), indicating a magmatic texture and short-distance provenance. The Early Paleozoic rocks (about 450 Ma), including granitic gneiss and some granitoid rocks that intruded into the Paleozoic sedimentary rocks in the Lancang Group and adjacent Baoshan block, respectively (Chen F et al., 2007; Peng ZM et al., 2018; Zhao TY et al., 2019; Han WW et al., 2020), could be potential sources for the youngest (about 445 Ma) sedimentary materials. However, igneous rocks older than 500 Ma have not been reported in the Lancang Group or adjacent blocks. What is noteworthy is that some zircon grains older than 500 Ma in the Lancang Group are nearly circular or short columnar in shape, indicating long-distance transportation or recycling of sediments. In this paper, Lancang samples show a clear age peak between about 550 Ma and 520 Ma (Fig. 10), which is distinctly different from the peak age of about 500 Ma to 400 Ma in the Yangze and Huaxia block (Fig. 9; Xia XP et al., 2016; Chen Y et al., 2017; Yang L et al., 2018). However, there are several orogenic belts related to 620–520 Ma Pan-African magmatic activity in East Gondwana, including the Kuunga (between India and West Australia) and Pinjarra (between West Australia and Antarctic) (Fitzsimons ICW, 2000; Goscombe B et al., 2020), and detrital zircons of this period also exist in the Baoshan block, Lhasa block, Tethyan Himalayan, and West Australian block (Fig. 9; Cawood PA and Nemchin AA, 2000; Veevers JJ et al., 2005; Gehrels GE et al., 2006; Pullen A et al., 2008; Myrow PM et al., 2009, 2010; Zhu DC et al., 2011b; Chen FK et al., 2021; Li DP et al., 2015). So, according to the age correlation of detritonal zircons in the Lancang Group, the provenance of the Lancang Group may be different from the Lanping block. The Lancang Group was likely adjacent to the Gondwana continent during the Early Paleozoic and received a large amount of Pan-African material (Fig. 10).
Notably, the Lancang Group contains many detrital zircons cluster of 910 Ma to 1100 Ma and 1150 Ma to 1490 Ma, with peaks at about 960 Ma and about 1168 Ma (Fig. 9). The Grenvillian orogens are commonly exited in the East Gondwana, including the 1330–1130 Ma Albany-Fraser (Australia)-Wilkes (East Antarctic) belt (Cawood PA and Nemchin AA, 2000; Clark DJ et al., 2000; Veevers JJ et al., 2005), the 1090‒1030 Ma Namaqua-Natal (Africa)-Maud (East Antarctic) belt (Eglington BM, 2006; Ksienzyk AK and Jacobs, 2015; Hokada T et al., 2019), and the 990‒900 Ma Eastern Ghats (India)-Rayner (East Antarctic) belt (Boger SD et al., 2000; DeCelles PG et al., 2000; Fitzsimons ICW, 2000; Halpin JA et al., 2012; Fig. 10). So, the Eastern Ghats-Rayner belt in India may have provided abundant sedimentary materials of about 910–1100 Ma of the Lancang Group likely with some contribution of about 1150–1490 Ma materials from the Albany-Fraser belt in West Australia.
The detrital zircon age cluster of 2600 Ma to 2400 Ma are generally present in the detrital zircon age maps (Fig. 9), the Lancang Group, similar to the Baoshan, Southern Qiangtang, Himalayan and Indian blocks, has a peak age of younger than 2500 Ma, while the Western Australia and Lhasa blocks have a peak age of about 2700 Ma. In the Aravalli Craton and the Bundelkhand Massif of Northern India, magmatic activity occurred in the ca. 2500 Ma (Wiedenbeck M et al., 1996; Mondal MEA et al., 2002; Wang W et al., 2019), while the magmatic activity is about 2800‒2600 Ma in the Yilgarn Craton of Australia (Pidgeon RT and Wilde SA, 1990; Griffin WL et al., 2004). In general, the North India might have provided Late Neoarchean and Early Paleoproterozoic components for the Lancang Group (Fig. 10).
Above all, the U‒Pb ages presented in this paper suggest that the Lancang Group has different origins and complex provenance. this paper proposes that in the Early Paleozoic the Lancang Group mainly received material composition from India and their adjacent cratons, they are similar to the detrital zircons in the metassedimentary rocks or strata of Baoshan block, the Southern Qiangtang block, Tethys Himalayas, and may have the same source.
(i) Combined with the material and deformation characteristics of the Lancang Group, the Lancang Group may be accretionary complex, overall with matric+block feature, which is the material record of subduction of Proto-Paleo Tethys Ocean.
(ii) The youngest detrital zircon in the Lancang Group has a peak age of about 445 Ma, which indicates that the depositional age should be no earlier than the Late Ordovician, Combined with volcanic rocks U‒Pb age in the Lancang Group, the accretionary complex of Lancang Group may form in the Early Paleozoic.
(iii) The sedimentary sources of the Lancang Group metamorphic rocks may be mainly magmatic rocks formed during the polymerization and cleavage of the Pan-African and Rodinia supercontinent. The age distribution characteristics of detrital zircons in Qiangtang, Tethys Himalayan and Baoshan block metassedimentary rocks or strata are compared with those in the Lancang Group, suggesting that they may have similar source.
Supplementary data (Table. S1) to this article can be found online at doi: 10.31035/cg2023019.
This research was supported by the Second Comprehensive Scientific Investigation and Research Program on the Qinghai-Tibet Plateau (2019QZKK0702), the China Geological Survey Program (DD20221715, DD20190053).
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