Provenance and tectonic settings of Late Triassic–Jurassic deposits in the southwestern margin of the Yangtze Block: Evidence from whole-rock elemental compositions and detrital zircon U‒Pb ages and Hf isotopes, SW China

Provenance and tectonic settings of Late Triassic–Jurassic deposits in the southwestern margin of the Yangtze Block: Evidence from whole-rock elemental compositions and detrital zircon U‒Pb ages and Hf isotopes, SW China | Research Square window.SnipcartSettings = { analytics: { enabled: false } }; (function() { var accessVector = localStorage.getItem('access_vector') || ''; window.dataLayer = window.dataLayer || []; if (accessVector) { window.dataLayer.push({ user: { profile: { profileInfo: { snid: accessVector } } } }); } })(); (function(w,d,s,l,i){w[l]=w[l]||[];w[l].push({'gtm.start':new Date().getTime(),event:'gtm.js'});var f=d.getElementsByTagName(s)[0],j=d.createElement(s),dl=l!='dataLayer'?'&l='+l:'';j.async=true;j.src='https://www.googletagmanager.com/gtm.js?id='+i+dl;f.parentNode.insertBefore(j,f);})(window,document,'script','dataLayer','GTM-K279D39R'); Browse Preprints In Review Journals COVID-19 Preprints AJE Video Bytes Research Tools Research Promotion AJE Professional Editing AJE Rubriq About Preprint Platform In Review Editorial Policies Our Team Advisory Board Help Center Sign In Submit a Preprint Cite Share Download PDF Article Provenance and tectonic settings of Late Triassic–Jurassic deposits in the southwestern margin of the Yangtze Block: Evidence from whole-rock elemental compositions and detrital zircon U‒Pb ages and Hf isotopes, SW China Shengyang Yao, Qiyu Wang, Chuanlong Mou, Peng Ren, Bowen Zan, and 3 more This is a preprint; it has not been peer reviewed by a journal. https://doi.org/ 10.21203/rs.3.rs-5860486/v1 This work is licensed under a CC BY 4.0 License Status: Published Journal Publication published 02 Jul, 2025 Read the published version in Scientific Reports → Version 1 posted 7 You are reading this latest preprint version Abstract During the Late Triassic to Jurassic, the western Yangtze Block transitioned from marine carbonate deposits to terrestrial detrital deposits. There are different views on the orogen evolution of the western margin of the Yangtze Block, such as whether the Longmenshan Thrust Belt was uplifted in the Late Triassic or Early Jurassic, and when the Yangtze Block began to receive the source from Yidun Terrane. In this paper, whole-rock elemental compositions and zircon U–Pb ages and Hf isotope data from the Upper Triassic to Jurassic successions are introduced. The whole-rock elemental compositions reveal that the clastic rocks were deposited in a collisional setting and were derived mainly from intermediate–felsic magmatic rocks and recycled sediments. The Upper Triassic zircon sample shows a single age peak at ~831 Ma. The three Jurassic samples show similar age patterns with four main age populations (e.g., 200–500 Ma, 788–834 Ma, 1863–1875 Ma, and 2462–2531 Ma). The results revealed that the Kangdian Palaeo-land was the main provenance area in the Late Triassic. In contrast, in the Early Jurassic (~198.7 Ma), the Longmenshan was massively uplifted, and the recycled sediments from the Longmenshan, Songpan–Ganzi Terrane and Yidun Terrane provided large amounts of detrital material to the southwestern Yangtze Block. Volcanic rocks from the Yidun Terrane also provided a partial source for the southwestern Yangtze Block. In the Middle Jurassic, owing to the weathering and erosion of the Longmenshan Thrust Belt in the Early Jurassic, the provenance supply in Longmenshan decreased, and the provenances from the Yidun Terrane and the Songpan–Ganzi Terrane increased. In the Late Triassic to the Early Jurassic, the tectonic setting of the southwestern Yangtze Block may have changed from a passive continental margin to a foreland basin. Earth and environmental sciences/Solid earth sciences/Geology Earth and environmental sciences/Solid earth sciences/Petrology Earth and environmental sciences/Solid earth sciences/Sedimentology Whole-rock elemental compositions Detrital zircon Hf isotopes Provenance SW Yangtze Block Figures Figure 1 Figure 2 Figure 3 Figure 4 Figure 5 Figure 6 Figure 7 Figure 8 Figure 9 Figure 10 Figure 11 Figure 12 Figure 13 Figure 14 Figure 15 1. Introduction Owing to the uplift of the Qinling Orogenic Belt (QOB) and Longmenshan Thrust Belt (LTB), the Sichuan Basin (SCB) on the western margin of the Yangtze Block (YZB) changed from a marine environment to a continental sedimentary setting. Many clastic rocks were deposited in the SCB. In the western part of the SCB, the foreland basin has developed and evolved. The sediments in the foreland basin can reflect the orogen process of the orogenic belt around the foreland basin. Orogenic belts significantly influence sedimentary rocks in basins, which offers valuable insights into the history of adjacent mountain belts (Sircombe and Freeman, 1999 ; Kelty et al., 2008 ; Luo et al., 2014 ; Li et al., 2018 ). By analyzing the Mesozoic clastic rock sediments in the SCB, the evolution of the peripheral orogenic belt can be predicted, such as the QOB and LTB. However, opinions differ on the orogenic belts that controls the Sichuan foreland basin. Some scholars believe that the western Sichuan foreland basin was controlled by the QOB, its main provenance was the QOB in the north, and the LTB was not uplifted in the Late Triassic. The SCB is connected to the entire Songpan-ganzi Thrust Belt (SGT) in the west (Ma et al., 2009 ; Deng et al., 2012 ; Mei, 2014 ; Luo et al., 2014 ; Yu, 2016 ; Zhu et al., 2017 ; Yu and Liang, 2017 ; Mu et al., 2019 ; Mu, 2020 ). Other scholars believe that during the Late Triassic Indosinian movement, owing to the southeastward thrusting activity of the SGT, the LTB formed; that is, in the Late Triassic, the western Sichuan foreland basin was controlled by the uplift of the LTB and was the main provenance area (Ratschbacher et al., 2003 ; Meng et al., 2005 ; Zheng et al., 2008 ; Shi et al., 2010 ; Li et al., 2014 ; Chen et al., 2016a ; Chen et al., 2021 ; Lu et al., 2023 ; Gou et al., 2024 ). Several scholars believe that the western SCB area was influenced by the Kangdian Paleo–Land (KPL) and the Emeishan Large Igneous Province (ELIP) in the Triassic (Zhu et al., 2017 ; Zhang et al., 2021 ). Moreover, it is doubtful whether the closing time of Songpan-Ganzi Ocean of the eastern branch of the Paleo-Tethys Ocean is Middle Triassic, Late Triassic or Early Jurassic (Li and Liu, 2015 ; Jian et al., 2019 ; Jackson et al., 2020 ; Xu et al., 2021 ; Yan et al., 2022 , 2024 ). When the Sichuan Basin began to receive the provenance supply from Yidun Terrane (YDT) can provide constraints for the closure of Songpan-Ganzi Ocean. Therefore, this study may also provide sedimentary evidence for the evolution of the eastern side of the Paleo-Tethys Ocean. The detrital zircons that are preserved during weathering, transport, and sedimentation are key minerals for investigating provenances and understanding regional tectonics. U–Pb geochronology plays an important role in understanding many sedimentary geological processes (Li et al., 2010a ; Zhang et al., 2015 ; Shao et al., 2016 ; Li et al., 2018 ; Liu et al., 2020 ). Moreover, zircon Hf isotopes can indicate sediment provenances more precisely. Detrital zircon U–Pb ages and Hf isotope characteristics are widely used to indicate the tectonic history of rocks (Wu et al., 2006 ; Zhou et al., 2016a ). When analysing many detrital zircons, these methods can be utilized to examine the provenance (Cawood et al., 2007 ; Condie et al., 2009 ; Hui et al., 2017 ). The whole-rock elemental compositions of terrigenous clastic rocks are also widely used to determine potential provenances. Some stable elements, such as SiO 2 , Al 2 O 3 , TiO 2 , K 2 O, Fe 2 O 3 , MgO, La, Th, Co, Y, Zr, Sc, Hf, and rare earth elements (REEs), could be good indicators for constraining the nature of clastic rocks and tectonic settings (Bhatia and Crook, 1986 ; Floyd and Leveridge, 1987 ; Girty, 1996; Hayashi et al., 1997 ; Fralick and Kronberg, 1997 ; Cullers, 2000 ; Paikaray et al., 2008 ; Ma et al., 2019 ; Xia et al., 2021 ; Zhang et al., 2022a ). Using the zircon U‒Pb ages and Hf isotope data from the detrital zircons obtained from the Triassic Xujiahe Formation and the Jurassic Ziliujing Formation, Shaximiao Formation and Suining Formation in the southern part of the western SCB, combined with results from previous studies, we analysed the provenance and evaluated the structural characteristics of the southwestern YZB during the Late Triassic to Jurassic period. 2. Geological setting The YZB is located in the west of the South China Block (S-CB), with the QOB and North China Block (N-CB) to the north, SGT to the west, Indochina Block to the south, and Jiangnan Orogenic Belt and Cathysia Block to the east. Located in the western part of the South China Block (S-CB) and YZB (Fig. 1 A), the SCB is a large, complex superimposed basin that developed in the Precambrian crystalline basement (Zhang, 2002 ; Shen et al., 2009 ). Owing to the transitional position between Gondwana and Laurentia, complex basins formed (Ren, 1996 ; Li et al., 2006 ). Its western margin is separated from the SGT in the west by the LTB (He, 2014 ) and in the north by the QOB and the N-CB (Hao et al., 2008 ; Liu et al., 2021a ). 2.1 Qinling Orogenic Belt (QOB) The QOB is an east‒west-trending orogenic belt with a length of approximately 1600 km and is located between the SCB and the NCB (Dong et al., 2022 ) (Fig. 1 A, B); it can be divided into the North Qinling Orogenic Belt (NQB) and the South Qinling Orogenic Belt (SQB) by the Shangdan suture belt (Dong et al., 2011a ; Zhang et al., 2015 ). The QOB evolved from the northernmost Paleo-Tethys Ocean (Chen and Santosh, 2014 ; Zhou et al, 2016a ). The QOB underwent two major stages of geological evolution after the formation of igneous rocks and migmatites in the late Archean–Neoproterozoic (Meng and Zhang, 2000 ): (a) in the Late Neoproterozoic to Middle Triassic, the South QOB and North QOB contained passive continental margin deposits in the northern and southern parts of the YZB and the NCB, respectively; (b) the Late Triassic orogeny was characterized by the development of thrust faults and foreland basins under the convergent setting of the SCB and NCB (Liu, 2006 ; Enkelmann et al., 2006 ; Chen, 2011 ; Tian et al., 2012 ; Wang et al., 2015 ; Chen et al., 2015 ). The SQB is mainly composed of Precambrian metamorphic crystalline basement (including gneiss, amphibolite, schist, quartzite) (~ 2500 Ma, ~ 744 Ma), Paleozoic clastic rocks (~ 445 Ma), and Triassic volcanic rocks (~ 224 Ma) (Dong et al., 2011a , b ; Dong et al., 2013 ; Hu et al., 2013 ; Li et al., 2018 ). The NQB is mainly composed of Paleoproterozoic and Neoproterozoic ophiolite suites, gneiss, marble and amphibolite, Neoproterozoic metamorphic rocks, metamorphic sedimentary rocks, Early-Paleozoic ophiolite, metamorphic rocks, granite, gabbro, basalt, andesite, ultrabasic rocks and clastic rocks (~ 2510 Ma, ~ 1462 Ma, ~ 937 Ma, and ~ 403 Ma), and Triassic volcanic rocks (~ 206 Ma) (Dong et al., 2011a , b ; Li et al., 2018 ). 2.2 Longmenshan Thrust Belt (LTB) The LTB extends from northeast to southwest and is approximately 500 km long. It is adjacent to the QOB in the north and the SGT in the middle and southern regions (Fig. 1 B) (Yan et al., 2011 ; Mu et al., 2019 ). After the Archean–Paleoproterozoic or Neoproterozoic basement formed (Zhao and Zhou, 2008; Dong et al., 2011b ; 2012 ; Deng et al., 2012 ; Meng et al., 2015 ), the LTB experienced two main stages of geological evolution: (a) a pre-Sinian to Triassic craton in a continental passive margin and (b) a Late Triassic orogenic stage that was characterized by the development of thrust faults, strike-slip faults and foreland basins under a compressional tectonic setting (Deng et al., 2012 ). The LTB can be further divided into northern, central and southern segments (Li et al., 2008 ; Jin et al., 2009 ), and the Jiaoziding complex, Pengguan complex and Baoxing complex usually form the core. The formation time of these complexes is mainly Neoproterozoic, and the lithology is mainly composed of granite, diabase, gabbro, metamorphic sedimentary rock, metamorphic volcanic rock (Lu, 2011 ; Yan et al., 2008 ; Li, 2014 ). The LTB is mainly composed of Precambrian clastic rocks (~ 743 Ma, ~ 849 Ma, and ~ 940 Ma) and Paleozoic clastic rocks (~ 500 Ma, ~ 950 Ma, and ~ 2500 Ma) (Duan et al., 2011 ; Chen et al., 2016c ; Mao et al., 2021 ). The LTB experienced many periods of conversion from a subsidence area to a denudation area due to changes in sea level in the Paleozoic. The most recent transition to denudation before the Triassic occurred in the early Permian (Ma et al., 2009 ; Zheng et al., 2010; Mou et al., 2016 ). 2.3 Songpan–Ganzi Terrane (SGT) The SGT is a triangular fold belt (Fig. 1 B) (Ding et al., 2013 ), the southern side of which is called the Ganzi–Litang area. The SGT consists of pre-Sinian crystalline basement and Sinian-Paleozoic sedimentary strata, which are covered with extremely thick Triassic turbidite sedimentary strata (Roger et al., 2004 ; Xiao et al., 2007 ). The major provenance area of the extremely thick Triassic turbidite deposits in Songpan-Ganzi Terranes is the Qinling Orogenic Belt (Bruguier et al., 1997 ; Roger et al., 2004 ; Weislogel et al., 2006 , 2010 ; Xiao et al., 2007 ; Luo et al., 2014 ; Mu et al., 2019 ). In the Late Triassic or later, due to the mutual squeezing between the YZB, NQB and SQB, the closure of the Paleo-Tethys Ocean led to shallow water depth in the SGT, and the flysch basin evolved into a fold belt during the Indosinian period, forming an orogenic belt (Sengör, 1985 , Nie et al., 1994 ; Mei, 2014 ; Yan et al., 2018 ; Yan et al., 2019 ; Mu et al., 2019 ). The SGT is mainly composed of large Triassic flysch deposits (greater than 10 km) (Liu et al., 2015 ; Mu et al., 2019 ) with multiple age peaks at ~ 266 Ma, ~ 438 Ma, ~ 824 Ma, and ~ 1822 Ma (Chen et al., 2009 ) and a small amount of high-potassium calc-alkaline granite with an age of 215 ± 3 Ma (Yuan et al., 2010 ). 2.4 Yidun Terrane (YDT) The YDT is tectonically located between the SGT and YZB (Fig. 1 B). The YDT and YZB have similar sedimentary strata and paleontological fossils from the Neoproterozoic and Paleozoic eras. The YDT has structural properties that are similar to those of the YZB (Song et al., 2004 ). Before the Paleozoic, the YDT consisted mainly of medium–acid volcanic rocks and metamorphic clastic rocks, in the Paleozoic, it consisted mainly of carbonate rocks and volcanic rocks (Tian et al., 2023 ). During the Middle Triassic to Late Triassic, owing to the westwards subduction of the SGT, the YDT formed many types of volcanic rocks in the island arc area, including basalt, andesite, dacite, rhyolite and intermediate-acid magmatic intrusive rocks (Li and Liu et al., 2015 ; Wang et al., 2017 ). The peak ages of the clastic rocks in the YDT and SGT are similar (~ 242 Ma, ~ 438 Ma, ~ 786 Ma and ~ 1810 Ma) (Wang et al., 2013a ; Wu et al., 2016 ; Liu et al., 2021b ), and the peak ages of the volcanic rocks are ~ 225 Ma and ~ 216 Ma (Peng et al., 2014 ). 2.5 Kangdian Paleo–land (KPL) The KPL is located on the western margin of the YZB (Fig. 1 B) and is composed mainly of Neoproterozoic basement and overlying Paleozoic cover. The KPL contains many Neoproterozoic igneous complexes (Plagioclase amphibolite, granulite, granite, diorite, basic rock), a small number of metamorphic volcanoes, and sedimentary rocks, ranging in age from 650 to 939 Ma, and its age peak is 825 Ma (Zhou et al., 2002 ; Geng et al., 2007 ; Lin et al., 2007 ; Lin, 2010 ; Yao et al., 2022 ). The metamorphic mixed complex in the KPL usually represents the Neoproterozoic crystalline basement observed in the southwest of the YZB (Zhou et al., 2002 ; Geng et al., 2007 ; Lin et al., 2007 ; Lin, 2010 ; Dong et al., 2011c ; Fan et al., 2015 ; Liu, 2020 ). Therefore, the U-Pb ages and Hf isotopes characteristics of the KPL zircon can represent the YZB. In addition, the ELIP, which formed between the Middle and Late Permian, has a similar location, so it may have a small amount of Middle and Late Permian age peaks when providing the provenance for the Triassic strata (Zhu et al., 2017 ; Zhang et al., 2021 ; Miao et al., 2021 ). However, the ELIP basalt provided a basic rock source and did not produce many zircons, so it is possible that zircons at approximately 260 Ma could not be detected. 2.6 Stratigraphic sequences and sedimentary characteristics The study area is located in the southwestern YZB, where Permian, Triassic, Jurassic and Cretaceous strata are widely exposed (Fig. 1 C). The strata are dominated by clastic rocks and minor carbonate rocks. The Mesozoic clastic strata are widely exposed, including the Upper Triassic Xujiahe Formation and the Jurassic Ziliujing Formation, Shaximiao Formation, Suining Formation, and Penglaizhen Formation (Fig. 2 ). The thickness of the study section is approximately 600 m, and the formation is mainly composed of fine sandstone, siltstone and mudstone. Among them, the Triassic Xujiahe Formation is mainly composed of gravel-bearing sandstone (Fig. 3 A), sandstone and coal (Fig. 3 B) from alluvial fan margin facies, which are in parallel unconformity with the Jurassic strata; the gravel-bearing sandstone of the Ziliujing Formation (Fig. 3 C) at the bottom of the Jurassic; and the purplish red and grey–green fine sandstone and mudstone that were deposited in the delta front environment in which the Ziliujing Formation to the Shaximiao Formation formed. Various sedimentary structures, including ripple bedding, parallel bedding (Fig. 3 D), wavy bedding and interference ripple marks (Fig. 3 E), have been observed in the rocks. The Suining Formation is a brick-red fine sandstone and mudstone that was deposited in a lacustrine environment, and ripple marks can be observed (Fig. 3 F). In addition, the thickness of the Xujiahe Formation decreases from the study area to the north. 3. Sampling and analytical methods The samples used in this study were taken from the Triassic Xujiahe Formation–Jurassic Suining Formation section in southwestern Sichuan, and 21 sandstone samples obtained from the Xujiahe Formation, Ziliujing Formation, Shaximiao Formation and Suining Formation were used for the whole-rock geochemical analysis. In addition, samples XJH-Z1, YTP-1-Z1, YTP-7-Z1 and YTP-27-Z1 were collected (Fig. 2), and zircon U–Pb dating and Hf isotope analysis were performed on 4 samples (Fig. 3). These zircon samples weighed at least 7 kg each and were used to select zircons. The samples were cleaned, ground to a 200 mesh powder, and analysed for major and trace elements by ZSX Primus Ⅱ XRF and Agilent 7700e ICP-MS at Wuhan SampleSolution Analytical Technology Co., Ltd., Wuhan, China, after the weathered surfaces were removed. The detrital zircons were separated, handpicked, mounted in epoxy, polished, and imaged at Langfang Yantuo Geological Service Co., Ltd., Langfang. Zircon U–Pb isotopes and cathodoluminescence (CL) images were obtained using analytical scanning electron microscope (JSM-IT100) and LA–MC–ICP–MS at the Key Laboratory for Sedimentary Basin and Oil and Gas Resources at the Chengdu Center of Geological Survey, China and Chengdu University of Technology. Data processing and Concordia diagrams were generated via the ICPMSDataCal 12.2 (Liu et al., 2008) and Isoplot 3.23 (Ludwig, 2003) software packages. In situ Hf isotope ratio analysis was conducted using a Neptune Plus LA–ICP‒MS and a GeoLas HD excimer ArF laser ablation system at Wuhan Sample Solution Analytical Technology Co., Ltd., Hubei, China. 4. Results 4.1 Petrography The samples from the Xujiahe Formation (XJH-Z1) are obviously different from those from the Jurassic (YTP-1-Z1, YTP-7-Z1 and YTP-27-Z1). Thin section analysis reveals that the sandstone samples of the Xujiahe Formation have coarse grain sizes, poor sorting, and subangular grains and are mainly composed of quartz (approximately 50%); the lithic fragments account for a high proportion (approximately 35%) of the sample; they are mainly consist of metamorphic, volcanic and sedimentary fragments, including granite, extrusive rocks, slate, phyllite, quartzite and mudstone fragments; the feldspar content is low, and it is mainly composed of K-feldspar and plagioclase (Fig. 4 A). The sandstone samples from the Ziliujing Formation (YTP-1-Z1) have fine grain sizes, poor sorting, subangular to subrounded grains, and are mainly quartz, accounting for about 75% of all the clastic grains. The rock fragments contain about 20% lithic fragments, which are mainly quartzite, shale and sedimentary rock fragments (Fig. 4 B).In addition to the clastic grains, the entire area also contains approximately 20% matrix. The sandstone samples of the Shaximiao Formation (YTP-7-Z1) have fine grain sizes; quartz contents of approximately 50%; rock fragment contents of approximately 40%; and they contain mainly quartzite, phyllite and sedimentary rock fragments (Fig. 4 C). The sandstone samples of the Suining Formation (YTP-27-Z1) have fine grain sizes, quartz contents of approximately 50%, and rock fragment contents of approximately 40%, and contain mainly extrusive rocks, phyllite and sedimentary rock fragments (Fig. 4 D). 4.2 Whole-rock elemental compositions 4.2.1 Major elements The contents of the major and trace elements are given in Supplementary Data 1. The SiO 2 contents in the Xujiahe Formation range from 70.35–93.00%, with an average of 78.10%. The TiO 2 contents range from 0.04 to 0.68%, with an average value of 0.42%; the Al 2 O 3 contents range between 2.91 and 13.92%, with an average of 9.46%; and the TFe 2 O 3 contents range between 0.53 and 4.75%, with an average of 3.17%. The SiO 2 contents of the Ziliujing Formation range from 60.92–88.30%, with an average of 70.94%. The TiO 2 contents range from 0.36 to 0.99%, with an average value of 0.75%; the Al 2 O 3 contents range between 5.67 and 21.73%, with an average of 14.47%; and the TFe 2 O 3 contents range between 2.66 and 6.67%, with an average of 4.42%. The SiO 2 contents in the Shaximiao Formation range from 50.04–89.17%, with an average of 70.64%. The TiO 2 contents range from 0.04–0.68%, with an average value of 0.42%; the Al 2 O 3 contents range from 2.93–18.37%, with an average of 10.49%; and the TFe 2 O 3 contents range from 0.45–7.52%, with an average of 3.12%. The SiO 2 contents in the Suining Group range from 59.11–85.17%, with an average of 72.14%. The TiO 2 contents range from 0.42 to 0.58%, with an average value of 0.50; the Al 2 O 3 contents range from 7.06–11.51%, with an average of 9.28%; and the TFe 2 O 3 contents range from 1.92–4.69%, with an average of 3.30%. Compared with those of the upper continental crust (UCC; Rudnick and Gao, 2003 ), the sandstone samples have higher SiO 2 contents (average of 71.05%) and lower TiO 2 contents (average of 0.58%). The Al 2 O 3 contents are low (average of 11.08%), and the TFe 2 O 3 contents are low (average of 3.39%). 4.2.2 Trace elements In the chondrite-normalized rare earth element distribution diagram (Fig. 5 A), all the samples present similar characteristics, with light rare earth element (LREE) enrichment, heavy rare earth element (HREE) flattening, and negative Eu anomalies. Only one sample (XJH-H0) presented significantly low levels of all rare earth elements. According to the UCC-normalized rare earth element distribution diagram (Fig. 5 B), the remaining samples exhibit relatively flat patterns, except that the XJH-H0 sample has significantly lower values than the UCC. 4.3 U–Pb ages of detrital zircons A total of 316 data points were detected in the 4 samples, and 309 data points had a concordance ≥ 90%. Samples with ages greater than 1000 Ma were selected for 207 Pb/ 206 Pb dating, and younger samples were selected for 206 Pb/ 238 U dating. The LA–ICP–MS zircon U–Pb data are given in Supplementary Data 2. Most grains are transparent to semitransparent. A representative zircon cathodoluminescence (CL) image is shown in Fig. 7 . The grain lengths are generally 100–200 µm, and the length-to-width ratios range from 1:1–3:1. The zircon grains are well preserved and have long to rounded shapes. Most of the zircon grains exhibit oscillatory zoning, with Th/U ratios > 0.1, indicating a magmatic origin. 4.3.1 Sample XJH-Z1 In the sample XJH-Z1, 78 of the 80 analysed zircons had ≥ 90% concordance. All the zircons range in age from 689 to 953 Ma (Fig. 7 A) and exhibit only one age peak (Fig. 8 A), with a weighted mean age of 831 ± 14 Ma; only one age is older than 900 Ma, two ages are younger than 700 Ma, and 13 ages are within 700–800 Ma. The remaining 62 ages are in the 800–900 Ma range. 4.3.2 Sample YTP-1-Z1 In the YTP-1-Z1 sample, 85 of the 86 data points have concordances ≥ 90%, showing five age groups of 198–443 Ma, 753–952 Ma, 1853–1917 Ma and 2350–2543 Ma (Fig. 7 B). The dominant peak is at 206 ± 2 Ma (n = 19), and the subordinate peak ages are 290 ± 3 Ma (n = 7), 434 ± 4 Ma (n = 8), 788 ± 7 Ma (n = 6), 1866 ± 16 Ma (n = 14), and 2531 ± 18 Ma (n = 13) (Fig. 8 B). The youngest age of the zircon grains is 198 ± 2 Ma, and the oldest is 2861 ± 13 Ma. From the single-grain zircon, the youngest zircon U‒Pb age of sample YTP-1-Z1 from the bottom of the Jurassic strata is 198.7 Ma (Supplementary Data 2), which is similar to the bottom boundary age of the Jurassic strata in the global standard stratified profile (201.3 ± 0.2 Ma; Huang, 2019 ) and the bottom boundary age of the Jurassic strata in China (199.6 Ma) (Ogg, 2019 ; Huang, 2019 ), providing stratigraphic constraints for this study. 4.3.3 Sample YTP-7-Z1 In the YTP-7-Z1 sample, 72 out of 75 data points have concordances ≥ 90%, showing five age groups of 209–482 Ma, 750–996 Ma, 1853–2095 Ma and 2379–2535 Ma (Fig. 7 C). The dominant peak is at 433 ± 5 Ma (n = 12), and the subordinate peak ages are 210 ± 3 Ma (n = 7), 309 ± 3 Ma (n = 12), 815 ± 8 Ma (n = 7), 1875 ± 25 Ma (n = 3), and 2513 ± 17 Ma (n = 4) (Fig. 8 C). From the single-grain zircon, the youngest age of the zircon grains is 209 ± 2 Ma, and the oldest is 2535 ± 15 Ma. 4.3.4 Sample YTP-27-Z1 In the YTP-27-Z1 sample, 74 out of 75 data points have concordances ≥ 90%, showing five age groups of 212–483 Ma, 735–990 Ma, 1861–2056 Ma and 2440–2598 Ma (Fig. 7 D). The dominant peak is at 243 ± 3 Ma (n = 16), and the subordinate peak ages are 359 ± 3 Ma (n = 7), 455 ± 5 Ma (n = 13), 834 ± 10 Ma (n = 7), 1863 ± 21 Ma (n = 4), and 2462 ± 19 Ma (n = 3) (Fig. 8 D). From the single-grain zircon, the youngest age of the zircon is 198 ± 2 Ma, and the oldest is 2798 ± 18 Ma. 4.4 Hf isotopes of detrital zircons Seventy-eight zircon grains were analysed via in situ zircon Hf isotope analysis (Supplementary Data 3). The 176 Hf/ 177 Hf values of the zircons range from 0.281192 to 0.282745, and the 176 Lu/ 177 Hf values range from 0.000143 to 0.003410. The ε Hf (0) values of the zircons range from − 55.9 to -1.0. The ε Hf (t) values of the zircons range from − 17.0 to 13.6. Their T DM1 ages range from 717 to 2846 Ma, and their T DM2 ages range from 823 to 3046 Ma. 4.4.1 Sample XJH-Z1 In sample XJH-Z1, for the 689 to 953 Ma group, the ε Hf (t) values of the zircons range from − 3.2 to 9.8. Their T DM1 ages range from 987 to 1419 Ma, and their T DM2 ages range from 1044 to 1672 Ma. 4.4.2 Sample YTP-1-Z1 In sample YTP-1-Z1, for the 198–443 Ma group, the ε Hf (t) values of their zircons range from − 7.9 to 7.3, their T DM1 ages range from 738 to 1153 Ma, and the T DM2 ages range from 871 to 1553 Ma. For the 753–952 Ma group, the ε Hf (t) values of the zircons range from − 13.8 to 9.8, their T DM1 ages range from 992 to 1893 Ma, and their T DM2 ages range from 1061 to 2327 Ma. For the 1853–1917 Ma group, the ε Hf (t) values of the zircons range from − 4.7 to 13.6, their T DM1 ages range from 1722 to 2476 Ma, and their T DM2 ages range from 1675 to 2712 Ma. For the 2350–2543 Ma group, the ε Hf (t) values of the zircons range from 0.91 to 12.9, their T DM1 ages range from 2344 to 2812 Ma, and their T DM2 ages range from 2268 to 2922 Ma. 4.4.3 Sample YTP-7-Z1 In sample YTP-7-Z1, for the 209–482 Ma group, the ε Hf (t) values of the zircons range from − 8.6 to 0.7, their T DM1 ages range from 861 to 1368 Ma, and their T DM2 ages range from 1097 to 1715 Ma. For the 750–996 Ma group, the ε Hf (t) values of the zircons range from − 13.8 to 7.5, their T DM1 ages range from 1074 to 1919 Ma, and their T DM2 ages range from 2349 to 2349 Ma. For the 2379–2535 Ma group, the ε Hf (t) values of the zircons range from − 4.2 to 2.8, their T DM1 ages range from 2676 to 2846 Ma, and their T DM2 ages range from 2758 to 3046 Ma. 4.4.4 Sample YTP-27-Z1 In sample YTP-27-Z1, for the 212–483 Ma group, the ε Hf (t) values of the zircons range from − 14.3 to 8.7, their T DM1 ages range from 717 to 1572 Ma, and their T DM2 ages range from 823 to 2002 Ma. For the 735–990 Ma group, the ε Hf (t) values of the zircons range from − 17.0 to 2.9, their T DM1 ages range from 1281 to 2043 Ma, and their T DM2 ages range from 1452 to 2543 Ma. For the 1861–2056 Ma group, the ε Hf (t) values of the zircons range from − 5.8 to 1.7, their T DM1 ages range from 2237 to 2532 Ma, and their T DM2 ages range from 2373 to 2786 Ma. 5. Discussion 5.1 Sedimentary sorting The major, trace and rare earth element data can reflect the nature of terrigenous clastic rocks and tectonic settings and include SiO 2 , Al 2 O 3 , TiO 2 , K 2 O, Fe 2 O 3 , MgO, La, Th, Co, Zr, Sc, Hf, and REEs (Bhatia and Crook, 1986 ; Floyd and Leveridge, 1987 ; Girty, 1996; Hayashi et al., 1997 ; Fralick and Kronberg, 1997 ; Paikaray et al., 2008 ; Ma et al., 2019 ; Xia et al., 2021 ). However, before analysing the properties of terrigenous clastic rocks and the tectonic setting, it is necessary to determine whether the fractionation of elements in sediments is affected by the sorting of sedimentary processes (Zhang, 2004 ; Singh, 2009 ; Hou et al., 2016 ; Wang et al., 2018 ; Ren et al., 2023 ). The diagrams of TFe 2 O 3 versus TiO 2 , TFe 2 O 3 and TiO 2 versus Al 2 O 3 reveal that TFe 2 O 3 versus TiO 2 , TFe 2 O 3 and TiO 2 versus Al 2 O 3 are strongly correlated (Fig. 9 A, B, C), whereas Cr/Th, Th/Sc versus Al 2 O 3 , TiO 2 and Zr have almost no correlation (Fig. 9 D, E, F, G, H, and I). These data indicate that the stable elements were not significantly affected by sedimentary sorting during deposition and can be used as effective indicators of the characteristics of the provenance region characteristics. 5.2 Nature of source rocks The TFe 2 O 3 /Al 2 O 3 versus TiO 2 /Al 2 O 3 binary curve shows that all the samples plot far from basalt; many samples plot near the Post-Archean Australian Shale (PAAS), UCC and andesite; a small number of samples plot near granites; and only one sample from the Xujiahe Formation plots near felsic volcanic rocks (Fig. 10 A), which indicates that it may be derived mainly from intermediate–felsic igneous rocks. The Zr/Sc and Th/Sc values can reflect changes in the sediment composition and degree of sorting. The Th/Sc values of sedimentary rocks reflect the average values in the provenance region, and the Zr/Sc ratios gradually increase as the sediments undergo diagenesis and as zircons are enriched (McLennan et al., 1993 ). On the Th/Sc versus Zr/Sc diagram (Fig. 10 B), except for one sample from the Xujiahe Formation, all the other samples range from andesite to felsic volcanic rocks and plot closer to the region of felsic volcanic rocks. Some of the samples exhibit characteristics of sediment recycling, indicating that the source rock may have been felsic volcanic rock and that the rock underwent recycling. According to the diagram of the La/Th ratio to Hf (Floyd and Leveridge, 1987 ), most of the studied samples plot in the source area of felsic rocks, whereas a small number of samples (mainly those from the Ziliujing Formation) plot in the area that has an increasing trend of old sedimentary components. These results indicate that there may be recycled old sediments in addition to intermediate–acidic igneous rocks (Fig. 10 C). The many sedimentary lithic fragments that are associated with the petrological characteristics also provide support (Fig. 4 ). 5.3 Provenance analysis Sample XJH-Z1 from the Xujiahe Formation is significantly different from samples YTP-1-Z1, YTP-7-Z1, and YTP-27-Z1 from the Jurassic strata, with a single peak age of 689–953 Ma (Fig. 11 A). In contrast, the detrital zircon ages of the three Jurassic samples show four similar dominant age groups. Among them, the dominant age peak of sample YTP-1-Z1 was 206 Ma, that of sample YTP-7-Z1 was 433 Ma, and that of sample YTP-27-Z1 was 243 Ma; the subordinate age peaks are 788–834 Ma, 1863–1875 Ma, and 2462–2531 Ma (Fig. 11 B, C, and D). 5.3.1 U–Pb ages and Hf values of detrital zircons (1) 2462–2531 Ma The oldest age group of 2462–2531 Ma corresponds to the Neoarchean to Paleoproterozoic basement in the YZB, such as the Kongling complex (Gao et al., 1999 ; 2011 ) and Huangtian basic rock mass (Fig. 11 H) (Liu et al., 2020 ). However, the sedimentary strata of the N-CB have obvious peak ages from the Neoarchean to the Paleoproterozoic (Li et al., 1993 ; Darby and Gehrels, 2006 ; Jian et al., 2019 ) (Fig. 11 F, G). Moreover, the 2462–2531 Ma zircons are mostly well rounded, indicating a large transport distance. In addition, the ε Hf (t) values of this age group all plot near the QOB and YZB (Fig. 12 ). Therefore, zircons from the N-CB cannot be ruled out. (2) 1863–1875 Ma The 1863–1875 Ma age group corresponds to the convergence and fragmentation of the Columbia supercontinent (Zhao et al., 2002 ; Yin et al., 2013 ; Chen et al., 2016b; Lu et al., 2020 ), and the fragmentation of the supercontinent has been recorded in many old cratons worldwide (Zhao et al., 2002 ; Cawood et al., 2018 ), including the Dongling complex (Chen and Xing, 2016) and the Kongling complex (Yin et al., 2013 ; Guo et al., 2015 ) in the YZB and southern N-CB. Owing to the existence of magmatic records in both the YZB and the N-CB (Fig. 11 I), it is impossible to determine whether the zircons originated from the YZB or N-CB. In terms of the ε Hf (t) values, the detrital zircons from the N-CB and those deposited in the QOB have negative values, whereas the ε Hf (t) values in the YZB have a wide range, and the data points plot near the YZB area (Fig. 12 ); therefore, the zircons in this age group are more likely to come from the YZB. (3) 788–834 Ma and 689–953 Ma The age groups of 788–834 Ma and 689–953 Ma correspond to the fragmentation of the Rodinia supercontinent (Li et al., 1999 ; Zhou et al., 2002 ; Wang et al., 2013b ; Zhou et al., 2014 ; Yang et al., 2017 ). This age group is found in many magmatic rocks that are located on the southwestern margins of the YZB and QOB, including the Baoxing complex (Zhao et al., 2008 a; Meng et al., 2015 ), Kangding complex (Zhou et al., 2002 ), Pengguan complex (Ma et al., 1996 ), Gongcai complex (Roger and Calassou, 1997) and Bikou Terrane (Wang et al., 2012 ). These age groups are similar in age (Fig. 11 ) but have different ε Hf (t) values. The ε Hf(t) values of the Bikou Terrane in the QOB are usually negative (Wang et al., 2012 ; Mu, 2020 ; Qin et al., 2021 ); zircon samples from other areas of the QOB also exhibit similar characteristics (Zhu et al., 2009 ), but some of them exhibit small positive values, whereas those from the YZB complex rocks usually exhibit positive values (Zhao et al., 2008b ; Meng et al., 2015 ; Kang et al., 2017 ). The KPL on the southwestern edge of the YZB contains many Neoproterozoic igneous complexes, a small number of metamorphic volcanoes, and sedimentary rocks, ranging in age from 650 to 939 Ma, and its age peak is 825 Ma (Fig. 11 L) (Zhou et al., 2002 ; Geng et al., 2007 ; Lin et al., 2007 ; Lin et al., 2010). In this age group, the zircon ε Hf (t) values of sample XJH-Z1 are positive, except for one data point with a small negative value, and all the data plot in the YZB (Fig. 12 ). In contrast, most of the three groups of Jurassic samples are negative, and only seven zircon grains have positive values, which is more consistent with the QOB. Therefore, the provenance of sample XJH-Z1 can be considered magmatic rocks related to the cracking of the Rodinia supercontinent in the YZB, whereas the Jurassic samples originated from the QOB. In addition, the zircon grains of sample XJH-Z1 are intact and angular (Fig. 6 A) and can also be judged to be from a relatively proximal source. (4) 200–500 Ma In the range of 200–500 Ma, the zircon U‒Pb ages have multiple age peaks (~ 440 Ma, ~ 310 Ma, and ~ 210 Ma) (Fig. 11 B, C, D). Among them, the ~ 440 Ma peak is found in many magmatic rocks in the NQB, which is related to the closure of the Shangdan Ocean caused by the collision between the SQB and the NQB (Lu et al., 2003 ; Zhang et al., 2006b ; Dong et al., 2011a ; Wang et al., 2013c ; 2015 ; Li, 2020 ); however, this age has rarely been reported in the YZB. The ε Hf (t) values for ~ 440 Ma plot entirely within the region of the QOB (Fig. 12 ); therefore, zircons of this age can come from the QOB. Moreover, ~ 310 Ma ages are rarely recorded in the QOB and YZB and are recorded only in the Paleo-Mianlue Ocean between the SOB and NQB, which also corresponds to the expansion of the Paleo-Mianlue Ocean (Dong et al., 1999 ; Li et al., 2004 ; Dong et al., 2011a ; Zhang et al., 2019 ; Li, 2020 ). The ~ 210 Ma peak is found in many rocks in the SQB, YZB, SGT and YDT, corresponding to the closure of the Paleo‒Tethys Ocean (Zhang et al., 2006b ; Jian et al., 2009 ; Zi et al., 2012 ; He et al., 2013 ; Peng et al., 2014 ; Wang et al., 2017 ; Xu et al., 2019 ). The Paleo-Mianlue Ocean was also closed at this time as part of the Paleo-Tethys Ocean (Dong and Santosh, 2016 ; Dong et al., 2021 ; Zhang et al., 2022b ; Huang et al., 2024 ; Chuan et al., 2024 ), so the zircon U‒Pb ages from the two provenances were not very different. However, the ε Hf (t) values in the QOB on the north side of the YZB are usually positive, whereas the ε Hf (t) values of the Paleo-Tethys volcanic rocks in the southern YZB are negative (Fig. 12 ); most ε Hf (t) values plot in the negative region, and a small number of ε Hf (t) values plot in the positive region. In addition, the zircon grains of this age group also have two characteristics: most are long, and a few are well rounded. In summary, most zircons of this age group originated from the YDT related to the Paleo-Tethys Ocean, and a small number came from the QOB. In addition, the ELIP rock province provided ~ 260 Ma zircon grains (Shellnutt et al., 2012 ; Huang et al., 2022 ), but the samples do not exhibit a peak value at 260 Ma; therefore, this area is not discussed. 5.3.2 Upper Triassic Xujiahe Formation There are many Precambrian and Paleozoic sandstone deposits in the LTB, whose zircon age peaks are ~ 500 Ma, ~ 743 Ma, ~ 849 Ma, ~ 950 Ma, and ~ 2500 Ma (Fig. 11 J) (Duan et al., 2011 ; Chen et al., 2016c ; Mao et al., 2021 ). If the provenance area of the Xujiahe Formation is the LTB, there is a lack of zircon age data for the sedimentary cover. Therefore, the single-age peak sandstone of the Xujiahe Formation obtained in this study indicates that the southern section of the LTB did not uplift in the Late Triassic and was not the provenance of the nearby southwestern YZB. The depositional time of the Xujiahe Formation is generally considered the Norian–Rhaetian stage in the YZB (Lu et al., 2013 ; Li et al., 2017 ; Tong et al., 2019 ; Jiang et al., 2023 ). The global sea level change was less than 26 m during the Norian‒Rhaetian stage (Huang et al., 2006 ; Xu et al., 2012 ; Kelley et al., 2014 ; Ruban et al., 2015; Ogg, 2019 ). It has also been suggested that the subsidence of the KPL may have been caused by the eastwards shortening and loading of the western YZB, due to the collision of the YZB and SGT (Yan et al., 2019 ). On the basis of our data, we propose that the KPL may have continued to provide terrigenous detritus during the Late Triassic, although some scholars consider the KPL to have been a settling region during the Late Triassic and Jurassic (He et al., 2003 ; Chen et al., 2011 ; Zhu et al., 2017 ; Yan et al., 2019 ). The KPL contains Neoproterozoic igneous complexes, a small number of metamorphic volcanoes and sedimentary rock, with an age peak of ~ 825 Ma (~ 650–~939 Ma) (Zhou et al., 2002 ; Geng et al., 2007 ; Lin et al., 2007 ; Lin et al., 2010). The zircon age distribution patterns of the XJH-Z1 samples are highly similar to those of the KPL samples. Moreover, XJH-Z1 rocks are characterized by coarse grain sizes, poor sorting, subangular particles, and intact and angular zircon particles, which support the view that the source of the Xujiahe Formation was near-source KPL rather than southern LTB (Ma et al., 2009 ; Deng et al., 2012 ; Mei, 2014 ; Luo et al., 2014 ; Yu, 2016 ; Zhu et al., 2017 ; Yu and Liang, 2017 ; Mu et al., 2019 ; Mu, 2020 ). Since the northern section of the LTB was the first to respond to the closing of Songpan-Ganzi Ocean and the collision between the YZB and the N-CB, the uplift of the LTB was not a short process, but a gradual process from the north to the south ((Liu et al., 2009 ; Li et al., 2010c ; Yan et al., 2013 ; Zhu et al., 2017 ; Huang et al., 2020b ; Lu et al., 2023 ; Gou et al., 2024 ), and the southern section of the LTB was the last uplift area. The detrital zircon distribution patterns of the Xujiahe Formation in other areas of SCB are different from those in the study area. The distribution patterns of zircon age with single peak value are relatively rare, but not without records (Yan et al., 2019 ; Lu et al., 2023 ). After considering factors such as paleocurrents directions, we think that the paleocurrent system may have mixed the detritic zircon records of the uplifted north and middle LTB, the north SGT, and the QOB in other areas. In the study area, only detritic zircon from the KPL were recorded. 5.3.3 Jurassic Zircons of the same age (~ 850 Ma) in the Jurassic samples have ε Hf(t) values significantly different from those of sample XJH-Z1 (Fig. 11 ). The zircon age distribution patterns of samples YTP-1-Z1, YTP-7-Z1 and YTP-27-Z1 are highly similar to those of the SGT and YTD (Fig. 11 E, K), and they are different from those of the LTB Precambrian‒Palaeozoic sedimentary cover. Therefore, it can be inferred that the provenance shifted and that the KPL provided little provenance in the Early Jurassic. The terrigenous detritus from the SGT and YDT areas could not be completely blocked by the LTB. The LTB had not yet reached its current scale, and the uplift scale of the southern LTB was even smaller than those of the northern and middle sections (Liu et al., 2009 ; Li et al., 2010c ; Yan et al., 2013 ; Huang et al., 2020b ). In the Late Triassic, the SGT was still a sedimentary area that was sourced mainly from the QOB (Bruguier et al., 1997 ; Weislogel et al., 2006 , 2010 ; Luo et al., 2014 ; Mu et al., 2019 ), and the SGT and QOB had similar zircon age distribution pattern characteristics (Wang et al., 2013a ; Wu et al., 2016 ; Liu et al., 2021b ). In the Early Jurassic, it was uplifted and provided detrital material for the southwestern YZB. In other words, the zircon U‒Pb ages of the Jurassic sandstone samples in the study area are similar to those of the SGT and QOB samples. According to the SE paleocurrents characteristics, the sample petromineral and geochemical characteristics of the Jurassic have the characteristics of recycled sediments. The differences in the petrological characteristics between the Xujiahe Formation samples and the Jurassic samples are significant (Fig. 4 A), which may represent changes in the provenance area. The Jurassic samples are characterized by low feldspar contents and rich sedimentary lithic fragments, which represent recycled sediments, and the contents of single-crystal quartz, sedimentary lithic fragments and clay minerals in the Ziliujing Formation (YTP-1-Z1) are significantly greater than those in the Shaximiao Formation (YTP-7-Z1) and Suining Formation (YTP-27-Z1) (Fig. 4 B, C, D). The textural maturity of the Ziliujing Formation is lower, indicating that the sediments within the Ziliujing Formation were probably sourced from proximal source(s). The sediments within the Shaximiao and Suining Formations experienced long-distance transport. The Middle and Late Jurassic samples show that the number of young zircons did not increase with gradual changes in strata, indicating that the SGT and YDT were in a relatively stable tectonic settings and lacked volcanic activity, at least from the Middle Jurassic to the Late Jurassic. The lack of volcanic rocks in the Middle‒Late Jurassic that are reported for the SGT and YDT also suggests that the tectonic setting is relatively stable (Yuan et al., 2010 ; Peng et al., 2014 ; Sigoyer et al., 2014 ; Li and Liu, 2015 ; Li et al., 2018 ; Zhao et al., 2020 ). The change in petrological characteristics may be due to the weathering and erosion of the southern LTB, which weakened the blocking effect of the LTB on the SGT and YDT, and more distant sources were transported to the study area. 5.4 Tectonic settings In addition, the whole-rock geochemical characteristics, such as the La, Th, Zr, Co, and Sc contents, of sedimentary rocks can be used to analyse the tectonic settings of the source area (Bhatia and Crook, 1986 ; Wei et al., 2009 ; Zheng et al., 2019 ). On the La‒Th‒Sc triangular diagram (Fig. 13 A), all the samples plot near the continental margin and continental island arc region, and no samples plot in the oceanic island arc region. On the Th‒Co‒Zr/10 triangular diagram (Fig. 13 B), most of the samples plot within and around the continental island arc, no samples plot in the oceanic island arc region, and only five samples plot in the continental margin region. According to the Th‒Sc‒Zr/10 triangular diagram (Fig. 13 C), most of the samples plot near the continental island arc and the passive continental margin regions, no samples are located in the oceanic island arc region, and only one sample is located in the passive continental margin region. The La‒Th‒Sc, Th‒Co‒Zr/10 and Th‒Sc‒Zr/10 triangular diagrams suggest that the main provenance area was a continental island arc tectonic setting and that a small amount of material was derived from the continental margin. The detrital zircon age can also reflect the tectonic setting of sedimentary basins and can be divided into three main types: convergent basins, collisional basins and extensional basins (Cawood et al., 2012 ). In the CDP diagram, all four samples plot within region B, so this region can be considered a collisional setting (Fig. 14 ). In the context of an arc–continent or continent–continent collision, the sample plots in region B lie in a collisional tectonic setting (Cawood et al., 2012 ). However, the youngest zircon age in sample XJH-Z1 is 689 Ma, which cannot represent the stratigraphic depositional age. Therefore, in the Late Triassic, 215 Ma was selected as the stratigraphic depositional age (the Late Triassic depositional age was ~ 237 to ~ 201 Ma (Ogg, 2019 ; Tong et al., 2019 ), regardless of which value was selected as the depositional age, it had no effect on the results). Sample XJH-Z1 plots in region C (dashed line) (Fig. 14 ), representing an extensional setting. Therefore, the Xujiahe Formation samples represent an extensional setting, whereas the Jurassic samples represent a collisional setting. 5.5 Implications Many sedimentary rocks in the tectonic setting of the passive continental margin were deposited on the western margin of the YZB during the Paleozoic (Zhou et al., 2016 b; Pan et al., 2021 ). During the Middle Triassic to Late Triassic, owing to the westwards subduction of the SGT, the YDT developed basalt, andesite, dacite, rhyolite and intermediate-acid magmatic intrusive rocks in the island arc setting (Li and Liu et al., 2015 ; Wang et al., 2017 ). Combined with the NE paleocurrents directions of the Xujiahe Formation and the SE paleocurrents directions of the Jurassic (Fig. 2 ), as well as the large amounts of volcanic debris and sedimentary debris, it can be inferred that the main provenances of the Jurassic strata are the sedimentary rocks deposited early at the western margin of the SGT and YDT, and the island arc volcanic rocks from the YDT. Owing to the inclusion of many magmatic rocks from the YDT continental island arc, the La-Th-Sc, Th-Co-Zr/10 and Th-Sc-Zr/10 triangular maps (Fig. 11 ) are characterized by passive continental margins and island arcs. There is a lack of Mesozoic zircons in the Xujiahe Formation; in contrast, many Mesozoic zircons were found in the Jurassic, which means that the study area was still a passive continental margin in the Late Triassic, and it was not until the Jurassic that the island arc area in the YDT began to provide terrigenous detritus. In other words, in the Early Jurassic, the southwestern YZB experienced an evolutionary stage from a passive continental margin to a foreland basin rather than in the Late Triassic (Zhou et al., 2016 b; Liu et al., 2017 ; Pan et al., 2021 ). The CDP diagram has similar characteristics (Fig. 14 ). In general, this study indicates that the main provenance of the southwestern YZB was the KPL in the Late Triassic. Since the Ganzi–Litang Ocean on the southern side of SGT had not yet closed, the material of the YDT island arc could not have been transported to southwestern YZB. In the Early Jurassic, the SGT and YDT were transformed into provenance areas, and the LTB rose, but these changes were not sufficient to block the provenance input from the SGT and YDT (Fig. 15 ). In the Middle Jurassic, the LTB shrank due to weathering and erosion, and the SGT and YDT continued to enter the southwestern YZB as source areas. In this study, the closure time of the eastern branch of the Paleo-Tethys Ocean (Ganzi–Litang Ocean) was no later than the early Early Jurassic. 6. Conclusions (1) Detrital zircons from the Xujiahe Formation samples originated from Neoproterozoic igneous complexes, a small number of metamorphic volcanoes, and sedimentary rocks on the KPL, whereas the detrital zircons from the Jurassic samples originated from Late Triassic detrital rocks deposited in the SGT and YDT after sedimentary recycling. (2) Triassic detrital rocks were deposited on a passive continental margin, Jurassic clastic rocks were deposited in a continental island arc setting, and the source materials were medium–acid igneous rocks and recycled sedimentary rocks. (3) In the Early Jurassic, the LTB uplifted and provided source material for the southwestern YZB. The uplift time of the southern LTB can be confined to the Early Jurassic. (4) In the Early Jurassic, there may have been a brief tectonic setting change from the passive continental margin to the foreland basin. Declarations Acknowledgements We are grateful to the China Geological Survey for its financial support. I am grateful to Dr. Xiuping Wang, Dr. Yu Xia. and M.D. Weiwei Chen for their supports in the petrographic section. Constructive suggestions from three anonymous reviewers are acknowledged with thanks. Funding This study was supported by National Natural Science Foundation of China [grant number 92055314], National Natural Science Foundation of China [grant number U2344209], and China Geological Survey [number: DD20242564]. Competing Interests The authors declare no conflicts of interest. Availability of data and materials The data that support the findings of this study are available from the first author upon reasonable request. References Bhatia, M.R., Crook, A.W., 1986. 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Also discoverable on Platform About Our Team In Review Editorial Policies Advisory Board Help Center Resources Author Services Accessibility API Access RSS feed Manage Cookie Preferences © Research Square 2026 | ISSN 2693-5015 (online) Privacy Policy Terms of Service Do Not Sell My Personal Information {"props":{"pageProps":{"initialData":{"identity":"rs-5860486","acceptedTermsAndConditions":true,"allowDirectSubmit":false,"archivedVersions":[],"articleType":"Article","associatedPublications":[],"authors":[{"id":446814311,"identity":"e0deab59-01ef-4664-9a99-d4ef8a686d5d","order_by":0,"name":"Shengyang Yao","email":"data:image/png;base64,iVBORw0KGgoAAAANSUhEUgAAAZAAAAAyAQMAAABI0h/eAAAABlBMVEX///8AAABVwtN+AAAACXBIWXMAAA7EAAAOxAGVKw4bAAAA00lEQVRIiWNgGAWjYNACAxs5fvbGxgcfiNdSkGYs2XO42XAG8Vo+HE7cMCO9TZqDKCfdyDH+zGMA1CL5sEGagcFOTreBgBbJnjNm0jwG6cbbpRMbjAsYko3NDhDQws/eY8bMY2Atu3N2YkPyDIYDidsIaWFj5gE5jJlxw82DDYd5iNECtMUA6DBnxQ03GBubidIi2XOsTHKOASiQE5sZZxgQ4ReDG8mbP7z5A4rK489/fKiwkyOohYGBw4CJB2ECQeUgwP6A8QdRCkfBKBgFo2DEAgCdMkNVlVn/wQAAAABJRU5ErkJggg==","orcid":"","institution":"Chengdu University of Technology","correspondingAuthor":true,"prefix":"","firstName":"Shengyang","middleName":"","lastName":"Yao","suffix":""},{"id":446814312,"identity":"f60fa9be-b19e-4e01-be4f-989b93a9b433","order_by":1,"name":"Qiyu Wang","email":"","orcid":"","institution":"Chengdu University of Technology","correspondingAuthor":false,"prefix":"","firstName":"Qiyu","middleName":"","lastName":"Wang","suffix":""},{"id":446814313,"identity":"582a8613-d166-423a-9767-c13d86daa5ad","order_by":2,"name":"Chuanlong Mou","email":"","orcid":"","institution":"Chengdu University of Technology","correspondingAuthor":false,"prefix":"","firstName":"Chuanlong","middleName":"","lastName":"Mou","suffix":""},{"id":446814314,"identity":"32b92603-ddf2-4ce9-999e-f976ab046689","order_by":3,"name":"Peng Ren","email":"","orcid":"","institution":"China Geological Survey (Geoscience Innovation Center of Southwest China)","correspondingAuthor":false,"prefix":"","firstName":"Peng","middleName":"","lastName":"Ren","suffix":""},{"id":446814315,"identity":"0424039d-682b-421e-9b99-470e6dac48e9","order_by":4,"name":"Bowen Zan","email":"","orcid":"","institution":"China Geological Survey (Geoscience Innovation Center of Southwest China)","correspondingAuthor":false,"prefix":"","firstName":"Bowen","middleName":"","lastName":"Zan","suffix":""},{"id":446814316,"identity":"d348106d-969e-4bd8-86ab-037343b415d2","order_by":5,"name":"Shangke Xie","email":"","orcid":"","institution":"China Geological Survey (Geoscience Innovation Center of Southwest China)","correspondingAuthor":false,"prefix":"","firstName":"Shangke","middleName":"","lastName":"Xie","suffix":""},{"id":446814317,"identity":"a36b472c-7879-46a7-98aa-22f83e0bc38e","order_by":6,"name":"Jiale Liu","email":"","orcid":"","institution":"Shandong University of Science and Technology","correspondingAuthor":false,"prefix":"","firstName":"Jiale","middleName":"","lastName":"Liu","suffix":""},{"id":446814318,"identity":"d910f66b-af83-4fee-9054-2c86971aedae","order_by":7,"name":"Xiao Liu","email":"","orcid":"","institution":"Shandong University of Science and Technology","correspondingAuthor":false,"prefix":"","firstName":"Xiao","middleName":"","lastName":"Liu","suffix":""}],"badges":[],"createdAt":"2025-01-19 16:23:12","currentVersionCode":1,"declarations":"","doi":"10.21203/rs.3.rs-5860486/v1","doiUrl":"https://doi.org/10.21203/rs.3.rs-5860486/v1","draftVersion":[],"editorialEvents":[{"content":"https://doi.org/10.1038/s41598-025-05155-1","type":"published","date":"2025-07-02T15:58:12+00:00"}],"editorialNote":"","failedWorkflow":false,"files":[{"id":81316150,"identity":"cd4d86f1-aa22-46ed-ba60-9a0a2b911351","added_by":"auto","created_at":"2025-04-24 16:16:50","extension":"png","order_by":1,"title":"Figure 1","display":"","copyAsset":false,"role":"figure","size":4992900,"visible":true,"origin":"","legend":"\u003cp\u003e(A)\u003cstrong\u003e \u003c/strong\u003eThe Diagram of tectonic zones, China (modified after Gs(2023) 2764, Zhao et al., 2001; Liang and Jones, 2021); (B) Geological map of the western Yangtze and igneous rocks in surrounding areas (Ma, 2002; Zhou et al., 2002; Li et al., 2018; Wang et al., 2018; Zheng et al., 2021); (C) Geological map of the southwestern Sichuan Basin (modified after Ma, 2002)\u003c/p\u003e","description":"","filename":"1.png","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/c0a74fd3b14d62a8cff44ff2.png"},{"id":81313621,"identity":"3b1cdd9a-2867-4427-938c-aa420b62ec85","added_by":"auto","created_at":"2025-04-24 15:52:54","extension":"png","order_by":2,"title":"Figure 2","display":"","copyAsset":false,"role":"figure","size":2190578,"visible":true,"origin":"","legend":"\u003cp\u003eStratigraphic columns of the Xujiahe Formation to the Suining Formation and the sampling site of the detrital zircon samples\u003c/p\u003e","description":"","filename":"2.png","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/0125b46d62946929524e41b8.png"},{"id":81314786,"identity":"e3f461e1-cb1e-4561-99bf-8c4b256c5869","added_by":"auto","created_at":"2025-04-24 16:00:50","extension":"png","order_by":3,"title":"Figure 3","display":"","copyAsset":false,"role":"figure","size":16417416,"visible":true,"origin":"","legend":"\u003cp\u003eTypical sedimentary features of the Xujiahe Formation to the Suining Formation\u003c/p\u003e\n\u003cp\u003e(A) Pebbly sandstone in the Xujiahe Formation; (B) sandstone and coal in the Xujiahe Formation; (C) bottom gravel-bearing sandstone in the Ziliujing Formation; (D) parallel bedding in the Shaximiao Formation sandstone; (E) interference ripple marks in the Shaximiao Formation; (F) ripple marks in the Suining Formation\u003c/p\u003e","description":"","filename":"3.png","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/6196dd6fb73b2cd1c987696c.png"},{"id":81313133,"identity":"7acf153d-9db1-4a15-a64c-7905247e0ddf","added_by":"auto","created_at":"2025-04-24 15:44:54","extension":"png","order_by":4,"title":"Figure 4","display":"","copyAsset":false,"role":"figure","size":23669937,"visible":true,"origin":"","legend":"\u003cp\u003ePhotomicrographs of representative samples under cross-polarized light. (A) XJH-Z1; (B) YTP-1-Z1; (C) YTP-7-Z1; (D) YTP-27-Z1\u003c/p\u003e\n\u003cp\u003eQm = Monocrystalline Quartz; Qp = Polycrystalline Quartz; K = K-feldspar; Pl = Plagioclase; Le = Extrusive lithic fragment; Lg = Granite lithic fragmen; Ch = Chert; Ls = Sedimentary lithic fragment; Lq = Quartzite lithic fragment; Lm = Metamorphic lithic rock\u003c/p\u003e","description":"","filename":"4.png","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/18724f8f21921ae1f21e39de.png"},{"id":81314795,"identity":"9a05aa7e-94c2-4690-8df3-3b4c93dd1807","added_by":"auto","created_at":"2025-04-24 16:00:51","extension":"png","order_by":5,"title":"Figure 5","display":"","copyAsset":false,"role":"figure","size":23669937,"visible":true,"origin":"","legend":"\u003cp\u003e(A) Chondrite-normalized REE pattern diagram; (B) UCC-normalized REE pattern diagram\u003c/p\u003e\n\u003cp\u003eThe chondrite values used for normalization are from Sun and McDonough (1989), and the UCC values used for normalization are from Rudnick and Gao (2003).\u003c/p\u003e","description":"","filename":"5.png","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/4f26de97860eaf8d1e8edb30.png"},{"id":81315802,"identity":"86e240fb-e9d2-49ce-a1d3-f90494b2a16a","added_by":"auto","created_at":"2025-04-24 16:08:50","extension":"png","order_by":6,"title":"Figure 6","display":"","copyAsset":false,"role":"figure","size":5869170,"visible":true,"origin":"","legend":"\u003cp\u003eCathodo-luminescence (CL) images of representative analysed zircons. The numbers in red color refer to the zircon \u003csup\u003e207\u003c/sup\u003ePb/\u003csup\u003e206\u003c/sup\u003ePb or \u003csup\u003e206\u003c/sup\u003ePb/\u003csup\u003e238\u003c/sup\u003eU ages, and \u003csub\u003eεHf\u003c/sub\u003e(t) values are indicated in yellow color.\u003c/p\u003e","description":"","filename":"6.png","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/e256a0a3fca734b22ee959b6.png"},{"id":81315801,"identity":"15099315-9f7b-4242-b640-b6eb81377660","added_by":"auto","created_at":"2025-04-24 16:08:50","extension":"png","order_by":7,"title":"Figure 7","display":"","copyAsset":false,"role":"figure","size":1657276,"visible":true,"origin":"","legend":"\u003cp\u003eConcordia diagrams of detrital zircons from theXJH-Z1, YTP-1-Z1, YTP-7-Z1, and YTP-27-Z1\u003c/p\u003e","description":"","filename":"7.png","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/dedf8603166e7235ecc16c1d.png"},{"id":81313586,"identity":"c9e8207c-c7a2-48e4-a41b-9cc55a5e78b4","added_by":"auto","created_at":"2025-04-24 15:52:50","extension":"png","order_by":8,"title":"Figure 8","display":"","copyAsset":false,"role":"figure","size":1950946,"visible":true,"origin":"","legend":"\u003cp\u003eRelative probability density diagram of the four studied samples (≥ 90% concordance)\u003c/p\u003e","description":"","filename":"8.png","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/4eb6923c4be1e793e38ae6fc.png"},{"id":81316151,"identity":"d4ec6100-94c6-43b6-90f3-d2042ba71de5","added_by":"auto","created_at":"2025-04-24 16:16:50","extension":"png","order_by":9,"title":"Figure 9","display":"","copyAsset":false,"role":"figure","size":1494390,"visible":true,"origin":"","legend":"\u003cp\u003eWhole-rock geochemical diagram of sandstones. TFe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e is positively correlated with TiO\u003csub\u003e2\u003c/sub\u003e, and TFe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e and TiO\u003csub\u003e2\u003c/sub\u003e are positively correlated with Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e. Cr/Th and Th/Sc are not obviously correlated with Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e, TiO\u003csub\u003e2\u003c/sub\u003e or Zr.\u003c/p\u003e","description":"","filename":"9.png","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/22e82433135042f3b52834f9.png"},{"id":81313068,"identity":"3c590b84-8b60-4823-b21c-c2c544da3a0e","added_by":"auto","created_at":"2025-04-24 15:44:50","extension":"png","order_by":10,"title":"Figure 10","display":"","copyAsset":false,"role":"figure","size":889374,"visible":true,"origin":"","legend":"\u003cp\u003eDiscriminant diagrams of the source rocks in the samples in this study. (A) TFe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e/Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e versus TiO\u003csub\u003e2\u003c/sub\u003e/Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e (modified after Wang et al., 2018); (B) Zr/Sc versus Th/Sc (modified after McLennan et al., 1993); (C) La/Th versus Hf (modified after Floyd and Leveridge, 1987).\u003c/p\u003e","description":"","filename":"10.png","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/d7c18463cd016efe62228981.png"},{"id":81313593,"identity":"60fc3fbb-2421-45f1-b7fe-8230bee88a91","added_by":"auto","created_at":"2025-04-24 15:52:50","extension":"png","order_by":11,"title":"Figure 11","display":"","copyAsset":false,"role":"figure","size":3461075,"visible":true,"origin":"","legend":"\u003cp\u003eDiagram comparing the age distribution. (A) The Xujiahe Formation (XJH-Z1, this study); (B) the Ziliujing Formation (YTP-1-Z1, this study); (C) the Shaximiao Formation (YTP-7-Z1, this study); (D) the Suining Formation (YTP-27-Z1, this study); (E) the Songpan–Ganzi Terrane (SGT) (Chen et al., 2009); (F) the South Qinling Orogenic Belt (SQB) (Li et al., 2018 and references therein); (G) the North Qinling Orogenic Belt (NQB) (Li et al., 2018 and references therein); (H) the Yangtze Block (Qiu et al., 2000; Zhang et al., 2006a, b; Zheng et al., 2006; Duan et al., 2011); (I) the Southern North China Block (N-CB) (Li et al., 2010b; Li and Huang, 2013; Zhu et al., 2014; Shao et al., 2016); (J) the Longmenshan Thrust Belt (LTB) (Duan et al., 2011; Chen et al., 2016c; Mao et al., 2021); (K) the Yidun Terrane (YDT) (Wang et al., 2013a; Wu et al., 2016; Liu et al., 2021b); (L) the Kangdian Paleo–land (KPL) (Zhou et al., 2002; Geng et al., 2007; Lin et al., 2007; Lin et al., 2010)\u003c/p\u003e","description":"","filename":"11.png","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/9fa1d77527ae5d2b33bf4c25.png"},{"id":81313085,"identity":"5f95b70c-de08-4a30-a3ec-ce9998637a9d","added_by":"auto","created_at":"2025-04-24 15:44:51","extension":"png","order_by":12,"title":"Figure 12","display":"","copyAsset":false,"role":"figure","size":830419,"visible":true,"origin":"","legend":"\u003cp\u003eComparison of εHf(t) values for zircons from the study area and adjacent areas. The QOB data are from Zhu et al., 2009; Wang et al., 2009; Wang et al., 2012; Zhou et al., 2016a; Shi et al., 2017; Huang et al., 2020a; and Qin et al., 2021. The ~1800 Ma age is based on detrital zircon data from the N-CB. The SGT detrital zircon data are from Liu et al., 2021b. The YZB data are from Zheng et al., 2006; Lin et al., 2007; Yu et al., 2009; Peng et al., 2012; Wang et al., 2012; Hu et al., 2013; Meng et al., 2015. The Yidun magmatic arc data are from Reid et al., 2007; He et al., 2013; Peng et al., 2014; and Wu et al., 2017. The Paleo‒Tethys volcanism data are from Chuan et al., 2023.\u003c/p\u003e","description":"","filename":"12.png","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/a182e69f29f8e48cdcac0241.png"},{"id":81313082,"identity":"b23f1f54-9ee1-4255-a5dc-ca4b35730d09","added_by":"auto","created_at":"2025-04-24 15:44:51","extension":"png","order_by":13,"title":"Figure 13","display":"","copyAsset":false,"role":"figure","size":1030135,"visible":true,"origin":"","legend":"\u003cp\u003e(A) La–Th–Sc diagram for discriminating the tectonic setting; (B) Th–Co–Zr/10 diagram for discriminating the tectonic setting; (C) Th–Sc–Zr/10 diagram for discriminating the tectonic setting (Bhatia and Crook, 1986)\u003c/p\u003e\n\u003cp\u003e1=oceanic island arc; 2=continental island arc; 3=active continental margin; 4=passive continental margin\u003c/p\u003e","description":"","filename":"13.png","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/bc35d23b60f7a4304cd6ec51.png"},{"id":81313083,"identity":"a0d3fd3e-e953-47fb-bc98-4d1d95799d80","added_by":"auto","created_at":"2025-04-24 15:44:51","extension":"png","order_by":14,"title":"Figure 14","display":"","copyAsset":false,"role":"figure","size":1370695,"visible":true,"origin":"","legend":"\u003cp\u003eDiscrimination diagram of crystallization ages (CAs), deposition ages (DAs), and cumulative proportions (CDPs) (modified from Cawood et al. 2012). A – convergent setting; B – collisional setting; C – extensional setting. The depositional ages were constrained by the youngest detrital zircons in this study.\u003c/p\u003e","description":"","filename":"14.png","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/fe05989a7b85dfbdd352c53c.png"},{"id":81313611,"identity":"ab496690-6339-49e2-a919-7ce34e211b67","added_by":"auto","created_at":"2025-04-24 15:52:52","extension":"png","order_by":15,"title":"Figure 15","display":"","copyAsset":false,"role":"figure","size":1746086,"visible":true,"origin":"","legend":"\u003cp\u003eSchematic diagram depicting of main source direction of the southwestern YZB during the Late Triassic to Middle Jurassic.\u003c/p\u003e","description":"","filename":"15.png","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/d9a31e86ed7d1178b3ae1c52.png"},{"id":86179204,"identity":"88df850f-8fd6-4b42-81d8-49e7229e4722","added_by":"auto","created_at":"2025-07-07 16:17:13","extension":"pdf","order_by":0,"title":"","display":"","copyAsset":false,"role":"manuscript-pdf","size":84132197,"visible":true,"origin":"","legend":"","description":"","filename":"manuscript.pdf","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/7e75ff38-f028-4baf-96d1-51cf68483036.pdf"},{"id":81313581,"identity":"71c848de-e3ba-46be-a772-c58b352322f0","added_by":"auto","created_at":"2025-04-24 15:52:50","extension":"xlsx","order_by":0,"title":"","display":"","copyAsset":false,"role":"supplement","size":24455,"visible":true,"origin":"","legend":"","description":"","filename":"SupplementaryData1.xlsx","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/927ab65fb0da7ce1cdd919c1.xlsx"},{"id":81313582,"identity":"85dd5abf-9fe1-4013-a25c-22656f9168d4","added_by":"auto","created_at":"2025-04-24 15:52:50","extension":"xlsx","order_by":1,"title":"","display":"","copyAsset":false,"role":"supplement","size":30641,"visible":true,"origin":"","legend":"","description":"","filename":"SupplementaryData3.xlsx","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/7d9b4305627b5e9c12264d19.xlsx"},{"id":81313131,"identity":"79ea86c0-4ff0-4a22-ad72-8e6e6034edb6","added_by":"auto","created_at":"2025-04-24 15:44:54","extension":"xlsx","order_by":2,"title":"","display":"","copyAsset":false,"role":"supplement","size":113644,"visible":true,"origin":"","legend":"","description":"","filename":"SupplementaryData2.xlsx","url":"https://assets-eu.researchsquare.com/files/rs-5860486/v1/845f43be67a97ac1a060af0a.xlsx"}],"financialInterests":"No competing interests reported.","formattedTitle":"Provenance and tectonic settings of Late Triassic–Jurassic deposits in the southwestern margin of the Yangtze Block: Evidence from whole-rock elemental compositions and detrital zircon U‒Pb ages and Hf isotopes, SW China","fulltext":[{"header":"1. Introduction","content":"\u003cp\u003eOwing to the uplift of the Qinling Orogenic Belt (QOB) and Longmenshan Thrust Belt (LTB), the Sichuan Basin (SCB) on the western margin of the Yangtze Block (YZB) changed from a marine environment to a continental sedimentary setting. Many clastic rocks were deposited in the SCB. In the western part of the SCB, the foreland basin has developed and evolved. The sediments in the foreland basin can reflect the orogen process of the orogenic belt around the foreland basin. Orogenic belts significantly influence sedimentary rocks in basins, which offers valuable insights into the history of adjacent mountain belts (Sircombe and Freeman, \u003cspan citationid=\"CR133\" class=\"CitationRef\"\u003e1999\u003c/span\u003e; Kelty et al., \u003cspan citationid=\"CR61\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; Luo et al., \u003cspan citationid=\"CR95\" class=\"CitationRef\"\u003e2014\u003c/span\u003e; Li et al., \u003cspan citationid=\"CR73\" class=\"CitationRef\"\u003e2018\u003c/span\u003e). By analyzing the Mesozoic clastic rock sediments in the SCB, the evolution of the peripheral orogenic belt can be predicted, such as the QOB and LTB.\u003c/p\u003e \u003cp\u003eHowever, opinions differ on the orogenic belts that controls the Sichuan foreland basin. Some scholars believe that the western Sichuan foreland basin was controlled by the QOB, its main provenance was the QOB in the north, and the LTB was not uplifted in the Late Triassic. The SCB is connected to the entire Songpan-ganzi Thrust Belt (SGT) in the west (Ma et al., \u003cspan citationid=\"CR98\" class=\"CitationRef\"\u003e2009\u003c/span\u003e; Deng et al., \u003cspan citationid=\"CR19\" class=\"CitationRef\"\u003e2012\u003c/span\u003e; Mei, \u003cspan citationid=\"CR102\" class=\"CitationRef\"\u003e2014\u003c/span\u003e; Luo et al., \u003cspan citationid=\"CR95\" class=\"CitationRef\"\u003e2014\u003c/span\u003e; Yu, \u003cspan citationid=\"CR169\" class=\"CitationRef\"\u003e2016\u003c/span\u003e; Zhu et al., \u003cspan citationid=\"CR195\" class=\"CitationRef\"\u003e2017\u003c/span\u003e; Yu and Liang, \u003cspan citationid=\"CR170\" class=\"CitationRef\"\u003e2017\u003c/span\u003e; Mu et al., \u003cspan citationid=\"CR109\" class=\"CitationRef\"\u003e2019\u003c/span\u003e; Mu, \u003cspan citationid=\"CR108\" class=\"CitationRef\"\u003e2020\u003c/span\u003e). Other scholars believe that during the Late Triassic Indosinian movement, owing to the southeastward thrusting activity of the SGT, the LTB formed; that is, in the Late Triassic, the western Sichuan foreland basin was controlled by the uplift of the LTB and was the main provenance area (Ratschbacher et al., \u003cspan citationid=\"CR118\" class=\"CitationRef\"\u003e2003\u003c/span\u003e; Meng et al., \u003cspan citationid=\"CR104\" class=\"CitationRef\"\u003e2005\u003c/span\u003e; Zheng et al., \u003cspan citationid=\"CR190\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; Shi et al., \u003cspan citationid=\"CR130\" class=\"CitationRef\"\u003e2010\u003c/span\u003e; Li et al., \u003cspan citationid=\"CR71\" class=\"CitationRef\"\u003e2014\u003c/span\u003e; Chen et al., \u003cspan citationid=\"CR6\" class=\"CitationRef\"\u003e2016a\u003c/span\u003e; Chen et al., \u003cspan citationid=\"CR8\" class=\"CitationRef\"\u003e2021\u003c/span\u003e; Lu et al., \u003cspan citationid=\"CR89\" class=\"CitationRef\"\u003e2023\u003c/span\u003e; Gou et al., \u003cspan citationid=\"CR39\" class=\"CitationRef\"\u003e2024\u003c/span\u003e). Several scholars believe that the western SCB area was influenced by the Kangdian Paleo\u0026ndash;Land (KPL) and the Emeishan Large Igneous Province (ELIP) in the Triassic (Zhu et al., \u003cspan citationid=\"CR195\" class=\"CitationRef\"\u003e2017\u003c/span\u003e; Zhang et al., \u003cspan citationid=\"CR179\" class=\"CitationRef\"\u003e2021\u003c/span\u003e). Moreover, it is doubtful whether the closing time of Songpan-Ganzi Ocean of the eastern branch of the Paleo-Tethys Ocean is Middle Triassic, Late Triassic or Early Jurassic (Li and Liu, \u003cspan citationid=\"CR64\" class=\"CitationRef\"\u003e2015\u003c/span\u003e; Jian et al., \u003cspan citationid=\"CR57\" class=\"CitationRef\"\u003e2019\u003c/span\u003e; Jackson et al., \u003cspan citationid=\"CR54\" class=\"CitationRef\"\u003e2020\u003c/span\u003e; Xu et al., \u003cspan citationid=\"CR156\" class=\"CitationRef\"\u003e2021\u003c/span\u003e; Yan et al., \u003cspan citationid=\"CR162\" class=\"CitationRef\"\u003e2022\u003c/span\u003e, \u003cspan citationid=\"CR161\" class=\"CitationRef\"\u003e2024\u003c/span\u003e). When the Sichuan Basin began to receive the provenance supply from Yidun Terrane (YDT) can provide constraints for the closure of Songpan-Ganzi Ocean. Therefore, this study may also provide sedimentary evidence for the evolution of the eastern side of the Paleo-Tethys Ocean.\u003c/p\u003e \u003cp\u003eThe detrital zircons that are preserved during weathering, transport, and sedimentation are key minerals for investigating provenances and understanding regional tectonics. U\u0026ndash;Pb geochronology plays an important role in understanding many sedimentary geological processes (Li et al., \u003cspan citationid=\"CR67\" class=\"CitationRef\"\u003e2010a\u003c/span\u003e; Zhang et al., \u003cspan citationid=\"CR178\" class=\"CitationRef\"\u003e2015\u003c/span\u003e; Shao et al., \u003cspan citationid=\"CR127\" class=\"CitationRef\"\u003e2016\u003c/span\u003e; Li et al., \u003cspan citationid=\"CR73\" class=\"CitationRef\"\u003e2018\u003c/span\u003e; Liu et al., \u003cspan citationid=\"CR87\" class=\"CitationRef\"\u003e2020\u003c/span\u003e). Moreover, zircon Hf isotopes can indicate sediment provenances more precisely. Detrital zircon U\u0026ndash;Pb ages and Hf isotope characteristics are widely used to indicate the tectonic history of rocks (Wu et al., \u003cspan citationid=\"CR151\" class=\"CitationRef\"\u003e2006\u003c/span\u003e; Zhou et al., \u003cspan citationid=\"CR194\" class=\"CitationRef\"\u003e2016a\u003c/span\u003e). When analysing many detrital zircons, these methods can be utilized to examine the provenance (Cawood et al., \u003cspan citationid=\"CR4\" class=\"CitationRef\"\u003e2007\u003c/span\u003e; Condie et al., \u003cspan citationid=\"CR16\" class=\"CitationRef\"\u003e2009\u003c/span\u003e; Hui et al., \u003cspan citationid=\"CR53\" class=\"CitationRef\"\u003e2017\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThe whole-rock elemental compositions of terrigenous clastic rocks are also widely used to determine potential provenances. Some stable elements, such as SiO\u003csub\u003e2\u003c/sub\u003e, Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e, TiO\u003csub\u003e2\u003c/sub\u003e, K\u003csub\u003e2\u003c/sub\u003eO, Fe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e, MgO, La, Th, Co, Y, Zr, Sc, Hf, and rare earth elements (REEs), could be good indicators for constraining the nature of clastic rocks and tectonic settings (Bhatia and Crook, \u003cspan citationid=\"CR1\" class=\"CitationRef\"\u003e1986\u003c/span\u003e; Floyd and Leveridge, \u003cspan citationid=\"CR33\" class=\"CitationRef\"\u003e1987\u003c/span\u003e; Girty, 1996; Hayashi et al., \u003cspan citationid=\"CR41\" class=\"CitationRef\"\u003e1997\u003c/span\u003e; Fralick and Kronberg, \u003cspan citationid=\"CR34\" class=\"CitationRef\"\u003e1997\u003c/span\u003e; Cullers, \u003cspan citationid=\"CR17\" class=\"CitationRef\"\u003e2000\u003c/span\u003e; Paikaray et al., \u003cspan citationid=\"CR112\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; Ma et al., \u003cspan citationid=\"CR97\" class=\"CitationRef\"\u003e2019\u003c/span\u003e; Xia et al., \u003cspan citationid=\"CR153\" class=\"CitationRef\"\u003e2021\u003c/span\u003e; Zhang et al., \u003cspan citationid=\"CR177\" class=\"CitationRef\"\u003e2022a\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eUsing the zircon U‒Pb ages and Hf isotope data from the detrital zircons obtained from the Triassic Xujiahe Formation and the Jurassic Ziliujing Formation, Shaximiao Formation and Suining Formation in the southern part of the western SCB, combined with results from previous studies, we analysed the provenance and evaluated the structural characteristics of the southwestern YZB during the Late Triassic to Jurassic period.\u003c/p\u003e"},{"header":"2. Geological setting","content":"\u003cp\u003eThe YZB is located in the west of the South China Block (S-CB), with the QOB and North China Block (N-CB) to the north, SGT to the west, Indochina Block to the south, and Jiangnan Orogenic Belt and Cathysia Block to the east. Located in the western part of the South China Block (S-CB) and YZB (Fig. \u003cspan class=\"InternalRef\"\u003e1\u003c/span\u003eA), the SCB is a large, complex superimposed basin that developed in the Precambrian crystalline basement (Zhang, \u003cspan class=\"CitationRef\"\u003e2002\u003c/span\u003e; Shen et al., \u003cspan class=\"CitationRef\"\u003e2009\u003c/span\u003e). Owing to the transitional position between Gondwana and Laurentia, complex basins formed (Ren, \u003cspan class=\"CitationRef\"\u003e1996\u003c/span\u003e; Li et al., \u003cspan class=\"CitationRef\"\u003e2006\u003c/span\u003e). Its western margin is separated from the SGT in the west by the LTB (He, \u003cspan class=\"CitationRef\"\u003e2014\u003c/span\u003e) and in the north by the QOB and the N-CB (Hao et al., \u003cspan class=\"CitationRef\"\u003e2008\u003c/span\u003e; Liu et al., \u003cspan class=\"CitationRef\"\u003e2021a\u003c/span\u003e).\u003c/p\u003e\n\u003cdiv id=\"Sec3\" class=\"Section2\"\u003e\n \u003ch2\u003e2.1 Qinling Orogenic Belt (QOB)\u003c/h2\u003e\n \u003cp\u003eThe QOB is an east‒west-trending orogenic belt with a length of approximately 1600 km and is located between the SCB and the NCB (Dong et al., \u003cspan class=\"CitationRef\"\u003e2022\u003c/span\u003e) (Fig. \u003cspan class=\"InternalRef\"\u003e1\u003c/span\u003eA, B); it can be divided into the North Qinling Orogenic Belt (NQB) and the South Qinling Orogenic Belt (SQB) by the Shangdan suture belt (Dong et al., \u003cspan class=\"CitationRef\"\u003e2011a\u003c/span\u003e; Zhang et al., \u003cspan class=\"CitationRef\"\u003e2015\u003c/span\u003e). The QOB evolved from the northernmost Paleo-Tethys Ocean (Chen and Santosh, \u003cspan class=\"CitationRef\"\u003e2014\u003c/span\u003e; Zhou et al, \u003cspan class=\"CitationRef\"\u003e2016a\u003c/span\u003e). The QOB underwent two major stages of geological evolution after the formation of igneous rocks and migmatites in the late Archean\u0026ndash;Neoproterozoic (Meng and Zhang, \u003cspan class=\"CitationRef\"\u003e2000\u003c/span\u003e): (a) in the Late Neoproterozoic to Middle Triassic, the South QOB and North QOB contained passive continental margin deposits in the northern and southern parts of the YZB and the NCB, respectively; (b) the Late Triassic orogeny was characterized by the development of thrust faults and foreland basins under the convergent setting of the SCB and NCB (Liu, \u003cspan class=\"CitationRef\"\u003e2006\u003c/span\u003e; Enkelmann et al., \u003cspan class=\"CitationRef\"\u003e2006\u003c/span\u003e; Chen, \u003cspan class=\"CitationRef\"\u003e2011\u003c/span\u003e; Tian et al., \u003cspan class=\"CitationRef\"\u003e2012\u003c/span\u003e; Wang et al., \u003cspan class=\"CitationRef\"\u003e2015\u003c/span\u003e; Chen et al., \u003cspan class=\"CitationRef\"\u003e2015\u003c/span\u003e). The SQB is mainly composed of Precambrian metamorphic crystalline basement (including gneiss, amphibolite, schist, quartzite) (~\u0026thinsp;2500 Ma, ~\u0026thinsp;744 Ma), Paleozoic clastic rocks (~\u0026thinsp;445 Ma), and Triassic volcanic rocks (~\u0026thinsp;224 Ma) (Dong et al., \u003cspan class=\"CitationRef\"\u003e2011a\u003c/span\u003e, \u003cspan class=\"CitationRef\"\u003eb\u003c/span\u003e; Dong et al., \u003cspan class=\"CitationRef\"\u003e2013\u003c/span\u003e; Hu et al., \u003cspan class=\"CitationRef\"\u003e2013\u003c/span\u003e; Li et al., \u003cspan class=\"CitationRef\"\u003e2018\u003c/span\u003e). The NQB is mainly composed of Paleoproterozoic and Neoproterozoic ophiolite suites, gneiss, marble and amphibolite, Neoproterozoic metamorphic rocks, metamorphic sedimentary rocks, Early-Paleozoic ophiolite, metamorphic rocks, granite, gabbro, basalt, andesite, ultrabasic rocks and clastic rocks (~\u0026thinsp;2510 Ma, ~\u0026thinsp;1462 Ma, ~\u0026thinsp;937 Ma, and ~\u0026thinsp;403 Ma), and Triassic volcanic rocks (~\u0026thinsp;206 Ma) (Dong et al., \u003cspan class=\"CitationRef\"\u003e2011a\u003c/span\u003e, \u003cspan class=\"CitationRef\"\u003eb\u003c/span\u003e; Li et al., \u003cspan class=\"CitationRef\"\u003e2018\u003c/span\u003e).\u003c/p\u003e\n\u003c/div\u003e\n\u003cdiv id=\"Sec4\" class=\"Section2\"\u003e\n \u003ch2\u003e2.2 Longmenshan Thrust Belt (LTB)\u003c/h2\u003e\n \u003cp\u003eThe LTB extends from northeast to southwest and is approximately 500 km long. It is adjacent to the QOB in the north and the SGT in the middle and southern regions (Fig.\u0026nbsp;\u003cspan class=\"InternalRef\"\u003e1\u003c/span\u003eB) (Yan et al., \u003cspan class=\"CitationRef\"\u003e2011\u003c/span\u003e; Mu et al., \u003cspan class=\"CitationRef\"\u003e2019\u003c/span\u003e). After the Archean\u0026ndash;Paleoproterozoic or Neoproterozoic basement formed (Zhao and Zhou, 2008; Dong et al., \u003cspan class=\"CitationRef\"\u003e2011b\u003c/span\u003e; \u003cspan class=\"CitationRef\"\u003e2012\u003c/span\u003e; Deng et al., \u003cspan class=\"CitationRef\"\u003e2012\u003c/span\u003e; Meng et al., \u003cspan class=\"CitationRef\"\u003e2015\u003c/span\u003e), the LTB experienced two main stages of geological evolution: (a) a pre-Sinian to Triassic craton in a continental passive margin and (b) a Late Triassic orogenic stage that was characterized by the development of thrust faults, strike-slip faults and foreland basins under a compressional tectonic setting (Deng et al., \u003cspan class=\"CitationRef\"\u003e2012\u003c/span\u003e). The LTB can be further divided into northern, central and southern segments (Li et al., \u003cspan class=\"CitationRef\"\u003e2008\u003c/span\u003e; Jin et al., \u003cspan class=\"CitationRef\"\u003e2009\u003c/span\u003e), and the Jiaoziding complex, Pengguan complex and Baoxing complex usually form the core. The formation time of these complexes is mainly Neoproterozoic, and the lithology is mainly composed of granite, diabase, gabbro, metamorphic sedimentary rock, metamorphic volcanic rock (Lu, \u003cspan class=\"CitationRef\"\u003e2011\u003c/span\u003e; Yan et al., \u003cspan class=\"CitationRef\"\u003e2008\u003c/span\u003e; Li, \u003cspan class=\"CitationRef\"\u003e2014\u003c/span\u003e). The LTB is mainly composed of Precambrian clastic rocks (~\u0026thinsp;743 Ma, ~\u0026thinsp;849 Ma, and ~\u0026thinsp;940 Ma) and Paleozoic clastic rocks (~\u0026thinsp;500 Ma, ~\u0026thinsp;950 Ma, and ~\u0026thinsp;2500 Ma) (Duan et al., \u003cspan class=\"CitationRef\"\u003e2011\u003c/span\u003e; Chen et al., \u003cspan class=\"CitationRef\"\u003e2016c\u003c/span\u003e; Mao et al., \u003cspan class=\"CitationRef\"\u003e2021\u003c/span\u003e). The LTB experienced many periods of conversion from a subsidence area to a denudation area due to changes in sea level in the Paleozoic. The most recent transition to denudation before the Triassic occurred in the early Permian (Ma et al., \u003cspan class=\"CitationRef\"\u003e2009\u003c/span\u003e; Zheng et al., 2010; Mou et al., \u003cspan class=\"CitationRef\"\u003e2016\u003c/span\u003e).\u003c/p\u003e\n\u003c/div\u003e\n\u003cdiv id=\"Sec5\" class=\"Section2\"\u003e\n \u003ch2\u003e2.3 Songpan\u0026ndash;Ganzi Terrane (SGT)\u003c/h2\u003e\n \u003cp\u003eThe SGT is a triangular fold belt (Fig.\u0026nbsp;\u003cspan class=\"InternalRef\"\u003e1\u003c/span\u003eB) (Ding et al., \u003cspan class=\"CitationRef\"\u003e2013\u003c/span\u003e), the southern side of which is called the Ganzi\u0026ndash;Litang area. The SGT consists of pre-Sinian crystalline basement and Sinian-Paleozoic sedimentary strata, which are covered with extremely thick Triassic turbidite sedimentary strata (Roger et al., \u003cspan class=\"CitationRef\"\u003e2004\u003c/span\u003e; Xiao et al., \u003cspan class=\"CitationRef\"\u003e2007\u003c/span\u003e). The major provenance area of the extremely thick Triassic turbidite deposits in Songpan-Ganzi Terranes is the Qinling Orogenic Belt (Bruguier et al., \u003cspan class=\"CitationRef\"\u003e1997\u003c/span\u003e; Roger et al., \u003cspan class=\"CitationRef\"\u003e2004\u003c/span\u003e; Weislogel et al., \u003cspan class=\"CitationRef\"\u003e2006\u003c/span\u003e, \u003cspan class=\"CitationRef\"\u003e2010\u003c/span\u003e; Xiao et al., \u003cspan class=\"CitationRef\"\u003e2007\u003c/span\u003e; Luo et al., \u003cspan class=\"CitationRef\"\u003e2014\u003c/span\u003e; Mu et al., \u003cspan class=\"CitationRef\"\u003e2019\u003c/span\u003e). In the Late Triassic or later, due to the mutual squeezing between the YZB, NQB and SQB, the closure of the Paleo-Tethys Ocean led to shallow water depth in the SGT, and the flysch basin evolved into a fold belt during the Indosinian period, forming an orogenic belt (Seng\u0026ouml;r, \u003cspan class=\"CitationRef\"\u003e1985\u003c/span\u003e, Nie et al., \u003cspan class=\"CitationRef\"\u003e1994\u003c/span\u003e; Mei, \u003cspan class=\"CitationRef\"\u003e2014\u003c/span\u003e; Yan et al., \u003cspan class=\"CitationRef\"\u003e2018\u003c/span\u003e; Yan et al., \u003cspan class=\"CitationRef\"\u003e2019\u003c/span\u003e; Mu et al., \u003cspan class=\"CitationRef\"\u003e2019\u003c/span\u003e). The SGT is mainly composed of large Triassic flysch deposits (greater than 10 km) (Liu et al., \u003cspan class=\"CitationRef\"\u003e2015\u003c/span\u003e; Mu et al., \u003cspan class=\"CitationRef\"\u003e2019\u003c/span\u003e) with multiple age peaks at ~\u0026thinsp;266 Ma, ~\u0026thinsp;438 Ma, ~\u0026thinsp;824 Ma, and ~\u0026thinsp;1822 Ma (Chen et al., \u003cspan class=\"CitationRef\"\u003e2009\u003c/span\u003e) and a small amount of high-potassium calc-alkaline granite with an age of 215\u0026thinsp;\u0026plusmn;\u0026thinsp;3 Ma (Yuan et al., \u003cspan class=\"CitationRef\"\u003e2010\u003c/span\u003e).\u003c/p\u003e\n\u003c/div\u003e\n\u003cdiv id=\"Sec6\" class=\"Section2\"\u003e\n \u003ch2\u003e2.4 Yidun Terrane (YDT)\u003c/h2\u003e\n \u003cp\u003eThe YDT is tectonically located between the SGT and YZB (Fig.\u0026nbsp;\u003cspan class=\"InternalRef\"\u003e1\u003c/span\u003eB). The YDT and YZB have similar sedimentary strata and paleontological fossils from the Neoproterozoic and Paleozoic eras. The YDT has structural properties that are similar to those of the YZB (Song et al., \u003cspan class=\"CitationRef\"\u003e2004\u003c/span\u003e). Before the Paleozoic, the YDT consisted mainly of medium\u0026ndash;acid volcanic rocks and metamorphic clastic rocks, in the Paleozoic, it consisted mainly of carbonate rocks and volcanic rocks (Tian et al., \u003cspan class=\"CitationRef\"\u003e2023\u003c/span\u003e). During the Middle Triassic to Late Triassic, owing to the westwards subduction of the SGT, the YDT formed many types of volcanic rocks in the island arc area, including basalt, andesite, dacite, rhyolite and intermediate-acid magmatic intrusive rocks (Li and Liu et al., \u003cspan class=\"CitationRef\"\u003e2015\u003c/span\u003e; Wang et al., \u003cspan class=\"CitationRef\"\u003e2017\u003c/span\u003e). The peak ages of the clastic rocks in the YDT and SGT are similar (~\u0026thinsp;242 Ma, ~\u0026thinsp;438 Ma, ~\u0026thinsp;786 Ma and ~\u0026thinsp;1810 Ma) (Wang et al., \u003cspan class=\"CitationRef\"\u003e2013a\u003c/span\u003e; Wu et al., \u003cspan class=\"CitationRef\"\u003e2016\u003c/span\u003e; Liu et al., \u003cspan class=\"CitationRef\"\u003e2021b\u003c/span\u003e), and the peak ages of the volcanic rocks are ~\u0026thinsp;225 Ma and ~\u0026thinsp;216 Ma (Peng et al., \u003cspan class=\"CitationRef\"\u003e2014\u003c/span\u003e).\u003c/p\u003e\n\u003c/div\u003e\n\u003cdiv id=\"Sec7\" class=\"Section2\"\u003e\n \u003ch2\u003e2.5 Kangdian Paleo\u0026ndash;land (KPL)\u003c/h2\u003e\n \u003cp\u003eThe KPL is located on the western margin of the YZB (Fig. \u003cspan class=\"InternalRef\"\u003e1\u003c/span\u003eB) and is composed mainly of Neoproterozoic basement and overlying Paleozoic cover. The KPL contains many Neoproterozoic igneous complexes (Plagioclase amphibolite, granulite, granite, diorite, basic rock), a small number of metamorphic volcanoes, and sedimentary rocks, ranging in age from 650 to 939 Ma, and its age peak is 825 Ma (Zhou et al., \u003cspan class=\"CitationRef\"\u003e2002\u003c/span\u003e; Geng et al., \u003cspan class=\"CitationRef\"\u003e2007\u003c/span\u003e; Lin et al., \u003cspan class=\"CitationRef\"\u003e2007\u003c/span\u003e; Lin, \u003cspan class=\"CitationRef\"\u003e2010\u003c/span\u003e; Yao et al., \u003cspan class=\"CitationRef\"\u003e2022\u003c/span\u003e). The metamorphic mixed complex in the KPL usually represents the Neoproterozoic crystalline basement observed in the southwest of the YZB (Zhou et al., \u003cspan class=\"CitationRef\"\u003e2002\u003c/span\u003e; Geng et al., \u003cspan class=\"CitationRef\"\u003e2007\u003c/span\u003e; Lin et al., \u003cspan class=\"CitationRef\"\u003e2007\u003c/span\u003e; Lin, \u003cspan class=\"CitationRef\"\u003e2010\u003c/span\u003e; Dong et al., \u003cspan class=\"CitationRef\"\u003e2011c\u003c/span\u003e; Fan et al., \u003cspan class=\"CitationRef\"\u003e2015\u003c/span\u003e; Liu, \u003cspan class=\"CitationRef\"\u003e2020\u003c/span\u003e). Therefore, the U-Pb ages and Hf isotopes characteristics of the KPL zircon can represent the YZB. In addition, the ELIP, which formed between the Middle and Late Permian, has a similar location, so it may have a small amount of Middle and Late Permian age peaks when providing the provenance for the Triassic strata (Zhu et al., \u003cspan class=\"CitationRef\"\u003e2017\u003c/span\u003e; Zhang et al., \u003cspan class=\"CitationRef\"\u003e2021\u003c/span\u003e; Miao et al., \u003cspan class=\"CitationRef\"\u003e2021\u003c/span\u003e). However, the ELIP basalt provided a basic rock source and did not produce many zircons, so it is possible that zircons at approximately 260 Ma could not be detected.\u003c/p\u003e\n\u003c/div\u003e\n\u003cdiv id=\"Sec8\" class=\"Section2\"\u003e\n \u003ch2\u003e2.6 Stratigraphic sequences and sedimentary characteristics\u003c/h2\u003e\n \u003cp\u003eThe study area is located in the southwestern YZB, where Permian, Triassic, Jurassic and Cretaceous strata are widely exposed (Fig. \u003cspan class=\"InternalRef\"\u003e1\u003c/span\u003eC). The strata are dominated by clastic rocks and minor carbonate rocks. The Mesozoic clastic strata are widely exposed, including the Upper Triassic Xujiahe Formation and the Jurassic Ziliujing Formation, Shaximiao Formation, Suining Formation, and Penglaizhen Formation (Fig. \u003cspan class=\"InternalRef\"\u003e2\u003c/span\u003e).\u003c/p\u003e\n \u003cp\u003eThe thickness of the study section is approximately 600 m, and the formation is mainly composed of fine sandstone, siltstone and mudstone. Among them, the Triassic Xujiahe Formation is mainly composed of gravel-bearing sandstone (Fig. \u003cspan class=\"InternalRef\"\u003e3\u003c/span\u003eA), sandstone and coal (Fig. \u003cspan class=\"InternalRef\"\u003e3\u003c/span\u003eB) from alluvial fan margin facies, which are in parallel unconformity with the Jurassic strata; the gravel-bearing sandstone of the Ziliujing Formation (Fig. \u003cspan class=\"InternalRef\"\u003e3\u003c/span\u003eC) at the bottom of the Jurassic; and the purplish red and grey\u0026ndash;green fine sandstone and mudstone that were deposited in the delta front environment in which the Ziliujing Formation to the Shaximiao Formation formed. Various sedimentary structures, including ripple bedding, parallel bedding (Fig. \u003cspan class=\"InternalRef\"\u003e3\u003c/span\u003eD), wavy bedding and interference ripple marks (Fig. \u003cspan class=\"InternalRef\"\u003e3\u003c/span\u003eE), have been observed in the rocks. The Suining Formation is a brick-red fine sandstone and mudstone that was deposited in a lacustrine environment, and ripple marks can be observed (Fig. \u003cspan class=\"InternalRef\"\u003e3\u003c/span\u003eF). In addition, the thickness of the Xujiahe Formation decreases from the study area to the north.\u003c/p\u003e\n\u003c/div\u003e"},{"header":"3. Sampling and analytical methods","content":"\u003cp\u003eThe samples used in this study were taken from the Triassic Xujiahe Formation\u0026ndash;Jurassic Suining Formation section in southwestern Sichuan, and 21 sandstone samples obtained from the Xujiahe Formation, Ziliujing Formation, Shaximiao Formation and Suining Formation were used for the whole-rock geochemical analysis. In addition, samples XJH-Z1, YTP-1-Z1, YTP-7-Z1 and YTP-27-Z1 were collected (Fig. 2), and zircon U\u0026ndash;Pb dating and Hf isotope analysis were performed on 4 samples (Fig. 3). These zircon samples weighed at least 7 kg each and were used to select zircons.\u003c/p\u003e\n\u003cp\u003eThe samples were cleaned, ground to a 200 mesh powder, and analysed for major and trace elements by ZSX Primus Ⅱ XRF and Agilent 7700e ICP-MS at Wuhan SampleSolution Analytical Technology Co., Ltd., Wuhan, China, after the weathered surfaces were removed.\u003c/p\u003e\n\u003cp\u003eThe detrital zircons were separated, handpicked, mounted in epoxy, polished, and imaged at Langfang Yantuo Geological Service Co., Ltd., Langfang. Zircon U\u0026ndash;Pb isotopes and cathodoluminescence (CL) images were obtained using analytical scanning electron microscope (JSM-IT100) and LA\u0026ndash;MC\u0026ndash;ICP\u0026ndash;MS at the Key Laboratory for Sedimentary Basin and Oil and Gas Resources at the Chengdu Center of Geological Survey, China and Chengdu University of Technology. Data processing and Concordia diagrams were generated via the ICPMSDataCal 12.2 (Liu et al., 2008) and Isoplot 3.23 (Ludwig, 2003) software packages.\u003c/p\u003e\n\u003cp\u003eIn situ Hf isotope ratio analysis was conducted using a Neptune Plus LA\u0026ndash;ICP‒MS and a GeoLas HD excimer ArF laser ablation system at Wuhan Sample Solution Analytical Technology Co., Ltd., Hubei, China.\u003c/p\u003e"},{"header":"4. Results","content":"\u003cdiv id=\"Sec11\" class=\"Section2\"\u003e\n \u003ch2\u003e4.1 Petrography\u003c/h2\u003e\n \u003cp\u003eThe samples from the Xujiahe Formation (XJH-Z1) are obviously different from those from the Jurassic (YTP-1-Z1, YTP-7-Z1 and YTP-27-Z1). Thin section analysis reveals that the sandstone samples of the Xujiahe Formation have coarse grain sizes, poor sorting, and subangular grains and are mainly composed of quartz (approximately 50%); the lithic fragments account for a high proportion (approximately 35%) of the sample; they are mainly consist of metamorphic, volcanic and sedimentary fragments, including granite, extrusive rocks, slate, phyllite, quartzite and mudstone fragments; the feldspar content is low, and it is mainly composed of K-feldspar and plagioclase (Fig. \u003cspan class=\"InternalRef\"\u003e4\u003c/span\u003eA). The sandstone samples from the Ziliujing Formation (YTP-1-Z1) have fine grain sizes, poor sorting, subangular to subrounded grains, and are mainly quartz, accounting for about 75% of all the clastic grains. The rock fragments contain about 20% lithic fragments, which are mainly quartzite, shale and sedimentary rock fragments (Fig. \u003cspan class=\"InternalRef\"\u003e4\u003c/span\u003eB).In addition to the clastic grains, the entire area also contains approximately 20% matrix. The sandstone samples of the Shaximiao Formation (YTP-7-Z1) have fine grain sizes; quartz contents of approximately 50%; rock fragment contents of approximately 40%; and they contain mainly quartzite, phyllite and sedimentary rock fragments (Fig. \u003cspan class=\"InternalRef\"\u003e4\u003c/span\u003eC). The sandstone samples of the Suining Formation (YTP-27-Z1) have fine grain sizes, quartz contents of approximately 50%, and rock fragment contents of approximately 40%, and contain mainly extrusive rocks, phyllite and sedimentary rock fragments (Fig. \u003cspan class=\"InternalRef\"\u003e4\u003c/span\u003eD).\u003c/p\u003e\n\u003c/div\u003e\n\u003cdiv id=\"Sec12\" class=\"Section2\"\u003e\n \u003ch2\u003e4.2 Whole-rock elemental compositions\u003c/h2\u003e\n \u003cdiv id=\"Sec13\" class=\"Section3\"\u003e\n \u003ch2\u003e4.2.1 Major elements\u003c/h2\u003e\n \u003cp\u003eThe contents of the major and trace elements are given in Supplementary Data 1. The SiO\u003csub\u003e2\u003c/sub\u003e contents in the Xujiahe Formation range from 70.35\u0026ndash;93.00%, with an average of 78.10%. The TiO\u003csub\u003e2\u003c/sub\u003e contents range from 0.04 to 0.68%, with an average value of 0.42%; the Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e contents range between 2.91 and 13.92%, with an average of 9.46%; and the TFe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e contents range between 0.53 and 4.75%, with an average of 3.17%. The SiO\u003csub\u003e2\u003c/sub\u003e contents of the Ziliujing Formation range from 60.92\u0026ndash;88.30%, with an average of 70.94%. The TiO\u003csub\u003e2\u003c/sub\u003e contents range from 0.36 to 0.99%, with an average value of 0.75%; the Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e contents range between 5.67 and 21.73%, with an average of 14.47%; and the TFe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e contents range between 2.66 and 6.67%, with an average of 4.42%. The SiO\u003csub\u003e2\u003c/sub\u003e contents in the Shaximiao Formation range from 50.04\u0026ndash;89.17%, with an average of 70.64%. The TiO\u003csub\u003e2\u003c/sub\u003e contents range from 0.04\u0026ndash;0.68%, with an average value of 0.42%; the Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e contents range from 2.93\u0026ndash;18.37%, with an average of 10.49%; and the TFe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e contents range from 0.45\u0026ndash;7.52%, with an average of 3.12%. The SiO\u003csub\u003e2\u003c/sub\u003e contents in the Suining Group range from 59.11\u0026ndash;85.17%, with an average of 72.14%. The TiO\u003csub\u003e2\u003c/sub\u003e contents range from 0.42 to 0.58%, with an average value of 0.50; the Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e contents range from 7.06\u0026ndash;11.51%, with an average of 9.28%; and the TFe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e contents range from 1.92\u0026ndash;4.69%, with an average of 3.30%. Compared with those of the upper continental crust (UCC; Rudnick and Gao, \u003cspan class=\"CitationRef\"\u003e2003\u003c/span\u003e), the sandstone samples have higher SiO\u003csub\u003e2\u003c/sub\u003e contents (average of 71.05%) and lower TiO\u003csub\u003e2\u003c/sub\u003e contents (average of 0.58%). The Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e contents are low (average of 11.08%), and the TFe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e contents are low (average of 3.39%).\u003c/p\u003e\n \u003c/div\u003e\n \u003cdiv id=\"Sec14\" class=\"Section3\"\u003e\n \u003ch2\u003e4.2.2 Trace elements\u003c/h2\u003e\n \u003cp\u003eIn the chondrite-normalized rare earth element distribution diagram (Fig. \u003cspan class=\"InternalRef\"\u003e5\u003c/span\u003eA), all the samples present similar characteristics, with light rare earth element (LREE) enrichment, heavy rare earth element (HREE) flattening, and negative Eu anomalies. Only one sample (XJH-H0) presented significantly low levels of all rare earth elements. According to the UCC-normalized rare earth element distribution diagram (Fig. \u003cspan class=\"InternalRef\"\u003e5\u003c/span\u003eB), the remaining samples exhibit relatively flat patterns, except that the XJH-H0 sample has significantly lower values than the UCC.\u003c/p\u003e\n \u003c/div\u003e\n\u003c/div\u003e\n\u003cdiv id=\"Sec15\" class=\"Section2\"\u003e\n \u003ch2\u003e4.3 U\u0026ndash;Pb ages of detrital zircons\u003c/h2\u003e\n \u003cp\u003eA total of 316 data points were detected in the 4 samples, and 309 data points had a concordance\u0026thinsp;\u0026ge;\u0026thinsp;90%. Samples with ages greater than 1000 Ma were selected for \u003csup\u003e207\u003c/sup\u003ePb/\u003csup\u003e206\u003c/sup\u003ePb dating, and younger samples were selected for \u003csup\u003e206\u003c/sup\u003ePb/\u003csup\u003e238\u003c/sup\u003eU dating. The LA\u0026ndash;ICP\u0026ndash;MS zircon U\u0026ndash;Pb data are given in Supplementary Data 2. Most grains are transparent to semitransparent. A representative zircon cathodoluminescence (CL) image is shown in Fig. \u003cspan class=\"InternalRef\"\u003e7\u003c/span\u003e. The grain lengths are generally 100\u0026ndash;200 \u0026micro;m, and the length-to-width ratios range from 1:1\u0026ndash;3:1. The zircon grains are well preserved and have long to rounded shapes. Most of the zircon grains exhibit oscillatory zoning, with Th/U ratios\u0026thinsp;\u0026gt;\u0026thinsp;0.1, indicating a magmatic origin.\u003c/p\u003e\n \u003cdiv id=\"Sec16\" class=\"Section3\"\u003e\n \u003ch2\u003e4.3.1 Sample XJH-Z1\u003c/h2\u003e\n \u003cp\u003eIn the sample XJH-Z1, 78 of the 80 analysed zircons had\u0026thinsp;\u0026ge;\u0026thinsp;90% concordance. All the zircons range in age from 689 to 953 Ma (Fig. \u003cspan class=\"InternalRef\"\u003e7\u003c/span\u003eA) and exhibit only one age peak (Fig. \u003cspan class=\"InternalRef\"\u003e8\u003c/span\u003eA), with a weighted mean age of 831\u0026thinsp;\u0026plusmn;\u0026thinsp;14 Ma; only one age is older than 900 Ma, two ages are younger than 700 Ma, and 13 ages are within 700\u0026ndash;800 Ma. The remaining 62 ages are in the 800\u0026ndash;900 Ma range.\u003c/p\u003e\n \u003c/div\u003e\n \u003cdiv id=\"Sec17\" class=\"Section3\"\u003e\n \u003ch2\u003e4.3.2 Sample YTP-1-Z1\u003c/h2\u003e\n \u003cp\u003eIn the YTP-1-Z1 sample, 85 of the 86 data points have concordances\u0026thinsp;\u0026ge;\u0026thinsp;90%, showing five age groups of 198\u0026ndash;443 Ma, 753\u0026ndash;952 Ma, 1853\u0026ndash;1917 Ma and 2350\u0026ndash;2543 Ma (Fig.\u0026nbsp;\u003cspan class=\"InternalRef\"\u003e7\u003c/span\u003eB). The dominant peak is at 206\u0026thinsp;\u0026plusmn;\u0026thinsp;2 Ma (n\u0026thinsp;=\u0026thinsp;19), and the subordinate peak ages are 290\u0026thinsp;\u0026plusmn;\u0026thinsp;3 Ma (n\u0026thinsp;=\u0026thinsp;7), 434\u0026thinsp;\u0026plusmn;\u0026thinsp;4 Ma (n\u0026thinsp;=\u0026thinsp;8), 788\u0026thinsp;\u0026plusmn;\u0026thinsp;7 Ma (n\u0026thinsp;=\u0026thinsp;6), 1866\u0026thinsp;\u0026plusmn;\u0026thinsp;16 Ma (n\u0026thinsp;=\u0026thinsp;14), and 2531\u0026thinsp;\u0026plusmn;\u0026thinsp;18 Ma (n\u0026thinsp;=\u0026thinsp;13) (Fig.\u0026nbsp;\u003cspan class=\"InternalRef\"\u003e8\u003c/span\u003eB). The youngest age of the zircon grains is 198\u0026thinsp;\u0026plusmn;\u0026thinsp;2 Ma, and the oldest is 2861\u0026thinsp;\u0026plusmn;\u0026thinsp;13 Ma. From the single-grain zircon, the youngest zircon U‒Pb age of sample YTP-1-Z1 from the bottom of the Jurassic strata is 198.7 Ma (Supplementary Data 2), which is similar to the bottom boundary age of the Jurassic strata in the global standard stratified profile (201.3\u0026thinsp;\u0026plusmn;\u0026thinsp;0.2 Ma; Huang, \u003cspan class=\"CitationRef\"\u003e2019\u003c/span\u003e) and the bottom boundary age of the Jurassic strata in China (199.6 Ma) (Ogg, \u003cspan class=\"CitationRef\"\u003e2019\u003c/span\u003e; Huang, \u003cspan class=\"CitationRef\"\u003e2019\u003c/span\u003e), providing stratigraphic constraints for this study.\u003c/p\u003e\n \u003c/div\u003e\n \u003cdiv id=\"Sec18\" class=\"Section3\"\u003e\n \u003ch2\u003e4.3.3 Sample YTP-7-Z1\u003c/h2\u003e\n \u003c/div\u003e\n \u003cdiv id=\"Sec19\" class=\"Section3\"\u003e\n \u003cp\u003eIn the YTP-7-Z1 sample, 72 out of 75 data points have concordances\u0026thinsp;\u0026ge;\u0026thinsp;90%, showing five age groups of 209\u0026ndash;482 Ma, 750\u0026ndash;996 Ma, 1853\u0026ndash;2095 Ma and 2379\u0026ndash;2535 Ma (Fig. \u003cspan class=\"InternalRef\"\u003e7\u003c/span\u003eC). The dominant peak is at 433\u0026thinsp;\u0026plusmn;\u0026thinsp;5 Ma (n\u0026thinsp;=\u0026thinsp;12), and the subordinate peak ages are 210\u0026thinsp;\u0026plusmn;\u0026thinsp;3 Ma (n\u0026thinsp;=\u0026thinsp;7), 309\u0026thinsp;\u0026plusmn;\u0026thinsp;3 Ma (n\u0026thinsp;=\u0026thinsp;12), 815\u0026thinsp;\u0026plusmn;\u0026thinsp;8 Ma (n\u0026thinsp;=\u0026thinsp;7), 1875\u0026thinsp;\u0026plusmn;\u0026thinsp;25 Ma (n\u0026thinsp;=\u0026thinsp;3), and 2513\u0026thinsp;\u0026plusmn;\u0026thinsp;17 Ma (n\u0026thinsp;=\u0026thinsp;4) (Fig.\u0026nbsp;\u003cspan class=\"InternalRef\"\u003e8\u003c/span\u003eC). From the single-grain zircon, the youngest age of the zircon grains is 209\u0026thinsp;\u0026plusmn;\u0026thinsp;2 Ma, and the oldest is 2535\u0026thinsp;\u0026plusmn;\u0026thinsp;15 Ma.\u003c/p\u003e\n \u003c/div\u003e\n \u003cdiv id=\"Sec20\" class=\"Section3\"\u003e\n \u003ch2\u003e4.3.4 Sample YTP-27-Z1\u003c/h2\u003e\n \u003c/div\u003e\n \u003cdiv id=\"Sec21\" class=\"Section3\"\u003e\n \u003cp\u003eIn the YTP-27-Z1 sample, 74 out of 75 data points have concordances\u0026thinsp;\u0026ge;\u0026thinsp;90%, showing five age groups of 212\u0026ndash;483 Ma, 735\u0026ndash;990 Ma, 1861\u0026ndash;2056 Ma and 2440\u0026ndash;2598 Ma (Fig. \u003cspan class=\"InternalRef\"\u003e7\u003c/span\u003eD). The dominant peak is at 243\u0026thinsp;\u0026plusmn;\u0026thinsp;3 Ma (n\u0026thinsp;=\u0026thinsp;16), and the subordinate peak ages are 359\u0026thinsp;\u0026plusmn;\u0026thinsp;3 Ma (n\u0026thinsp;=\u0026thinsp;7), 455\u0026thinsp;\u0026plusmn;\u0026thinsp;5 Ma (n\u0026thinsp;=\u0026thinsp;13), 834\u0026thinsp;\u0026plusmn;\u0026thinsp;10 Ma (n\u0026thinsp;=\u0026thinsp;7), 1863\u0026thinsp;\u0026plusmn;\u0026thinsp;21 Ma (n\u0026thinsp;=\u0026thinsp;4), and 2462\u0026thinsp;\u0026plusmn;\u0026thinsp;19 Ma (n\u0026thinsp;=\u0026thinsp;3) (Fig.\u0026nbsp;\u003cspan class=\"InternalRef\"\u003e8\u003c/span\u003eD). From the single-grain zircon, the youngest age of the zircon is 198\u0026thinsp;\u0026plusmn;\u0026thinsp;2 Ma, and the oldest is 2798\u0026thinsp;\u0026plusmn;\u0026thinsp;18 Ma.\u003c/p\u003e\n \u003c/div\u003e\n\u003c/div\u003e\n\u003cdiv id=\"Sec22\" class=\"Section2\"\u003e\n \u003ch2\u003e4.4 Hf isotopes of detrital zircons\u003c/h2\u003e\n \u003cp\u003eSeventy-eight zircon grains were analysed via in situ zircon Hf isotope analysis (Supplementary Data 3). The \u003csup\u003e176\u003c/sup\u003eHf/\u003csup\u003e177\u003c/sup\u003eHf values of the zircons range from 0.281192 to 0.282745, and the \u003csup\u003e176\u003c/sup\u003eLu/\u003csup\u003e177\u003c/sup\u003eHf values range from 0.000143 to 0.003410. The \u003cem\u003e\u0026epsilon;\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(0)\u003c/sub\u003e values of the zircons range from \u0026minus;\u0026thinsp;55.9 to -1.0. The \u003cem\u003e\u0026epsilon;\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values of the zircons range from \u0026minus;\u0026thinsp;17.0 to 13.6. Their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM1\u003c/sub\u003e ages range from 717 to 2846 Ma, and their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM2\u003c/sub\u003e ages range from 823 to 3046 Ma.\u003c/p\u003e\n \u003cdiv id=\"Sec23\" class=\"Section3\"\u003e\n \u003ch2\u003e4.4.1 Sample XJH-Z1\u003c/h2\u003e\n \u003c/div\u003e\n \u003cdiv id=\"Sec24\" class=\"Section3\"\u003e\n \u003cp\u003eIn sample XJH-Z1, for the 689 to 953 Ma group, the \u003cem\u003e\u0026epsilon;\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values of the zircons range from \u0026minus;\u0026thinsp;3.2 to 9.8. Their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM1\u003c/sub\u003e ages range from 987 to 1419 Ma, and their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM2\u003c/sub\u003e ages range from 1044 to 1672 Ma.\u003c/p\u003e\n \u003c/div\u003e\n \u003cdiv id=\"Sec25\" class=\"Section3\"\u003e\n \u003ch2\u003e4.4.2 Sample YTP-1-Z1\u003c/h2\u003e\n \u003c/div\u003e\n \u003cdiv id=\"Sec26\" class=\"Section3\"\u003e\n \u003cp\u003eIn sample YTP-1-Z1, for the 198\u0026ndash;443 Ma group, the \u003cem\u003e\u0026epsilon;\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values of their zircons range from \u0026minus;\u0026thinsp;7.9 to 7.3, their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM1\u003c/sub\u003e ages range from 738 to 1153 Ma, and the \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM2\u003c/sub\u003e ages range from 871 to 1553 Ma. For the 753\u0026ndash;952 Ma group, the \u003cem\u003e\u0026epsilon;\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values of the zircons range from \u0026minus;\u0026thinsp;13.8 to 9.8, their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM1\u003c/sub\u003e ages range from 992 to 1893 Ma, and their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM2\u003c/sub\u003e ages range from 1061 to 2327 Ma. For the 1853\u0026ndash;1917 Ma group, the \u003cem\u003e\u0026epsilon;\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values of the zircons range from \u0026minus;\u0026thinsp;4.7 to 13.6, their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM1\u003c/sub\u003e ages range from 1722 to 2476 Ma, and their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM2\u003c/sub\u003e ages range from 1675 to 2712 Ma. For the 2350\u0026ndash;2543 Ma group, the \u003cem\u003e\u0026epsilon;\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values of the zircons range from 0.91 to 12.9, their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM1\u003c/sub\u003e ages range from 2344 to 2812 Ma, and their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM2\u003c/sub\u003e ages range from 2268 to 2922 Ma.\u003c/p\u003e\n \u003c/div\u003e\n \u003cdiv id=\"Sec27\" class=\"Section3\"\u003e\n \u003ch2\u003e4.4.3 Sample YTP-7-Z1\u003c/h2\u003e\n \u003c/div\u003e\n \u003cdiv id=\"Sec28\" class=\"Section3\"\u003e\n \u003cp\u003eIn sample YTP-7-Z1, for the 209\u0026ndash;482 Ma group, the \u003cem\u003e\u0026epsilon;\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values of the zircons range from \u0026minus;\u0026thinsp;8.6 to 0.7, their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM1\u003c/sub\u003e ages range from 861 to 1368 Ma, and their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM2\u003c/sub\u003e ages range from 1097 to 1715 Ma. For the 750\u0026ndash;996 Ma group, the \u003cem\u003e\u0026epsilon;\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values of the zircons range from \u0026minus;\u0026thinsp;13.8 to 7.5, their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM1\u003c/sub\u003e ages range from 1074 to 1919 Ma, and their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM2\u003c/sub\u003e ages range from 2349 to 2349 Ma. For the 2379\u0026ndash;2535 Ma group, the \u003cem\u003e\u0026epsilon;\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values of the zircons range from \u0026minus;\u0026thinsp;4.2 to 2.8, their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM1\u003c/sub\u003e ages range from 2676 to 2846 Ma, and their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM2\u003c/sub\u003e ages range from 2758 to 3046 Ma.\u003c/p\u003e\n \u003c/div\u003e\n \u003cdiv id=\"Sec29\" class=\"Section3\"\u003e\n \u003ch2\u003e4.4.4 Sample YTP-27-Z1\u003c/h2\u003e\n \u003c/div\u003e\n \u003cdiv id=\"Sec30\" class=\"Section3\"\u003e\n \u003cp\u003eIn sample YTP-27-Z1, for the 212\u0026ndash;483 Ma group, the \u003cem\u003e\u0026epsilon;\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values of the zircons range from \u0026minus;\u0026thinsp;14.3 to 8.7, their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM1\u003c/sub\u003e ages range from 717 to 1572 Ma, and their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM2\u003c/sub\u003e ages range from 823 to 2002 Ma. For the 735\u0026ndash;990 Ma group, the \u003cem\u003e\u0026epsilon;\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values of the zircons range from \u0026minus;\u0026thinsp;17.0 to 2.9, their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM1\u003c/sub\u003e ages range from 1281 to 2043 Ma, and their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM2\u003c/sub\u003e ages range from 1452 to 2543 Ma. For the 1861\u0026ndash;2056 Ma group, the \u003cem\u003e\u0026epsilon;\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values of the zircons range from \u0026minus;\u0026thinsp;5.8 to 1.7, their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM1\u003c/sub\u003e ages range from 2237 to 2532 Ma, and their \u003cem\u003eT\u003c/em\u003e\u003csub\u003eDM2\u003c/sub\u003e ages range from 2373 to 2786 Ma.\u003c/p\u003e\n \u003c/div\u003e\n\u003c/div\u003e"},{"header":"5. Discussion","content":"\u003cdiv id=\"Sec32\" class=\"Section2\"\u003e \u003ch2\u003e5.1 Sedimentary sorting\u003c/h2\u003e \u003cp\u003eThe major, trace and rare earth element data can reflect the nature of terrigenous clastic rocks and tectonic settings and include SiO\u003csub\u003e2\u003c/sub\u003e, Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e, TiO\u003csub\u003e2\u003c/sub\u003e, K\u003csub\u003e2\u003c/sub\u003eO, Fe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e, MgO, La, Th, Co, Zr, Sc, Hf, and REEs (Bhatia and Crook, \u003cspan citationid=\"CR1\" class=\"CitationRef\"\u003e1986\u003c/span\u003e; Floyd and Leveridge, \u003cspan citationid=\"CR33\" class=\"CitationRef\"\u003e1987\u003c/span\u003e; Girty, 1996; Hayashi et al., \u003cspan citationid=\"CR41\" class=\"CitationRef\"\u003e1997\u003c/span\u003e; Fralick and Kronberg, \u003cspan citationid=\"CR34\" class=\"CitationRef\"\u003e1997\u003c/span\u003e; Paikaray et al., \u003cspan citationid=\"CR112\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; Ma et al., \u003cspan citationid=\"CR97\" class=\"CitationRef\"\u003e2019\u003c/span\u003e; Xia et al., \u003cspan citationid=\"CR153\" class=\"CitationRef\"\u003e2021\u003c/span\u003e). However, before analysing the properties of terrigenous clastic rocks and the tectonic setting, it is necessary to determine whether the fractionation of elements in sediments is affected by the sorting of sedimentary processes (Zhang, \u003cspan citationid=\"CR174\" class=\"CitationRef\"\u003e2004\u003c/span\u003e; Singh, \u003cspan citationid=\"CR131\" class=\"CitationRef\"\u003e2009\u003c/span\u003e; Hou et al., \u003cspan citationid=\"CR45\" class=\"CitationRef\"\u003e2016\u003c/span\u003e; Wang et al., \u003cspan citationid=\"CR144\" class=\"CitationRef\"\u003e2018\u003c/span\u003e; Ren et al., \u003cspan citationid=\"CR121\" class=\"CitationRef\"\u003e2023\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThe diagrams of TFe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e versus TiO\u003csub\u003e2\u003c/sub\u003e, TFe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e and TiO\u003csub\u003e2\u003c/sub\u003e versus Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e reveal that TFe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e versus TiO\u003csub\u003e2\u003c/sub\u003e, TFe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e and TiO\u003csub\u003e2\u003c/sub\u003e versus Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e are strongly correlated (Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e9\u003c/span\u003eA, B, C), whereas Cr/Th, Th/Sc versus Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e, TiO\u003csub\u003e2\u003c/sub\u003e and Zr have almost no correlation (Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e9\u003c/span\u003eD, E, F, G, H, and I). These data indicate that the stable elements were not significantly affected by sedimentary sorting during deposition and can be used as effective indicators of the characteristics of the provenance region characteristics.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec33\" class=\"Section2\"\u003e \u003ch2\u003e5.2 Nature of source rocks\u003c/h2\u003e \u003cp\u003eThe TFe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e/Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e versus TiO\u003csub\u003e2\u003c/sub\u003e/Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e binary curve shows that all the samples plot far from basalt; many samples plot near the Post-Archean Australian Shale (PAAS), UCC and andesite; a small number of samples plot near granites; and only one sample from the Xujiahe Formation plots near felsic volcanic rocks (Fig.\u0026nbsp;\u003cspan refid=\"Fig9\" class=\"InternalRef\"\u003e10\u003c/span\u003eA), which indicates that it may be derived mainly from intermediate\u0026ndash;felsic igneous rocks.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eThe Zr/Sc and Th/Sc values can reflect changes in the sediment composition and degree of sorting. The Th/Sc values of sedimentary rocks reflect the average values in the provenance region, and the Zr/Sc ratios gradually increase as the sediments undergo diagenesis and as zircons are enriched (McLennan et al., \u003cspan citationid=\"CR101\" class=\"CitationRef\"\u003e1993\u003c/span\u003e). On the Th/Sc versus Zr/Sc diagram (Fig.\u0026nbsp;\u003cspan refid=\"Fig9\" class=\"InternalRef\"\u003e10\u003c/span\u003eB), except for one sample from the Xujiahe Formation, all the other samples range from andesite to felsic volcanic rocks and plot closer to the region of felsic volcanic rocks. Some of the samples exhibit characteristics of sediment recycling, indicating that the source rock may have been felsic volcanic rock and that the rock underwent recycling.\u003c/p\u003e \u003cp\u003eAccording to the diagram of the La/Th ratio to Hf (Floyd and Leveridge, \u003cspan citationid=\"CR33\" class=\"CitationRef\"\u003e1987\u003c/span\u003e), most of the studied samples plot in the source area of felsic rocks, whereas a small number of samples (mainly those from the Ziliujing Formation) plot in the area that has an increasing trend of old sedimentary components. These results indicate that there may be recycled old sediments in addition to intermediate\u0026ndash;acidic igneous rocks (Fig.\u0026nbsp;\u003cspan refid=\"Fig9\" class=\"InternalRef\"\u003e10\u003c/span\u003eC). The many sedimentary lithic fragments that are associated with the petrological characteristics also provide support (Fig.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec34\" class=\"Section2\"\u003e \u003ch2\u003e5.3 Provenance analysis\u003c/h2\u003e \u003cp\u003eSample XJH-Z1 from the Xujiahe Formation is significantly different from samples YTP-1-Z1, YTP-7-Z1, and YTP-27-Z1 from the Jurassic strata, with a single peak age of 689\u0026ndash;953 Ma (Fig.\u0026nbsp;\u003cspan refid=\"Fig10\" class=\"InternalRef\"\u003e11\u003c/span\u003eA). In contrast, the detrital zircon ages of the three Jurassic samples show four similar dominant age groups. Among them, the dominant age peak of sample YTP-1-Z1 was 206 Ma, that of sample YTP-7-Z1 was 433 Ma, and that of sample YTP-27-Z1 was 243 Ma; the subordinate age peaks are 788\u0026ndash;834 Ma, 1863\u0026ndash;1875 Ma, and 2462\u0026ndash;2531 Ma (Fig.\u0026nbsp;\u003cspan refid=\"Fig10\" class=\"InternalRef\"\u003e11\u003c/span\u003eB, C, and D).\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cdiv id=\"Sec35\" class=\"Section3\"\u003e \u003ch2\u003e5.3.1 U\u0026ndash;Pb ages and Hf values of detrital zircons\u003c/h2\u003e \u003cp\u003e(1) 2462\u0026ndash;2531 Ma\u003c/p\u003e \u003cp\u003eThe oldest age group of 2462\u0026ndash;2531 Ma corresponds to the Neoarchean to Paleoproterozoic basement in the YZB, such as the Kongling complex (Gao et al., \u003cspan citationid=\"CR35\" class=\"CitationRef\"\u003e1999\u003c/span\u003e; \u003cspan citationid=\"CR36\" class=\"CitationRef\"\u003e2011\u003c/span\u003e) and Huangtian basic rock mass (Fig.\u0026nbsp;\u003cspan refid=\"Fig10\" class=\"InternalRef\"\u003e11\u003c/span\u003eH) (Liu et al., \u003cspan citationid=\"CR87\" class=\"CitationRef\"\u003e2020\u003c/span\u003e). However, the sedimentary strata of the N-CB have obvious peak ages from the Neoarchean to the Paleoproterozoic (Li et al., \u003cspan citationid=\"CR69\" class=\"CitationRef\"\u003e1993\u003c/span\u003e; Darby and Gehrels, \u003cspan citationid=\"CR18\" class=\"CitationRef\"\u003e2006\u003c/span\u003e; Jian et al., \u003cspan citationid=\"CR57\" class=\"CitationRef\"\u003e2019\u003c/span\u003e) (Fig.\u0026nbsp;\u003cspan refid=\"Fig10\" class=\"InternalRef\"\u003e11\u003c/span\u003eF, G). Moreover, the 2462\u0026ndash;2531 Ma zircons are mostly well rounded, indicating a large transport distance. In addition, the \u003cem\u003eε\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values of this age group all plot near the QOB and YZB (Fig.\u0026nbsp;\u003cspan refid=\"Fig11\" class=\"InternalRef\"\u003e12\u003c/span\u003e). Therefore, zircons from the N-CB cannot be ruled out.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003e(2) 1863\u0026ndash;1875 Ma\u003c/p\u003e \u003cp\u003eThe 1863\u0026ndash;1875 Ma age group corresponds to the convergence and fragmentation of the Columbia supercontinent (Zhao et al., \u003cspan citationid=\"CR181\" class=\"CitationRef\"\u003e2002\u003c/span\u003e; Yin et al., \u003cspan citationid=\"CR167\" class=\"CitationRef\"\u003e2013\u003c/span\u003e; Chen et al., 2016b; Lu et al., \u003cspan citationid=\"CR90\" class=\"CitationRef\"\u003e2020\u003c/span\u003e), and the fragmentation of the supercontinent has been recorded in many old cratons worldwide (Zhao et al., \u003cspan citationid=\"CR181\" class=\"CitationRef\"\u003e2002\u003c/span\u003e; Cawood et al., \u003cspan citationid=\"CR5\" class=\"CitationRef\"\u003e2018\u003c/span\u003e), including the Dongling complex (Chen and Xing, 2016) and the Kongling complex (Yin et al., \u003cspan citationid=\"CR167\" class=\"CitationRef\"\u003e2013\u003c/span\u003e; Guo et al., \u003cspan citationid=\"CR38\" class=\"CitationRef\"\u003e2015\u003c/span\u003e) in the YZB and southern N-CB. Owing to the existence of magmatic records in both the YZB and the N-CB (Fig.\u0026nbsp;\u003cspan refid=\"Fig10\" class=\"InternalRef\"\u003e11\u003c/span\u003eI), it is impossible to determine whether the zircons originated from the YZB or N-CB. In terms of the \u003cem\u003eε\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values, the detrital zircons from the N-CB and those deposited in the QOB have negative values, whereas the \u003cem\u003eε\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values in the YZB have a wide range, and the data points plot near the YZB area (Fig.\u0026nbsp;\u003cspan refid=\"Fig11\" class=\"InternalRef\"\u003e12\u003c/span\u003e); therefore, the zircons in this age group are more likely to come from the YZB.\u003c/p\u003e \u003cp\u003e(3) 788\u0026ndash;834 Ma and 689\u0026ndash;953 Ma\u003c/p\u003e \u003cp\u003eThe age groups of 788\u0026ndash;834 Ma and 689\u0026ndash;953 Ma correspond to the fragmentation of the Rodinia supercontinent (Li et al., \u003cspan citationid=\"CR76\" class=\"CitationRef\"\u003e1999\u003c/span\u003e; Zhou et al., \u003cspan citationid=\"CR192\" class=\"CitationRef\"\u003e2002\u003c/span\u003e; Wang et al., \u003cspan citationid=\"CR140\" class=\"CitationRef\"\u003e2013b\u003c/span\u003e; Zhou et al., \u003cspan citationid=\"CR193\" class=\"CitationRef\"\u003e2014\u003c/span\u003e; Yang et al., \u003cspan citationid=\"CR165\" class=\"CitationRef\"\u003e2017\u003c/span\u003e). This age group is found in many magmatic rocks that are located on the southwestern margins of the YZB and QOB, including the Baoxing complex (Zhao et al., \u003cspan citationid=\"CR40\" class=\"CitationRef\"\u003e2008\u003c/span\u003ea; Meng et al., \u003cspan citationid=\"CR103\" class=\"CitationRef\"\u003e2015\u003c/span\u003e), Kangding complex (Zhou et al., \u003cspan citationid=\"CR192\" class=\"CitationRef\"\u003e2002\u003c/span\u003e), Pengguan complex (Ma et al., \u003cspan citationid=\"CR99\" class=\"CitationRef\"\u003e1996\u003c/span\u003e), Gongcai complex (Roger and Calassou, 1997) and Bikou Terrane (Wang et al., \u003cspan citationid=\"CR143\" class=\"CitationRef\"\u003e2012\u003c/span\u003e). These age groups are similar in age (Fig.\u0026nbsp;\u003cspan refid=\"Fig10\" class=\"InternalRef\"\u003e11\u003c/span\u003e) but have different \u003cem\u003eε\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values. The \u003cem\u003eε\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf(t)\u003c/em\u003e\u003c/sub\u003e values of the Bikou Terrane in the QOB are usually negative (Wang et al., \u003cspan citationid=\"CR143\" class=\"CitationRef\"\u003e2012\u003c/span\u003e; Mu, \u003cspan citationid=\"CR108\" class=\"CitationRef\"\u003e2020\u003c/span\u003e; Qin et al., \u003cspan citationid=\"CR116\" class=\"CitationRef\"\u003e2021\u003c/span\u003e); zircon samples from other areas of the QOB also exhibit similar characteristics (Zhu et al., \u003cspan citationid=\"CR197\" class=\"CitationRef\"\u003e2009\u003c/span\u003e), but some of them exhibit small positive values, whereas those from the YZB complex rocks usually exhibit positive values (Zhao et al., \u003cspan citationid=\"CR185\" class=\"CitationRef\"\u003e2008b\u003c/span\u003e; Meng et al., \u003cspan citationid=\"CR103\" class=\"CitationRef\"\u003e2015\u003c/span\u003e; Kang et al., \u003cspan citationid=\"CR59\" class=\"CitationRef\"\u003e2017\u003c/span\u003e). The KPL on the southwestern edge of the YZB contains many Neoproterozoic igneous complexes, a small number of metamorphic volcanoes, and sedimentary rocks, ranging in age from 650 to 939 Ma, and its age peak is 825 Ma (Fig.\u0026nbsp;\u003cspan refid=\"Fig10\" class=\"InternalRef\"\u003e11\u003c/span\u003eL) (Zhou et al., \u003cspan citationid=\"CR192\" class=\"CitationRef\"\u003e2002\u003c/span\u003e; Geng et al., \u003cspan citationid=\"CR37\" class=\"CitationRef\"\u003e2007\u003c/span\u003e; Lin et al., \u003cspan citationid=\"CR78\" class=\"CitationRef\"\u003e2007\u003c/span\u003e; Lin et al., 2010). In this age group, the zircon \u003cem\u003eε\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values of sample XJH-Z1 are positive, except for one data point with a small negative value, and all the data plot in the YZB (Fig.\u0026nbsp;\u003cspan refid=\"Fig11\" class=\"InternalRef\"\u003e12\u003c/span\u003e). In contrast, most of the three groups of Jurassic samples are negative, and only seven zircon grains have positive values, which is more consistent with the QOB. Therefore, the provenance of sample XJH-Z1 can be considered magmatic rocks related to the cracking of the Rodinia supercontinent in the YZB, whereas the Jurassic samples originated from the QOB. In addition, the zircon grains of sample XJH-Z1 are intact and angular (Fig.\u0026nbsp;\u003cspan refid=\"Fig12\" class=\"InternalRef\"\u003e6\u003c/span\u003eA) and can also be judged to be from a relatively proximal source.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003e(4) 200\u0026ndash;500 Ma\u003c/p\u003e \u003cp\u003eIn the range of 200\u0026ndash;500 Ma, the zircon U‒Pb ages have multiple age peaks (~\u0026thinsp;440 Ma, ~\u0026thinsp;310 Ma, and ~\u0026thinsp;210 Ma) (Fig.\u0026nbsp;\u003cspan refid=\"Fig10\" class=\"InternalRef\"\u003e11\u003c/span\u003eB, C, D). Among them, the ~\u0026thinsp;440 Ma peak is found in many magmatic rocks in the NQB, which is related to the closure of the Shangdan Ocean caused by the collision between the SQB and the NQB (Lu et al., \u003cspan citationid=\"CR92\" class=\"CitationRef\"\u003e2003\u003c/span\u003e; Zhang et al., \u003cspan citationid=\"CR173\" class=\"CitationRef\"\u003e2006b\u003c/span\u003e; Dong et al., \u003cspan citationid=\"CR26\" class=\"CitationRef\"\u003e2011a\u003c/span\u003e; Wang et al., \u003cspan citationid=\"CR145\" class=\"CitationRef\"\u003e2013c\u003c/span\u003e; \u003cspan citationid=\"CR146\" class=\"CitationRef\"\u003e2015\u003c/span\u003e; Li, \u003cspan citationid=\"CR72\" class=\"CitationRef\"\u003e2020\u003c/span\u003e); however, this age has rarely been reported in the YZB. The \u003cem\u003eε\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values for ~\u0026thinsp;440 Ma plot entirely within the region of the QOB (Fig.\u0026nbsp;\u003cspan refid=\"Fig11\" class=\"InternalRef\"\u003e12\u003c/span\u003e); therefore, zircons of this age can come from the QOB.\u003c/p\u003e \u003cp\u003eMoreover, ~\u0026thinsp;310 Ma ages are rarely recorded in the QOB and YZB and are recorded only in the Paleo-Mianlue Ocean between the SOB and NQB, which also corresponds to the expansion of the Paleo-Mianlue Ocean (Dong et al., \u003cspan citationid=\"CR29\" class=\"CitationRef\"\u003e1999\u003c/span\u003e; Li et al., \u003cspan citationid=\"CR68\" class=\"CitationRef\"\u003e2004\u003c/span\u003e; Dong et al., \u003cspan citationid=\"CR26\" class=\"CitationRef\"\u003e2011a\u003c/span\u003e; Zhang et al., \u003cspan citationid=\"CR172\" class=\"CitationRef\"\u003e2019\u003c/span\u003e; Li, \u003cspan citationid=\"CR72\" class=\"CitationRef\"\u003e2020\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThe ~\u0026thinsp;210 Ma peak is found in many rocks in the SQB, YZB, SGT and YDT, corresponding to the closure of the Paleo‒Tethys Ocean (Zhang et al., \u003cspan citationid=\"CR173\" class=\"CitationRef\"\u003e2006b\u003c/span\u003e; Jian et al., \u003cspan citationid=\"CR56\" class=\"CitationRef\"\u003e2009\u003c/span\u003e; Zi et al., \u003cspan citationid=\"CR198\" class=\"CitationRef\"\u003e2012\u003c/span\u003e; He et al., \u003cspan citationid=\"CR43\" class=\"CitationRef\"\u003e2013\u003c/span\u003e; Peng et al., \u003cspan citationid=\"CR115\" class=\"CitationRef\"\u003e2014\u003c/span\u003e; Wang et al., \u003cspan citationid=\"CR141\" class=\"CitationRef\"\u003e2017\u003c/span\u003e; Xu et al., \u003cspan citationid=\"CR155\" class=\"CitationRef\"\u003e2019\u003c/span\u003e). The Paleo-Mianlue Ocean was also closed at this time as part of the Paleo-Tethys Ocean (Dong and Santosh, \u003cspan citationid=\"CR24\" class=\"CitationRef\"\u003e2016\u003c/span\u003e; Dong et al., \u003cspan citationid=\"CR25\" class=\"CitationRef\"\u003e2021\u003c/span\u003e; Zhang et al., \u003cspan citationid=\"CR180\" class=\"CitationRef\"\u003e2022b\u003c/span\u003e; Huang et al., \u003cspan citationid=\"CR47\" class=\"CitationRef\"\u003e2024\u003c/span\u003e; Chuan et al., \u003cspan citationid=\"CR15\" class=\"CitationRef\"\u003e2024\u003c/span\u003e), so the zircon U‒Pb ages from the two provenances were not very different. However, the \u003cem\u003eε\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values in the QOB on the north side of the YZB are usually positive, whereas the \u003cem\u003eε\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values of the Paleo-Tethys volcanic rocks in the southern YZB are negative (Fig.\u0026nbsp;\u003cspan refid=\"Fig11\" class=\"InternalRef\"\u003e12\u003c/span\u003e); most \u003cem\u003eε\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values plot in the negative region, and a small number of \u003cem\u003eε\u003c/em\u003e\u003csub\u003e\u003cem\u003eHf\u003c/em\u003e(t)\u003c/sub\u003e values plot in the positive region. In addition, the zircon grains of this age group also have two characteristics: most are long, and a few are well rounded. In summary, most zircons of this age group originated from the YDT related to the Paleo-Tethys Ocean, and a small number came from the QOB. In addition, the ELIP rock province provided ~\u0026thinsp;260 Ma zircon grains (Shellnutt et al., \u003cspan citationid=\"CR128\" class=\"CitationRef\"\u003e2012\u003c/span\u003e; Huang et al., \u003cspan citationid=\"CR51\" class=\"CitationRef\"\u003e2022\u003c/span\u003e), but the samples do not exhibit a peak value at 260 Ma; therefore, this area is not discussed.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec36\" class=\"Section3\"\u003e \u003ch2\u003e5.3.2 Upper Triassic Xujiahe Formation\u003c/h2\u003e \u003cp\u003eThere are many Precambrian and Paleozoic sandstone deposits in the LTB, whose zircon age peaks are ~\u0026thinsp;500 Ma, ~\u0026thinsp;743 Ma, ~\u0026thinsp;849 Ma, ~\u0026thinsp;950 Ma, and ~\u0026thinsp;2500 Ma (Fig.\u0026nbsp;\u003cspan refid=\"Fig10\" class=\"InternalRef\"\u003e11\u003c/span\u003eJ) (Duan et al., \u003cspan citationid=\"CR30\" class=\"CitationRef\"\u003e2011\u003c/span\u003e; Chen et al., \u003cspan citationid=\"CR10\" class=\"CitationRef\"\u003e2016c\u003c/span\u003e; Mao et al., \u003cspan citationid=\"CR100\" class=\"CitationRef\"\u003e2021\u003c/span\u003e). If the provenance area of the Xujiahe Formation is the LTB, there is a lack of zircon age data for the sedimentary cover. Therefore, the single-age peak sandstone of the Xujiahe Formation obtained in this study indicates that the southern section of the LTB did not uplift in the Late Triassic and was not the provenance of the nearby southwestern YZB.\u003c/p\u003e \u003cp\u003eThe depositional time of the Xujiahe Formation is generally considered the Norian\u0026ndash;Rhaetian stage in the YZB (Lu et al., \u003cspan citationid=\"CR93\" class=\"CitationRef\"\u003e2013\u003c/span\u003e; Li et al., \u003cspan citationid=\"CR65\" class=\"CitationRef\"\u003e2017\u003c/span\u003e; Tong et al., \u003cspan citationid=\"CR138\" class=\"CitationRef\"\u003e2019\u003c/span\u003e; Jiang et al., \u003cspan citationid=\"CR55\" class=\"CitationRef\"\u003e2023\u003c/span\u003e). The global sea level change was less than 26 m during the Norian‒Rhaetian stage (Huang et al., \u003cspan citationid=\"CR52\" class=\"CitationRef\"\u003e2006\u003c/span\u003e; Xu et al., \u003cspan citationid=\"CR157\" class=\"CitationRef\"\u003e2012\u003c/span\u003e; Kelley et al., \u003cspan citationid=\"CR60\" class=\"CitationRef\"\u003e2014\u003c/span\u003e; Ruban et al., 2015; Ogg, \u003cspan citationid=\"CR111\" class=\"CitationRef\"\u003e2019\u003c/span\u003e). It has also been suggested that the subsidence of the KPL may have been caused by the eastwards shortening and loading of the western YZB, due to the collision of the YZB and SGT (Yan et al., \u003cspan citationid=\"CR164\" class=\"CitationRef\"\u003e2019\u003c/span\u003e). On the basis of our data, we propose that the KPL may have continued to provide terrigenous detritus during the Late Triassic, although some scholars consider the KPL to have been a settling region during the Late Triassic and Jurassic (He et al., \u003cspan citationid=\"CR42\" class=\"CitationRef\"\u003e2003\u003c/span\u003e; Chen et al., \u003cspan citationid=\"CR9\" class=\"CitationRef\"\u003e2011\u003c/span\u003e; Zhu et al., \u003cspan citationid=\"CR195\" class=\"CitationRef\"\u003e2017\u003c/span\u003e; Yan et al., \u003cspan citationid=\"CR164\" class=\"CitationRef\"\u003e2019\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThe KPL contains Neoproterozoic igneous complexes, a small number of metamorphic volcanoes and sedimentary rock, with an age peak of ~\u0026thinsp;825 Ma (~\u0026thinsp;650\u0026ndash;~939 Ma) (Zhou et al., \u003cspan citationid=\"CR192\" class=\"CitationRef\"\u003e2002\u003c/span\u003e; Geng et al., \u003cspan citationid=\"CR37\" class=\"CitationRef\"\u003e2007\u003c/span\u003e; Lin et al., \u003cspan citationid=\"CR78\" class=\"CitationRef\"\u003e2007\u003c/span\u003e; Lin et al., 2010). The zircon age distribution patterns of the XJH-Z1 samples are highly similar to those of the KPL samples. Moreover, XJH-Z1 rocks are characterized by coarse grain sizes, poor sorting, subangular particles, and intact and angular zircon particles, which support the view that the source of the Xujiahe Formation was near-source KPL rather than southern LTB (Ma et al., \u003cspan citationid=\"CR98\" class=\"CitationRef\"\u003e2009\u003c/span\u003e; Deng et al., \u003cspan citationid=\"CR19\" class=\"CitationRef\"\u003e2012\u003c/span\u003e; Mei, \u003cspan citationid=\"CR102\" class=\"CitationRef\"\u003e2014\u003c/span\u003e; Luo et al., \u003cspan citationid=\"CR95\" class=\"CitationRef\"\u003e2014\u003c/span\u003e; Yu, \u003cspan citationid=\"CR169\" class=\"CitationRef\"\u003e2016\u003c/span\u003e; Zhu et al., \u003cspan citationid=\"CR195\" class=\"CitationRef\"\u003e2017\u003c/span\u003e; Yu and Liang, \u003cspan citationid=\"CR170\" class=\"CitationRef\"\u003e2017\u003c/span\u003e; Mu et al., \u003cspan citationid=\"CR109\" class=\"CitationRef\"\u003e2019\u003c/span\u003e; Mu, \u003cspan citationid=\"CR108\" class=\"CitationRef\"\u003e2020\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eSince the northern section of the LTB was the first to respond to the closing of Songpan-Ganzi Ocean and the collision between the YZB and the N-CB, the uplift of the LTB was not a short process, but a gradual process from the north to the south ((Liu et al., \u003cspan citationid=\"CR85\" class=\"CitationRef\"\u003e2009\u003c/span\u003e; Li et al., \u003cspan citationid=\"CR75\" class=\"CitationRef\"\u003e2010c\u003c/span\u003e; Yan et al., \u003cspan citationid=\"CR163\" class=\"CitationRef\"\u003e2013\u003c/span\u003e; Zhu et al., \u003cspan citationid=\"CR195\" class=\"CitationRef\"\u003e2017\u003c/span\u003e; Huang et al., \u003cspan citationid=\"CR50\" class=\"CitationRef\"\u003e2020b\u003c/span\u003e; Lu et al., \u003cspan citationid=\"CR89\" class=\"CitationRef\"\u003e2023\u003c/span\u003e; Gou et al., \u003cspan citationid=\"CR39\" class=\"CitationRef\"\u003e2024\u003c/span\u003e), and the southern section of the LTB was the last uplift area. The detrital zircon distribution patterns of the Xujiahe Formation in other areas of SCB are different from those in the study area. The distribution patterns of zircon age with single peak value are relatively rare, but not without records (Yan et al., \u003cspan citationid=\"CR164\" class=\"CitationRef\"\u003e2019\u003c/span\u003e; Lu et al., \u003cspan citationid=\"CR89\" class=\"CitationRef\"\u003e2023\u003c/span\u003e). After considering factors such as paleocurrents directions, we think that the paleocurrent system may have mixed the detritic zircon records of the uplifted north and middle LTB, the north SGT, and the QOB in other areas. In the study area, only detritic zircon from the KPL were recorded.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec37\" class=\"Section3\"\u003e \u003ch2\u003e5.3.3 Jurassic\u003c/h2\u003e \u003cp\u003eZircons of the same age (~\u0026thinsp;850 Ma) in the Jurassic samples have ε\u003csub\u003e\u003cem\u003eHf(t)\u003c/em\u003e\u003c/sub\u003e values significantly different from those of sample XJH-Z1 (Fig.\u0026nbsp;\u003cspan refid=\"Fig10\" class=\"InternalRef\"\u003e11\u003c/span\u003e). The zircon age distribution patterns of samples YTP-1-Z1, YTP-7-Z1 and YTP-27-Z1 are highly similar to those of the SGT and YTD (Fig.\u0026nbsp;\u003cspan refid=\"Fig10\" class=\"InternalRef\"\u003e11\u003c/span\u003eE, K), and they are different from those of the LTB Precambrian‒Palaeozoic sedimentary cover. Therefore, it can be inferred that the provenance shifted and that the KPL provided little provenance in the Early Jurassic. The terrigenous detritus from the SGT and YDT areas could not be completely blocked by the LTB. The LTB had not yet reached its current scale, and the uplift scale of the southern LTB was even smaller than those of the northern and middle sections (Liu et al., \u003cspan citationid=\"CR85\" class=\"CitationRef\"\u003e2009\u003c/span\u003e; Li et al., \u003cspan citationid=\"CR75\" class=\"CitationRef\"\u003e2010c\u003c/span\u003e; Yan et al., \u003cspan citationid=\"CR163\" class=\"CitationRef\"\u003e2013\u003c/span\u003e; Huang et al., \u003cspan citationid=\"CR50\" class=\"CitationRef\"\u003e2020b\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eIn the Late Triassic, the SGT was still a sedimentary area that was sourced mainly from the QOB (Bruguier et al., \u003cspan citationid=\"CR2\" class=\"CitationRef\"\u003e1997\u003c/span\u003e; Weislogel et al., \u003cspan citationid=\"CR149\" class=\"CitationRef\"\u003e2006\u003c/span\u003e, \u003cspan citationid=\"CR148\" class=\"CitationRef\"\u003e2010\u003c/span\u003e; Luo et al., \u003cspan citationid=\"CR95\" class=\"CitationRef\"\u003e2014\u003c/span\u003e; Mu et al., \u003cspan citationid=\"CR109\" class=\"CitationRef\"\u003e2019\u003c/span\u003e), and the SGT and QOB had similar zircon age distribution pattern characteristics (Wang et al., \u003cspan citationid=\"CR139\" class=\"CitationRef\"\u003e2013a\u003c/span\u003e; Wu et al., \u003cspan citationid=\"CR150\" class=\"CitationRef\"\u003e2016\u003c/span\u003e; Liu et al., \u003cspan citationid=\"CR86\" class=\"CitationRef\"\u003e2021b\u003c/span\u003e). In the Early Jurassic, it was uplifted and provided detrital material for the southwestern YZB. In other words, the zircon U‒Pb ages of the Jurassic sandstone samples in the study area are similar to those of the SGT and QOB samples. According to the SE paleocurrents characteristics, the sample petromineral and geochemical characteristics of the Jurassic have the characteristics of recycled sediments.\u003c/p\u003e \u003cp\u003eThe differences in the petrological characteristics between the Xujiahe Formation samples and the Jurassic samples are significant (Fig.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003eA), which may represent changes in the provenance area. The Jurassic samples are characterized by low feldspar contents and rich sedimentary lithic fragments, which represent recycled sediments, and the contents of single-crystal quartz, sedimentary lithic fragments and clay minerals in the Ziliujing Formation (YTP-1-Z1) are significantly greater than those in the Shaximiao Formation (YTP-7-Z1) and Suining Formation (YTP-27-Z1) (Fig.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003eB, C, D). The textural maturity of the Ziliujing Formation is lower, indicating that the sediments within the Ziliujing Formation were probably sourced from proximal source(s). The sediments within the Shaximiao and Suining Formations experienced long-distance transport.\u003c/p\u003e \u003cp\u003eThe Middle and Late Jurassic samples show that the number of young zircons did not increase with gradual changes in strata, indicating that the SGT and YDT were in a relatively stable tectonic settings and lacked volcanic activity, at least from the Middle Jurassic to the Late Jurassic. The lack of volcanic rocks in the Middle‒Late Jurassic that are reported for the SGT and YDT also suggests that the tectonic setting is relatively stable (Yuan et al., \u003cspan citationid=\"CR171\" class=\"CitationRef\"\u003e2010\u003c/span\u003e; Peng et al., \u003cspan citationid=\"CR115\" class=\"CitationRef\"\u003e2014\u003c/span\u003e; Sigoyer et al., \u003cspan citationid=\"CR132\" class=\"CitationRef\"\u003e2014\u003c/span\u003e; Li and Liu, \u003cspan citationid=\"CR64\" class=\"CitationRef\"\u003e2015\u003c/span\u003e; Li et al., \u003cspan citationid=\"CR73\" class=\"CitationRef\"\u003e2018\u003c/span\u003e; Zhao et al., \u003cspan citationid=\"CR183\" class=\"CitationRef\"\u003e2020\u003c/span\u003e). The change in petrological characteristics may be due to the weathering and erosion of the southern LTB, which weakened the blocking effect of the LTB on the SGT and YDT, and more distant sources were transported to the study area.\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv id=\"Sec38\" class=\"Section2\"\u003e \u003ch2\u003e5.4 Tectonic settings\u003c/h2\u003e \u003cp\u003eIn addition, the whole-rock geochemical characteristics, such as the La, Th, Zr, Co, and Sc contents, of sedimentary rocks can be used to analyse the tectonic settings of the source area (Bhatia and Crook, \u003cspan citationid=\"CR1\" class=\"CitationRef\"\u003e1986\u003c/span\u003e; Wei et al., \u003cspan citationid=\"CR147\" class=\"CitationRef\"\u003e2009\u003c/span\u003e; Zheng et al., \u003cspan citationid=\"CR187\" class=\"CitationRef\"\u003e2019\u003c/span\u003e). On the La‒Th‒Sc triangular diagram (Fig.\u0026nbsp;\u003cspan refid=\"Fig13\" class=\"InternalRef\"\u003e13\u003c/span\u003eA), all the samples plot near the continental margin and continental island arc region, and no samples plot in the oceanic island arc region. On the Th‒Co‒Zr/10 triangular diagram (Fig.\u0026nbsp;\u003cspan refid=\"Fig13\" class=\"InternalRef\"\u003e13\u003c/span\u003eB), most of the samples plot within and around the continental island arc, no samples plot in the oceanic island arc region, and only five samples plot in the continental margin region. According to the Th‒Sc‒Zr/10 triangular diagram (Fig.\u0026nbsp;\u003cspan refid=\"Fig13\" class=\"InternalRef\"\u003e13\u003c/span\u003eC), most of the samples plot near the continental island arc and the passive continental margin regions, no samples are located in the oceanic island arc region, and only one sample is located in the passive continental margin region.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eThe La‒Th‒Sc, Th‒Co‒Zr/10 and Th‒Sc‒Zr/10 triangular diagrams suggest that the main provenance area was a continental island arc tectonic setting and that a small amount of material was derived from the continental margin.\u003c/p\u003e \u003cp\u003eThe detrital zircon age can also reflect the tectonic setting of sedimentary basins and can be divided into three main types: convergent basins, collisional basins and extensional basins (Cawood et al., \u003cspan citationid=\"CR3\" class=\"CitationRef\"\u003e2012\u003c/span\u003e). In the CDP diagram, all four samples plot within region B, so this region can be considered a collisional setting (Fig.\u0026nbsp;\u003cspan refid=\"Fig14\" class=\"InternalRef\"\u003e14\u003c/span\u003e). In the context of an arc\u0026ndash;continent or continent\u0026ndash;continent collision, the sample plots in region B lie in a collisional tectonic setting (Cawood et al., \u003cspan citationid=\"CR3\" class=\"CitationRef\"\u003e2012\u003c/span\u003e). However, the youngest zircon age in sample XJH-Z1 is 689 Ma, which cannot represent the stratigraphic depositional age. Therefore, in the Late Triassic, 215 Ma was selected as the stratigraphic depositional age (the Late Triassic depositional age was ~\u0026thinsp;237 to ~\u0026thinsp;201 Ma (Ogg, \u003cspan citationid=\"CR111\" class=\"CitationRef\"\u003e2019\u003c/span\u003e; Tong et al., \u003cspan citationid=\"CR138\" class=\"CitationRef\"\u003e2019\u003c/span\u003e), regardless of which value was selected as the depositional age, it had no effect on the results). Sample XJH-Z1 plots in region C (dashed line) (Fig.\u0026nbsp;\u003cspan refid=\"Fig14\" class=\"InternalRef\"\u003e14\u003c/span\u003e), representing an extensional setting. Therefore, the Xujiahe Formation samples represent an extensional setting, whereas the Jurassic samples represent a collisional setting.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec39\" class=\"Section2\"\u003e \u003ch2\u003e5.5 Implications\u003c/h2\u003e \u003cp\u003eMany sedimentary rocks in the tectonic setting of the passive continental margin were deposited on the western margin of the YZB during the Paleozoic (Zhou et al., \u003cspan citationid=\"CR45\" class=\"CitationRef\"\u003e2016\u003c/span\u003eb; Pan et al., \u003cspan citationid=\"CR113\" class=\"CitationRef\"\u003e2021\u003c/span\u003e). During the Middle Triassic to Late Triassic, owing to the westwards subduction of the SGT, the YDT developed basalt, andesite, dacite, rhyolite and intermediate-acid magmatic intrusive rocks in the island arc setting (Li and Liu et al., \u003cspan citationid=\"CR83\" class=\"CitationRef\"\u003e2015\u003c/span\u003e; Wang et al., \u003cspan citationid=\"CR141\" class=\"CitationRef\"\u003e2017\u003c/span\u003e). Combined with the NE paleocurrents directions of the Xujiahe Formation and the SE paleocurrents directions of the Jurassic (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e), as well as the large amounts of volcanic debris and sedimentary debris, it can be inferred that the main provenances of the Jurassic strata are the sedimentary rocks deposited early at the western margin of the SGT and YDT, and the island arc volcanic rocks from the YDT. Owing to the inclusion of many magmatic rocks from the YDT continental island arc, the La-Th-Sc, Th-Co-Zr/10 and Th-Sc-Zr/10 triangular maps (Fig.\u0026nbsp;\u003cspan refid=\"Fig10\" class=\"InternalRef\"\u003e11\u003c/span\u003e) are characterized by passive continental margins and island arcs. There is a lack of Mesozoic zircons in the Xujiahe Formation; in contrast, many Mesozoic zircons were found in the Jurassic, which means that the study area was still a passive continental margin in the Late Triassic, and it was not until the Jurassic that the island arc area in the YDT began to provide terrigenous detritus.\u003c/p\u003e \u003cp\u003eIn other words, in the Early Jurassic, the southwestern YZB experienced an evolutionary stage from a passive continental margin to a foreland basin rather than in the Late Triassic (Zhou et al., \u003cspan citationid=\"CR45\" class=\"CitationRef\"\u003e2016\u003c/span\u003eb; Liu et al., \u003cspan citationid=\"CR84\" class=\"CitationRef\"\u003e2017\u003c/span\u003e; Pan et al., \u003cspan citationid=\"CR113\" class=\"CitationRef\"\u003e2021\u003c/span\u003e). The CDP diagram has similar characteristics (Fig.\u0026nbsp;\u003cspan refid=\"Fig14\" class=\"InternalRef\"\u003e14\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eIn general, this study indicates that the main provenance of the southwestern YZB was the KPL in the Late Triassic. Since the Ganzi\u0026ndash;Litang Ocean on the southern side of SGT had not yet closed, the material of the YDT island arc could not have been transported to southwestern YZB. In the Early Jurassic, the SGT and YDT were transformed into provenance areas, and the LTB rose, but these changes were not sufficient to block the provenance input from the SGT and YDT (Fig.\u0026nbsp;\u003cspan refid=\"Fig15\" class=\"InternalRef\"\u003e15\u003c/span\u003e). In the Middle Jurassic, the LTB shrank due to weathering and erosion, and the SGT and YDT continued to enter the southwestern YZB as source areas. In this study, the closure time of the eastern branch of the Paleo-Tethys Ocean (Ganzi\u0026ndash;Litang Ocean) was no later than the early Early Jurassic.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003c/div\u003e"},{"header":"6. Conclusions","content":"\u003cp\u003e(1) Detrital zircons from the Xujiahe Formation samples originated from Neoproterozoic igneous complexes, a small number of metamorphic volcanoes, and sedimentary rocks on the KPL, whereas the detrital zircons from the Jurassic samples originated from Late Triassic detrital rocks deposited in the SGT and YDT after sedimentary recycling.\u003c/p\u003e \u003cp\u003e(2) Triassic detrital rocks were deposited on a passive continental margin, Jurassic clastic rocks were deposited in a continental island arc setting, and the source materials were medium\u0026ndash;acid igneous rocks and recycled sedimentary rocks.\u003c/p\u003e \u003cp\u003e(3) In the Early Jurassic, the LTB uplifted and provided source material for the southwestern YZB. The uplift time of the southern LTB can be confined to the Early Jurassic.\u003c/p\u003e \u003cp\u003e(4) In the Early Jurassic, there may have been a brief tectonic setting change from the passive continental margin to the foreland basin.\u003c/p\u003e"},{"header":"Declarations","content":"\u003cp\u003e\u003cstrong\u003eAcknowledgements\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eWe are grateful to the China Geological Survey for its financial support. I am grateful to Dr. Xiuping Wang, Dr. Yu Xia. and M.D. Weiwei Chen for their supports in the petrographic section. Constructive suggestions from three anonymous reviewers are acknowledged with thanks.\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eFunding\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eThis study was supported by National Natural Science Foundation of China [grant number 92055314], National Natural Science Foundation of China [grant number U2344209], and China Geological Survey [number: DD20242564].\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eCompeting Interests\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eThe authors declare no conflicts of interest.\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eAvailability of data and materials\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eThe data that support the findings of this study are available from the first author upon reasonable request.\u003c/p\u003e"},{"header":"References","content":"\u003col\u003e\n\u003cli\u003eBhatia, M.R., Crook, A.W., 1986. 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Science in China Series D: Earth Sciences 52(9), 1359\u0026ndash;1384.\u003c/li\u003e\n\u003cli\u003eWang, W., Liu, S.W., Feng, Y.G., Li, Q.G., Wu, F.H., Wang, Z.Q., Wang, R.T., Yang, P.T., 2012. Chronology, petrogenesis and tectonic setting of the Neoproterozoic Tongchang dioritic pluton at the northwestern margin of the Yangtze Block: constraints from geochemistry and zircon U\u0026ndash;Pb\u0026ndash;Hf isotopic systematics. Gondwana Research 22(2), 699\u0026ndash;716.\u003c/li\u003e\n\u003cli\u003eWang, W., Zeng, M.F., Zhou, M.F., Zhao, J.H., Zheng, J.P., Lan, Z.F., 2018. Age, provenance and tectonic setting of Neoproterozoic to early Paleozoic sequences in southeastern South China Block: Constraints on its linkage to western Australia-East Antarctica.Precambrian Research 309, 290\u0026ndash;308.\u003c/li\u003e\n\u003cli\u003eWang, X.X., Wang, T., Zhang, C.L., 2013c. 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Zircon U\u0026ndash;Pb age and Hf isotope evidence for 3.8 Ga crustal remnant and episodic reworking of Archean crust in South China. Earth and Planetary Science Letters 252, 56\u0026ndash;71.\u003c/li\u003e\n\u003cli\u003eZhang, T.F., Cheng, X.Y., Wang, S.Y., Miao, P.S., Ao, C., 2022a. Middle Jurassic-Early Cretaceous drastic paleoenvironmental changes in the Ordos Basin: Constraints on sandstone-type uranium mineralization. Ore Geology Reviews 142, 104652.\u003c/li\u003e\n\u003cli\u003eZhang, Y., Jia, D., Shen, L., Yin, H.W., Chen, Z.X., Li, H.B., Li, Z.G., Sun, C., 2015. Provenance of detrital zircons in the Late Triassic Sichuan foreland basin: constraints on the evolution of the Qinling Orogen and Longmen Shan thrust-fold belt in central China. International Geology Review 57(14), 1806\u0026ndash;1824.\u003c/li\u003e\n\u003cli\u003eZhang, Y.L., Jia, X.T., Wang, K.M., Wang, Z.Q., Chen, M.Y., 2021. 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Triassic collision in the Paleo-Tethys Ocean constrained by volcanic activity in SW China. Lithos 144, 145\u0026ndash;160.\u003c/li\u003e\n\u003c/ol\u003e"}],"fulltextSource":"","fullText":"","funders":[],"hasAdminPriorityOnWorkflow":false,"hasManuscriptDocX":true,"hasOptedInToPreprint":true,"hasPassedJournalQc":"","hasAnyPriority":false,"hideJournal":false,"highlight":"","institution":"","isAcceptedByJournal":true,"isAuthorSuppliedPdf":false,"isDeskRejected":"","isHiddenFromSearch":false,"isInQc":false,"isInWorkflow":false,"isPdf":false,"isPdfUpToDate":true,"isWithdrawnOrRetracted":false,"journal":{"display":true,"email":"[email protected]","identity":"scientific-reports","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":false,"externalIdentity":"scirep","sideBox":"Learn more about [Scientific Reports](http://www.nature.com/srep/)","snPcode":"","submissionUrl":"","title":"Scientific Reports","twitterHandle":"","acdcEnabled":true,"dfaEnabled":true,"editorialSystem":"stoa","reportingPortfolio":"Scientific Reports","inReviewEnabled":true,"inReviewRevisionsEnabled":true},"keywords":"Whole-rock elemental compositions, Detrital zircon, Hf isotopes, Provenance, SW Yangtze Block","lastPublishedDoi":"10.21203/rs.3.rs-5860486/v1","lastPublishedDoiUrl":"https://doi.org/10.21203/rs.3.rs-5860486/v1","license":{"name":"CC BY 4.0","url":"https://creativecommons.org/licenses/by/4.0/"},"manuscriptAbstract":"\u003cp\u003eDuring the Late Triassic to Jurassic, the western Yangtze Block transitioned from marine carbonate deposits to terrestrial detrital deposits. There are different views on the orogen evolution of the western margin of the Yangtze Block, such as whether the Longmenshan Thrust Belt was uplifted in the Late Triassic or Early Jurassic, and when the Yangtze Block began to receive the source from Yidun Terrane. In this paper, whole-rock elemental compositions and zircon U–Pb ages and Hf isotope data from the Upper Triassic to Jurassic successions are introduced. The whole-rock elemental compositions reveal that the clastic rocks were deposited in a collisional setting and were derived mainly from intermediate–felsic magmatic rocks and recycled sediments. The Upper Triassic zircon sample shows a single age peak at ~831 Ma. The three Jurassic samples show similar age patterns with four main age populations (e.g., 200–500 Ma, 788–834 Ma, 1863–1875 Ma, and 2462–2531 Ma). The results revealed that the Kangdian Palaeo-land was the main provenance area in the Late Triassic. In contrast, in the Early Jurassic (~198.7 Ma), the Longmenshan was massively uplifted, and the recycled sediments from the Longmenshan, Songpan–Ganzi Terrane and Yidun Terrane provided large amounts of detrital material to the southwestern Yangtze Block. Volcanic rocks from the Yidun Terrane also provided a partial source for the southwestern Yangtze Block. In the Middle Jurassic, owing to the weathering and erosion of the Longmenshan Thrust Belt in the Early Jurassic, the provenance supply in Longmenshan decreased, and the provenances from the Yidun Terrane and the Songpan–Ganzi Terrane increased. In the Late Triassic to the Early Jurassic, the tectonic setting of the southwestern Yangtze Block may have changed from a passive continental margin to a foreland basin.\u003c/p\u003e","manuscriptTitle":"Provenance and tectonic settings of Late Triassic–Jurassic deposits in the southwestern margin of the Yangtze Block: Evidence from whole-rock elemental compositions and detrital zircon U‒Pb ages and Hf isotopes, SW China","msid":"","msnumber":"","nonDraftVersions":[{"code":1,"date":"2025-04-24 15:44:45","doi":"10.21203/rs.3.rs-5860486/v1","editorialEvents":[{"type":"communityComments","content":0},{"type":"decision","content":"Revision requested","date":"2025-05-21T09:42:09+00:00","index":"","fulltext":""},{"type":"editorAssigned","content":"","date":"2025-05-21T09:28:57+00:00","index":"","fulltext":""},{"type":"editorInvitedReview","content":"","date":"2025-05-18T12:50:03+00:00","index":"hide","fulltext":""},{"type":"reviewerAgreed","content":"206144578257050476217909929393697936759","date":"2025-04-23T09:16:58+00:00","index":"hide","fulltext":""},{"type":"reviewersInvited","content":"","date":"2025-04-23T09:05:01+00:00","index":"","fulltext":""},{"type":"checksComplete","content":"","date":"2025-04-21T04:31:27+00:00","index":"","fulltext":""},{"type":"submitted","content":"Scientific Reports","date":"2025-04-13T15:40:53+00:00","index":"","fulltext":""}],"status":"published","journal":{"display":true,"email":"[email protected]","identity":"scientific-reports","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":false,"externalIdentity":"scirep","sideBox":"Learn more about [Scientific Reports](http://www.nature.com/srep/)","snPcode":"","submissionUrl":"","title":"Scientific Reports","twitterHandle":"","acdcEnabled":true,"dfaEnabled":true,"editorialSystem":"stoa","reportingPortfolio":"Scientific Reports","inReviewEnabled":true,"inReviewRevisionsEnabled":true}}],"origin":"","ownerIdentity":"14069f3e-a738-44f2-acd4-f3b921622d69","owner":[],"postedDate":"April 24th, 2025","published":true,"recentEditorialEvents":[],"rejectedJournal":[],"revision":"","amendment":"","status":"published-in-journal","subjectAreas":[{"id":47557472,"name":"Earth and environmental sciences/Solid earth sciences/Geology"},{"id":47557473,"name":"Earth and environmental sciences/Solid earth sciences/Petrology"},{"id":47557474,"name":"Earth and environmental sciences/Solid earth sciences/Sedimentology"}],"tags":[],"updatedAt":"2025-07-07T16:05:57+00:00","versionOfRecord":{"articleIdentity":"rs-5860486","link":"https://doi.org/10.1038/s41598-025-05155-1","journal":{"identity":"scientific-reports","isVorOnly":false,"title":"Scientific Reports"},"publishedOn":"2025-07-02 15:58:12","publishedOnDateReadable":"July 2nd, 2025"},"versionCreatedAt":"2025-04-24 15:44:45","video":"","vorDoi":"10.1038/s41598-025-05155-1","vorDoiUrl":"https://doi.org/10.1038/s41598-025-05155-1","workflowStages":[]},"version":"v1","identity":"rs-5860486","journalConfig":"researchsquare"},"__N_SSP":true},"page":"/article/[identity]/[[...version]]","query":{"redirect":"/article/rs-5860486","identity":"rs-5860486","version":["v1"]},"buildId":"8U1c8b4HqxoKbykW_rLl7","isFallback":false,"isExperimentalCompile":false,"dynamicIds":[84888],"gssp":true,"scriptLoader":[]}