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Mar 21, 2018 - H. Liu, Z.-G. Song, W.-J. Zhong, C. Han, M. Han, Q.-X. Du, L.-H. Gao, J.-J. Li, and J.-L. Yan. College of Earth Science and Engineering, ...
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Geochronology, geochemistry, and tectonic implications of Upper Silurian-Lower

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Devonian meta-sedimentary rocks from the Jiangyu Group in eastern Jilin

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Province, NE China

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Zuo-Zhen Hana,b,c*, Hui Liua,b, Zhi-Gang Songa,b, Wen-Jian Zhonga,b, Chao Hana,b, Mei

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Hana,b, Qing-Xiang Dua,b, Li-Hua Gaoa,b, Jing-Jing Lia,b and Jun-Lei Yana,b

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a

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Technology, Qingdao 266590, China

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b

College of Earth Science and Engineering, Shandong University of Science and

Key Laboratory of Depositional Mineralization & Sedimentary Mineral of Shandong

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Province, Shandong University of Science and Technology, Qingdao 266590, China

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c

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Science and Technology, Qingdao 266237, China

Laboratory for Marine Mineral Resources, Qingdao National Laboratory for Marine

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*Corresponding author: Zuo-Zhen Han

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College of Earth Science and Engineering, Shandong University of Science and

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Technology, Qingdao, 266590, China

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E-mail: [email protected]

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Abstract

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In this study, we present detrital zircon U-Pb ages and Hf isotopic data and whole-rock

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geochemical data from meta-sedimentary rocks of the Jiangyu Group in eastern Jilin

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Province (NE China) to constrain the late Silurian-Early Devonian tectonic evolution of

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the

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meta-sedimentary rocks from the Jiangyu Group yielded concordant ages ranging from

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2926 Ma to 415 Ma, and the youngest zircon populations of the two samples yielded

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weighted mean ages of 427±3 Ma and 426±3 Ma, respectively. Combined with

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reliable published muscovite

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metamorphic ophiolitic mélange, these data indicate that the protoliths of the Jiangyu

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Group were deposited during the late Silurian-Early Devonian Era. A comparison of the

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U-Pb ages and Hf isotopic data for detrital zircons from northeastern Gondwana and the

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Jiangyu Group indicates a probable tectonic affinity. The whole-rock geochemical data

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indicate that the protoliths of the meta-sedimentary rocks from the Jiangyu Group were

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graywackes deposited in a continental arc setting. Based on the recognition of the early

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to middle Paleozoic subduction-accretion events along the eastern segment of the

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northern margin of the North China Craton (NCC), we infer that the

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subduction-accretion events may have occurred in the Yanbian area followed by one or

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more arc-continent collisions after the Early Devonian.

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Keywords: Zircon geochronology, Geochemistry, Detrital zircons, Jiangyu Group,

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Xing’an-Mongolia Orogenic Belt

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southeastern

Xing’an-Mongolia

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Orogenic

Belt.

Two

samples

of

the

Ar-39Ar ages of 408 Ma from the overlying

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Introduction

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Orogenic belts feature intense tectonic activities and have long been studied by

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geologists. The Central Asian Orogenic Belt (CAOB) is one of the largest and

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longest-lived Phanerozoic accretionary orogens on Earth, and it has experienced

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multiple complex subduction-collision phases with various structural domains since the

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late Mesoproterozoic (Fig. 1a, Tang 1990; Shao 1991; Sengör and Natal'in 1996; Khain

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et al. 2002; Xiao et al. 2003, 2009; Jahn et al. 2004, Jian et al. 2008; Windley et al. 2007;

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Zhang et al. 2014; Wang et al. 2015a). The Xing’an-Mongolia Orogenic Belt (XMOB,

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i.e., the eastern section of the CAOB) is sandwiched between the Siberian Craton (SC)

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in the north and the North China Craton (NCC) in the south (Fig. 1a). The tectonic

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evolution of northeast (NE) China and adjacent regions located within the eastern

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section of the XMOB was dominated by the assembly of several microcontinental

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blocks (Fig. 1b) and the closure of the Palaeo-Asian ocean during the Palaeozoic to

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early Mesozoic (JBGMR 1988; Li et al. 1999, 2006, 2014; Xu et al. 2003; Wu et al.

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2007; Meng et al. 2010; Cao et al. 2013), with subsequent superimposition of the

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Circum-Pacific and Mongolia Okhotsk tectonic systems during the Mesozoic (Ying et

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al. 2008; Yu et al. 2012; Sun et al. 2013a; Tang et al. 2014).

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The Yanbian area in eastern Jilin Province is located at the junction of NE China, Far

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East Russia and Korea. Tectonically, it is located in the southeastern section of the

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XMOB at the junction of the Khanka-Jiamusi block, the Songnen-Zhangguangcai

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Range (SZR) massif and the NCC (Fig. 1b; Jia et al. 2004). The Yanbian area is

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characterized by large volumes of Phanerozoic granitoids with small amounts of

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Palaeozoic to Mesozoic strata (Fang 1992; JBGMR 1988; Sun et al. 2013b) and the

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existence of three types of flora (Cathaysian flora, Angara flora, mixed

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Cathaysian-Angara flora; Peng et al. 1999). The strata are distributed among the

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Phanerozoic granitoids in the forms of isolated islands, tectonic remnants and variously

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sized xenoliths. The early Palaeozoic tectonic evolution of this area remains

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controversial. Based on the analysis of pre-Mesozoic metamorphic rocks in the

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Yanbian area, Wang (1998) proposed that the strata were deposited on deformed middle

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and upper Proterozoic crust that was then deformed in an orogenic belt during the early

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Palaeozoic. However, according to comparison of stratigraphic, petrological and

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palaeontological data, Jia (1995) and Tang and Zhao (2007) suggested that the Yanbian

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area, which differs from the surrounding massifs, is an allochthonous terrane.

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Furthermore, there are two contrasting viewpoints on the tectonic setting of the Yanbian

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area: passive continental margin (Jia et al. 2004) or active continental margin (Zhao et

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al. 1996; Wang et al. 1997; Wang 1998).

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These different interpretations arise from the paucity of reliable geochronologic and

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geochemical data from the Palaeozoic strata in the Yanbian region. In this paper, we

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present results from zircon U-Pb dating and Hf isotopic analyses as well as whole-rock

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geochemical analyses of meta-sedimentary rocks in the Jiangyu Group at Kaishantun

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town in the southern Yanbian region. These new results offer new evidence to better

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understand the tectonic evolution of the southeastern section of the XMOB.

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Geologic setting and sample descriptions

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The Yanbian area is situated in the southeastern section of the CAOB and is

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sandwiched by the NCC, SZR massif and Khanka-Jiamusi block. These terranes are

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separated by the Gudonghe-Fuerhe-Chongjin fault belt (GFC), the Dunhua-Mishan

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fault belt (DM) and the Wangqing-Hunchun (WH) or Dashanzui-Antu-Kaishantun

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suture belt (DAK) , respectively (Fig. 1b; Zhao et al. 1996; Jia et al. 2004; Sun et al.

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2013b). The Yanbian area was influenced by collisions between microcontinental

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blocks and the NCC in the Palaeo-Asian ocean tectonic domain from the Paleozoic to

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Early Triassic. Subsequently, the region was dominated by tectonic overprinting and

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transformation related to the Circum-Pacific structural domain (Jia et al. 2004; Zhang et

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al. 2004; Xu et al. 2013). Large volumes of Phanerozoic granitoids are widespread in

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this area; however, Palaeozoic and Mesozoic rocks are rare and present as remnants in a

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“sea” of granitoids (JBGMR 1988). The main Palaeozoic stratigraphic units in the

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Yanbian area are distributed to the southwest of Kaishantun town in the southern

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Yanbian area and are surrounded by intrusive Mesozoic granitoids. The strata in this

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area are dominated by widespread upper Palaeozoic units, including the upper

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Carboniferous Shanxiuling Formation, the Carboniferous to Permian Dasuangou

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Formation and Hesheng Formation, and the lower Permian Miaoling Formation, as

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well as Mesozoic and Cenozoic strata. The study area also features widespread

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Mesozoic granitoids, as well as minor ophiolitic mélange and upper Permian

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mafic-ultramafic rocks (Fig. 2; JBGMR 1988, 2000; Tang and Zhao 2007). Outcrops

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are rare, and the terrane in this area is heavily forested. The Jiangyu Group is distributed

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in the west of Jiangyu village to the southwest of Kaishantun town and mainly consists

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of chlorite schist, biotite-plagioclase gneiss, two-mica schist, and magnetite quartzite.

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The samples used in this paper were collected from the Jiangyu Group.

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Sample HC-1 is a biotite-plagioclase gneiss from the Jiangyu Group that was

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collected ~18 km to the southwest of Kaishantun town (GPS location: 42º32'51" N,

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129º42'1" E; Fig. 2), to the south of Yanji City. In addition, we collected seven samples

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(HC-2, 3, 4, 5, 6, 7 and 8) at the same location for whole-rock geochemical analysis

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(Table S2). These charcoal grey rocks feature a medium- to fine-grained

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lepidogranoblastic texture, gneissic structure and little sericitization. The samples are

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composed of plagioclase (~40%), quartz (~39%), biotite (~16%), and muscovite (~5%),

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with minor opaque minerals (Fig. 3a, b and c). Quartz aggregates exhibit a directional

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strip-shaped arrangement. Biotite and muscovite display a continuous directional

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arrangement, and the grains are bent. The plagioclase grains exhibit sericitization, and

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the sericite is thin and flaky. Thus, the samples are mid-grade metamorphic products.

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Sample HC-9 is a two-mica schist from the Jiangyu Group that was collected ~0.9

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km to the southwest of HC-1 (GPS location: 42º32'50" N, 129º41'47" E; Fig. 2). In

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addition, we also collected seven samples (HC-10, 11, 12, 13, 14, 15 and 16) from the

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same location for whole-rock geochemical analysis (Table S2). The samples are grey

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and characterized by a medium- to fine-grained lepidogranoblastic texture, weak

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schistosity and sericitization (Fig. 3d, e and f). The samples contain quartz (~42%),

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muscovite (~22%), plagioclase (~18%), biotite (~16%) and garnet (~2%), with minor

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opaque minerals. Quartz aggregates exhibit a directional strip-shaped arrangement, and

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the plagioclase grains display strong sericitization. Moreover, a small amount of

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plagioclase is completely metasomatised, and the granular crystals of the original

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minerals are preserved. Biotite displays a flaky texture and continuous directional

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arrangement. Additionally, some biotite was partially transformed into muscovite.

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Sericite exhibits a thin and flaky composition. The garnet grains are cracked and

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distributed in star shapes. Thus, the samples are mid-grade metamorphic products.

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Methods

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Zircon U-Pb dating

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The samples were first crushed to 80-100 mesh, and the low-density minerals were

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then removed using conventional heavy-liquid techniques. High-purity zircon samples

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were then separated from the remaining heavy minerals using magnetic separation

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techniques at the Langfang Regional Geological Survey, Hebei Province, China.

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High-quality non-fractured zircon grains were inlaid in epoxy, polished down to half

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their original thickness and washed in an acid bath before analysis. Transmitted light

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and reflected light images were captured using a microscope, and cathodoluminescence

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(CL) images were collected using a JEOL scanning electron microscope at the State

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Key Laboratory of Continental Dynamics, Northwest University, Xi’an, China. Based

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on analysis of the CL images, distinct locations within the zircons were selected as the

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best points for laser ablation inductively coupled plasma mass spectrometer

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(LA-ICP-MS) measurements. An Agilent 7500a ICP-MS equipped with ComPex 102

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ArF excimer laser was used to measure the U-Pb isotope ages of the zircons. Helium

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gas was used as the carrier gas, and a crater diameter of 30 µm and a laser intensity of

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50 J cm-1 were used in all analyses. The standard zircon 91500 was used as the external

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age calibration standard. In addition, the standard material NIST 610 was used as the

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external standard to calculate the trace element concentrations in the zircons, and 29Si

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was used as an internal standard to calibrate the contents of U, Th and Pb in the zircons.

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The detailed instrument operating conditions and data processing methods were

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described by Yuan et al. (2004). Common Pb corrections were performed using the

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method of Anderson (2002). The isotope ratio and element content calculations for

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zircon dating were performed using GLITTER (ver. 4.0), and the age calculations and

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concordia diagrams were generated using Isoplot (Ludwig, 2003). Individual analyses

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of the isotope ratio and age error (standard error) are reported at the 1 sigma level, and

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errors in the weighted mean

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confidence level.

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Major and trace element analyses

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Pb/206Pb ages are reported at the 95% (2 sigma)

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After removal of altered surfaces, whole-rock samples were crushed to ~200 mesh.

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The whole-rock major and trace element compositions of the samples were determined

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at the Supervision and Inspection Center of Mineral Resources, the Ministry of Land

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and Resources of Jinan, China. The contents of SiO2 and Al2O3 were analysed via the

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gravimetric approach based on gelatin coagulation and the xylenol orange method,

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respectively. The concentrations of major oxides (Fe2O3, CaO, MgO, FeO, K2O, Na2O,

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TiO2, MnO, and P2O5) and trace elements, including Ba, Sr, V, and Cr, were measured

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using an IRI-Intrepid plasma spectrometer and the standard GB/T14506-2010 for the

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oxides. The remaining trace elements were determined using an XSeries 2 ICP-MS.

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Zircon Hf isotopic analyses

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Zircon Hf isotope analyses were performed at the State Key Laboratory of

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Continental Dynamics, Northwest University, China, using a Nu Plasma HR

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multicollector (MC) ICP-MS coupled with a Geolas 200M laser ablation system made

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by the German Microlas company. The Hf analyses were performed on the same spots

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as the previous U-Pb isotope analyses, with a spot size of 44 µm and a repetition rate of

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10 Hz. Detailed instrument operating conditions and data processing methods were

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described by Yuan et al. (2008). Isobaric interference corrections for the sample

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Lu/177Hf and

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Lu/175Lu=0.02669 (Biévre and Taylor 1993) and

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2002). During the analyses, instrument monitoring and sample correction were

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performed using the zircon standards 91500 and GJ-1. The

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standard 91500 is 0.282295±0.000029 (n=17, 2σ), which is relatively consistent with

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the recommended value (0.2823075±0.000058, 2σ, Wu et al. 2006). The

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constant of 1.867×10-11 year-1 (Albarède et al. 2006) and the present-day chondritic

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ratios of 176Hf/177Hf = 0.282785 and 176Lu/177Hf = 0.0336 were adopted to calculate the

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ƐHf(t) values (Bouvier et al. 2006). Single-stage model ages (TDM1) were calculated

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based on a depleted mantle with a present-day

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176

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calculated using an assumed 176Lu/177Hf ratio of 0.01544 for average continental crust

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(Rudnick and Gao, 2003).

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Results

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Zircon U-Pb dating

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Hf/177Hf ratios were applied based on the values of 176

Yb/172Yb=0.5886 (Chu et al.

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Hf/177Hf ratio of zircon

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Lu decay

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Hf/177Hf ratio of 0.28325 and an

Lu/177Hf ratio of 0.0384 (Vervoort et al. 1999). Two-stage model ages (TDM2) were

Most zircon grains from sample HC-1 are euhedral to subhedral in the CL images,

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and some display oscillatory zoned cores with homogeneous rims that are too narrow to

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be analyzed, suggesting that these grains may have experienced a late metamorphic

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event (Fig. 4a; Wang et al 2014). The Th/U ratios are between 0.11 and 1.28 (excluding

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one analysis, HC-1-76, with a Th/U ratio of 0.03), indicating a magmatic origin

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(Koschek 1993). Some zircon grains are rounded to subrounded, and some contain

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inherited core-rim textures in the CL images (Fig. 4a). A total of one hundred and one

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analyses were performed on one hundred grains, and the results are presented in Table

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S1. Apart from seven analyses (HC-1-01, 42, 59, 79, 88, 90 and 99), the other

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ninety-four U-Pb analyses were less than 10% discordant and yielded ages of 418±6 to

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2658±12 Ma (Fig. 5a) that can be divided into three age populations: a main age

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population of 418-494 Ma (n=61, with one peak value at 454 Ma and two weak peaks at

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428 and 473 Ma; Fig. 5b, c) and two secondary age populations of 562-657 Ma (n=10,

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with peak values at 569 and 633 Ma) and 889-1259 Ma (n=13, with peak values at 933

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and 1091 Ma, respectively). Additionally, other individual ages and minor groups

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include 1442, 1587-1616, 1770-1832, 1979, 2288, 2439 and 2658 Ma (n=10; Fig. 5a, c).

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Notably, one grain from the sample HC-1 with a core-rim texture yielded a core age of

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2591±14 Ma (HC-1-42) and a rim age of 562±6 Ma (HC-1-43) (Fig. 4a).

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The majority of grains from sample HC-9 are euhedral to subhedral in the CL

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images and exhibit oscillatory growth zoning and internal core-rim structures (Fig. 4b).

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The Th/U ratios are between 0.12 and 1.54, suggesting a magmatic origin (Koschek

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1993). Some zircons are rounded to subrounded, and some contain inherited core-rim

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textures in the CL images (Fig. 4b). Additionally, some zircons in this sample have thin

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homogenous rims, suggesting they may have experienced a late metamorphic event

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(Wang et al. 2014). Overall, ninety-six analyses were performed on ninety-six grains,

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and the results are presented in Table S1. Apart from four analyses (HC-9-39, 79, 86

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and 93), the other ninety-two U-Pb analyses were less than 10% discordant and yielded

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ages of 415±9 Ma to 2926±28 Ma (Fig. 5d) that can be divided into four age

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populations: a main age population of 415-504 Ma (n=52, with peak values at 428 Ma,

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455 Ma and 478 Ma) and three secondary age populations of 567-649 (n=7, with a peak

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value at 597 Ma), 933-1138 Ma (n=9, with peak values at 943 Ma and 1124 Ma) and

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1607-1866 Ma (n=12, with peak values at 1676 Ma and 1800 Ma). In addition,

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individual and minor group ages of 1225-1529, 2408-2462, 2597, 2636 and 2926 Ma

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were also obtained (n=12; Fig. 5d, f).

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Geochemistry

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Major element compositions

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The metamorphic rocks of the Jiangyu Group have compositions of

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SiO2=64.54-68.20

wt.%,

TiO2=0.63-0.79

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Fe2O3T=5.78-7.07

wt.%,

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K2O+Na2O=4.19-5.15 wt.%, and SiO2/Al2O3=4.20-4.88 (Table S2). The average major

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element contents of the samples are highly consistent with normalized upper

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continental crust (UCC) values, except for their low CaO, Na2O, and K2O contents

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(Rudnick and Gao 2003). However, in comparison with post-Archean average shale

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(PAAS), the samples have low Fe2O3T, TiO2, Al2O3, and K2O contents and high SiO2,

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Na2O, CaO, and MgO contents (Table S2; McLennan et al. 1993).

Na2O=1.58-2.53

wt.%, wt.%,

Al2O3=13.65-15.35

wt.%,

K2O=2.00-3.16

wt.%,

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Trace element compositions

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According to the chondrite-normalized rare earth element (REE) diagram (Fig. 6a;

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Sun and McDonough 1989), these samples are enriched in light REEs (LREEs),

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depleted in heavy REEs (HREEs), and feature ∑LREE/∑HREE ratios of 5.83-8.52.

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Furthermore, the total REE abundances are low (∑REE=139-198 ppm, average=157

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ppm). These patterns are generally similar to those of the UCC and PAAS, although the

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sample patterns differ somewhat from the UCC patterns in terms of HREEs (Fig. 6a).

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The REE patterns are moderately fractionated, with (La/Yb)N ratios that vary from 5.60

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to 8.97 (average=6.92) and weakly negative Eu anomalies of 0.61-0.81 (average=0.69,

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Fig. 6a; Table S2). On the UCC-normalized variation diagram, these rocks are depleted

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in large ion lithophile elements (LILEs; e.g., Rb, Sr, and Ba) and enriched in high field

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strength elements (HFSEs; e.g., Ta, Y, and U) and Pb (Fig. 6b; Rudnick and Gao 2003).

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Furthermore, the LILE and HFSE contents of PAAS are mostly higher than those of the

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studied samples; in contrast, the Dy, Er, Yb, and Lu contents of PAAS are lower than

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those of the Jiangyu Group samples (Fig. 6b; Table S2). Additionally, the samples have

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high Cr (247.6-382.7) and Co (13.03-20.25) concentrations.

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Zircon Hf isotopes

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Some of the zircon grains analysed for U-Pb dating were also analysed via in situ Hf

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isotopic analysis. The results are shown in Fig. 7a-b and are listed in Supplementary

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Table 3.

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A total of 44 detrital zircons from sample HC-1 were chosen for Hf isotopic

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composition analysis. One Archean (2658 Ma) zircon yielded a negative ƐHf(t) value of

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-6.99 and TDM2 age of 3558 Ma. Three zircons with Palaeoproterozoic U-Pb ages (2439

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to 1832 Ma) yielded negative ƐHf(t) values from -10.07 to -4.08 and TDM2 ages of

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3358-2852 Ma; the remaining zircons yielded positive ƐHf(t) values between 1.90 to

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9.84 and corresponding TDM2 ages of 2320-1869 Ma. Most of the Mesoproterozoic

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detrital zircons yielded positive values of 0.61 to 9.92 and TDM2 ages of 2256-1315 Ma;

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the remaining two Mesoproterozoic zircons yielded negative ƐHf(t) values of -3.60 and

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-8.35 and corresponding TDM2 ages of 2403 and 2439 Ma, respectively. The

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Neoproterozoic zircons yielded positive ƐHf(t) values ranging from 0.11 to 10.85 and

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TDM2 ages of 1498-1093 Ma, barring one zircon (934 Ma) with a negative ƐHf(t) value

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of -1.14 and a TDM2 age of 1853 Ma. The majority of detrital zircons in the 487-420 Ma

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population yielded positive ƐHf(t) values from 2.39 to 13.56, with TDM2 ages of

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1240-540 Ma; the remaining early Palaeozoic zircons in this group yielded negative

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ƐHf(t) values from -7.29 to -0.05, with TDM2 ages of 1870-1393 Ma.

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A total of 45 detrital zircons from sample HC-9 were chosen for Hf isotopic analysis.

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Two Archean (2636 and 2597 Ma) zircon grains yielded positive ƐHf(t) values of 1.75

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and 4.91, with TDM2 ages of 3012 and 2789 Ma, respectively. Most of the

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Palaeoproterozoic zircon grains yielded positive ƐHf(t) values between 1.35 and 10.11,

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with TDM2 ages of 2342-1870 Ma; the secondary Palaeoproterozoic zircon grain

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population yielded negative ƐHf(t) values of -5.01 to -2.95, with corresponding TDM2

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ages of 3134-2767 Ma. Detrital zircons with concordant ages of 1529 to 933 Ma

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yielded positive ƐHf(t) values from 1.13 to 9.43 and TDM2 ages of 2178-1466 Ma,

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barring one grain with a ƐHf(t) value of -0.13 and a TDM2 age of 1790 Ma. All detrital

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zircons with concordant ages of 649-567 Ma yielded positive ƐHf(t) values between

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1.71 and 6.70 and TDM2 ages of 1452-1072 Ma. The majority of the detrital zircons in

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the 504-415 Ma age population yielded positive ƐHf(t) values of 0.67 to 10.57, with

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TDM2 ages of 1378-735 Ma; the remaining Phanerozoic detrital grains yielded negative

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ƐHf(t) values from -18.95 to -3.55 and TDM2 ages of 2613-1656 Ma.

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Discussion

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Protolith reconstruction

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The study area experienced intensive erosion and various degrees of deformation

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and metamorphism during late tectonic and/or magmatic events (Jia et al. 2004).

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Consequently, fluid-mobile elements in the rocks may have experienced various

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degrees of reallocation during metamorphism. However, considerable information

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related to the nature of the protoliths and tectonic setting can be obtained from the

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concentrations and ratios of these relatively immobile elements relative to those of

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fluid-mobile elements (Shaw 1972; Bhatia 1983; Bhatia and Crook 1986). Hence, we

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primarily use immobile elements to determine the nature of the protoliths and tectonic

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setting using other elements as a reference.

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The discriminant function (DF) (Shaw 1972), TiO2-SiO2 diagram (Tarrey et al.

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1976), Niggli parameter diagram (Simonen 1953), and log(Na2O/K2O)-log(SiO2/Al2O3)

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diagram (Pettijohn et al. 1987) methods were used to reconstruct the protoliths. All DF

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values for the studied samples were negative (ranging from -3.83 to -2.13), indicating

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probable sedimentary parentage. This conclusion is supported by the TiO2-SiO2

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discrimination diagram (Fig. 8a). In the Niggli parameter discrimination diagram, the

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samples plot in the sedimentary rock domain (Fig. 8b), suggesting that these samples

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are sedimentary in origin. The log(Na2O/K2O)-log(SiO2/Al2O3) diagram developed by

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Pettijohn et al. (1987) demonstrates that these samples were derived from graywacke

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(Fig. 8c).

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The depositional age of the Jiangyu Group

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Since it is hard to directly obtain the ages of rocks based on the lithostratigraphic

315

or biostratigraphic relationships with other strata in this region, the protolith

316

depositional age of the Jingyu Group cannot be corroborated by other datasets. Notably,

317

the

318

Permo-Carboniferous in age (JBGMR 1988, 2000; Tang and Zhao 2007). It is generally

319

accepted that the maximum age of deposition may be older than the actual time of

320

sedimentary deposition based on the ages of the youngest zircon or zircons (Nelson

321

2001; Fedo 2003; Dickinson and Gehrels 2009; Gehrels 2014). The reliable youngest

322

age approach is based on the youngest concordant zircon U-Pb age, the youngest peak

323

age or the mean age of the youngest zircons (n≥2) with ages overlapping at 1 sigma

324

(YC1σ(2+)) (Dickinson and Gehrels 2009). Here, we opt to use the YC1σ(2+) approach

325

as a reliable estimate of the maximum depositional age of the Jiangyu Group to reduce

326

the impact of later tectonothermal events and the uncertainty related to the analysis of

327

detrital zircons. Our new zircon U-Pb dating results for the detrital grains from HC-1

328

show that the youngest zircon population (ca. 438-418 Ma) yields a weighted mean age

329

of 426±3 Ma (MSWD=1.10, n=18; Fig. 5b), suggesting that the protolith of the

330

biotite-plagioclase gneiss was not deposited prior to 426 Ma. Furthermore, concordant

group

has

previously

been

considered

Precambrian,

Cambrian

or

Page 16 of 62

331

detrital grains from sample HC-9 produced results that are essentially in agreement

332

with HC-1. The youngest zircon population (ca. 436-415 Ma) from sample HC-9 yields

333

a weighted mean age of 427±3 Ma (MSWD=0.91, n=15; Fig. 5e), suggesting that the

334

protolith of the two-mica schist was deposited after ca. 427 Ma. Consequently, the

335

detrital zircon results show that the protoliths of the Jingyu Group were deposited no

336

earlier than the late Silurian. Based on the published reliable muscovite 40Ar-39Ar age of

337

408 Ma from the overlying metamorphic ophiolitic mélange (Tang and Zhao 2007), the

338

Jiangyu Group likely formed before 408 Ma. We conclude, therefore, that the protoliths

339

of the group were deposited during the late Silurian-early Devonian and not during the

340

Precambrian, Cambrian or Permo-Carboniferous, as previously claimed.

341

Sedimentary provenance of the Jiangyu Group and its tectonic affinity

342

Zircon is characterized by its high weathering resistance and a high U-Pb closure

343

temperature; thus, zircon grains feature a U-Pb isotopic system that remains stable

344

throughout various geological processes (Bruguier et al. 1997; Cherniak and Watson

345

2000). Therefore, it is generally accepted that the age spectra of detrital zircons from

346

sedimentary rocks can retain information regarding the depositional provenance and

347

can be used to reconstruct the tectonic evolution of ancient basins and orogenic belts

348

(Carter and Steve 1999; Fedo et al. 2003; Rojas-Agramonte et al. 2011; Wang et al.

349

2016).

350

In total, 186 of the 197 analyses of the two samples yield concordant ages (less than

351

±10% discordant) ranging from 2926 Ma to 415 Ma, with prominent age peaks at 428,

352

455, 476, 564, 622, 935, 1124, 1676 and 1816 Ma and minor peaks at 889, 1529-1313,

Page 17 of 62

353

1979, 2288, 2649-2423 and 2926 Ma (Fig. 9d).

354

In the Jiangyu Group, most detrital zircons produced concordant ages ranging

355

from 504 to 415 Ma, with peaks at 476, 455 and 428 Ma. These data are comparable

356

with the ages of lower Palaeozoic igneous rocks in the SZR massif, the Jiamusi massif

357

(Liu et al. 2008; Wang et al. 2012a), central Jilin Province (Pei et al. 2015) and central

358

Inner Mongolia (Jian et al. 2008; Guo et al. 2009; Zhang et al. 2014). Additionally,

359

these data are concordant with the early Palaeozoic detrital zircon ages reported from

360

the lower Permian Hesheng Formation (Sun et al. 2013b) and the upper Permian

361

Dasuangou and Miaoling formations (Zhou et al. 2017) in this area. Furthermore,

362

similar detrital zircon or inherited zircon ages are common in the sedimentary and

363

igneous rocks in other parts of the eastern margin of the XMOB (Wilde et al. 2003;

364

Gladkochub 2008; Meng et al. 2010; Zhou et al. 2010a; Wang et al. 2012a, 2012b, 2014,

365

2015b; Pei et al. 2015). Moreover, the Hf isotopic compositions (ƐHf(t) values of -3.55

366

to 13.56, with TDM2 ages of 1656 to 540 Ma) of the majority of early Palaeozoic detrital

367

zircons are analogous to those of coeval grains from the eastern XMOB (Guo et al.

368

2009; Wang et al. 2012b, 2015a; Pei et al. 2014;2015), suggesting that these detrital

369

zircons may have originated from juvenile crust within the eastern XMOB. Therefore,

370

the early Palaeozoic detrital zircons of the Jiangyu Group may have been

371

predominantly sourced from the eastern XMOB.

372

In the Jiangyu Group, detrital grains with ages of 562-657 Ma and 889-1268 Ma

373

reveal that the provenance of these rocks included considerable proportions of upper

374

Mesoproterozoic and Neoproterozoic magmatic rocks. Zircons with ages of 562-657

Page 18 of 62

375

Ma are rare in the metamorphic rocks of the eastern XMOB (Fig. 9a; Wilde et al. 2000,

376

2003; Zhou et al. 2010a, 2010b). However, the detrital or inherited zircon age group of

377

ca. 800 Ma, which is common in the Palaeozoic terranes and older rock groups in the

378

microcontinents of the eastern XMOB (Fig. 9a; Stern 2008; Zhou et al. 2012; Wang et

379

al. 2014), is absent in the Jiangyu Group, and late Mesoproterozoic magmatism

380

(1268-1000 Ma) has not been reported in the eastern XMOB (Meng et al. 2010; Li et al.

381

2011a; Wu et al. 2011; Wang et al. 2014). The NCC also does not record evidence of

382

late Meso-Neoproterozoic magmatism (Fig. 9b; Cope et al. 2005; Li et al. 2009; Zhao

383

and Guo, 2012b). Therefore, these microcontinents and the NCC are not considered

384

potential source areas for the late Meso-Neoproterozoic detrital zircons of the Jiangyu

385

Group. However, detrital zircon populations from ca. 650-550 Ma and ca. 1200-900 Ma

386

accounted for high proportions of the lower to middle Cambrian clastic strata in

387

terranes located along the northeastern margin of Gondwana during the early

388

Palaeozoic (Fig. 9c; Li et al. 2001; Squire et al. 2006; Wang et al. 2016), e.g., Australia

389

(Ireland and Bowring 1998), Antarctica (Goodge et al. 2004), New Zealand (Richard

390

Jongens et al. 2003), and northern India (Myrow et al. 2003). These late

391

Meso-Neoproterozoic detrital grains from the Jiangyu Group are primarily euhedral to

392

subhedral, indicating that they likely experienced only short-distance transport in the

393

sedimentary regime. Therefore, these zircons were potentially derived from a local

394

source, suggesting that a Precambrian crystalline basement may have existed in the

395

southern Yanbian region and may have supplied material to the Jiangyu Group. In

396

addition, these late Meso-Neoproterozoic detrital zircons yield ƐHf(t) values ranging

Page 19 of 62

397

from -8.35 to +10.85 and TDM2 ages of 2439 to 1093 Ma and consequently resemble

398

zircons from northeastern Gondwana (Fig. 7a, b; Kemp et al. 2006; Ravikant et al. 2011;

399

Wang et al. 2016). Furthermore, the fossil assemblages of the upper Carboniferous

400

Shanxiuling Formation and lower Permian Miaoling Formation in this area resemble

401

those of the Gondwanan and Tethyan tectonic domains but not those from the adjacent

402

domains (Jia 1995). Therefore, we suggest that the late Meso-Neoproterozoic detrital

403

zircons of the Jiangyu Group were likely sourced from a ‘missing’ local Precambrian

404

basement with a tectonic affinity to northeastern Gondwana.

405

In the Jiangyu Group, the detrital zircons with ages of 1607-1979 Ma and

406

2288-2926 Ma reveal that Mesoarchaean and Palaeoproterozoic magmatic rocks were a

407

source of sediment. These two groups, which are related to magmatic-thermal events,

408

are widespread in the SC, Tarim Craton (TC), and NCC (Zhai et al. 2005; Rosen et al.

409

2006; Sal’nikova et al. 2007; Lu et al. 2008; Li et al. 2009; Long et al. 2010; Meng et al.

410

2010; Zhu et al. 2011; Zhao et al. 2012a; Liu et al. 2013) and are also present in the

411

form of detrital zircons or inherited or magmatic zircons within magmatic rocks in

412

Palaeozoic metamorphic complexes and strata in NE China (Miao et al. 2007; Pei et al.

413

2007; Chen et al. 2009; Li et al. 2005; 2010). Additionally, zircons of similar age were

414

observed as igneous and detrital zircons in regions that formerly comprised

415

northeastern Gondwana (Condie et al. 2009; Rojas-Agramonte et al. 2011). However,

416

despite the similarity of the age associations (~2500 Ma and ~1800 Ma) to those in the

417

TC and SC, we suggest that these ancient zircon-bearing sediments of the Jiangyu

418

Group were most likely not sourced from these cratons based on the location of the

Page 20 of 62

419

study area in the southeastern XMOB and far from these cratons (Fig. 1a). In addition,

420

these Palaeoproterozoic and Archean detrital zircons are predominantly euhedral to

421

subhedral (Fig. 4a, b), indicating that they experienced relatively minimal transport

422

prior to deposition. Therefore, these zircons might have been sourced from the missing

423

local Precambrian basement with a tectonic affinity to northeastern Gondwana or the

424

eastern XMOB. In contrast, the remaining zircons are rounded to subrounded,

425

indicating that they experienced long-distance transport before deposition. This

426

observation suggests that these zircons might have been sourced from the NCC.

427

In conclusion, the Palaeozoic detrital zircons of the Jiangyu Group were sourced

428

predominantly from the eastern XMOB. The Meso-Neoproterozoic detrital grains of

429

the group were like sourced from a missing local Precambrian basement with a tectonic

430

affinity to northeastern Gondwana. Similarly, the Palaeoproterozoic and Archean

431

detrital grains of the group were potentially sourced from the same missing local

432

Precambrian basement or from the eastern XMOB and to a lesser degree from the NCC.

433

Depositional setting

434

The protoliths of meta-sedimentary rocks in different tectonic environments have

435

different geochemical characteristics, and these characteristics can be used to determine

436

the sedimentary tectonic setting (Bhatia 1983). Based on the tectonic setting

437

discrimination diagrams for clastic rocks proposed by Roser and Korsch (1986), the

438

tectonic setting can be divided into passive continental margin (PM), active continental

439

margin (ACM) and oceanic island arc (OIA). In the K2O/Na2O-SiO2 discrimination

440

diagram (Fig. 10a), all the samples from the Jiangyu Group plot in the ACM domain.

Page 21 of 62

441

Similarly, these results are supported by the SiO2/Al2O3-K2O/Na2O tectonic diagram

442

(Fig. 10b; Maynard et al. 1982).

443

Furthermore, Bhatia and Crook (1986) demonstrated that immobile trace elements

444

in meta-sedimentary rocks can be used to discriminate among various tectonic settings.

445

In the La-Th-Sc diagram (Fig. 11a), all samples from the Jiangyu Group plot in the

446

continental island arc (CIA) domain. Moreover, the same results are obtained from the

447

Th-Sc-Zr/10 and Ti/Zr-La/Sc discrimination diagrams (Fig. 11b, c). An ‘island’ arc is

448

typically defined as a magmatic arc that has formed in the ocean, forming islands, via

449

oceanic-oceanic subduction; however, an arc that has formed in continental crust via

450

the subduction of oceanic crust beneath a continent is in nature a continental arc,

451

regardless of whether it has been rifted away from the continent via back-arc extension.

452

In this study, all the samples from the Jiangyu Group exhibit typical continental arc

453

geochemical signatures instead of island arc signatures. Therefore, the protolith of

454

these meta-sedimentary rocks was deposited in a continental arc setting. These results

455

are supported by the comparison of the average REE values from the Jiangyu Group

456

samples and those from various tectonic settings (Table 1; Bhatia 1985). The

457

remarkable similarities in the average REE values between the Jiangyu Group samples

458

and the CIA setting suggest that the protoliths of the Jiangyu Group were deposited in a

459

continental arc setting.

460

In summary, the characteristics of the meta-sedimentary Jiangyu Group are

461

consistent, in terms of both major elements and trace elements, with rocks formed in a

462

continental arc tectonic setting related to an ACM. Based on these data and the results

Page 22 of 62

463

of the sedimentary provenance analysis, the Jiangyu Group may represent a continental

464

arc terrane with a tectonic affinity to northeastern Gondwana.

465

Tectonic implications

466

The results presented here indicate that an upper Silurian-Lower Devonian terrane is

467

present in the southern Yanbian area. The precise geochronological data from detrital

468

zircons from the Jiangyu Group have constrained the sedimentary provenance of the

469

meta-sedimentary rocks and have provided us with a new understanding of the

470

Palaeozoic tectonic evolution of the southeastern section of the XMOB.

471

Based on the comparisons of the detrital zircon U-Pb ages and Hf isotopic data

472

between northeastern Gondwana and the Jiangyu Group (Fig. 9a, b; Kemp et al. 2006;

473

Ravikant et al. 2011; Wang et al. 2016), we propose that the Jiangyu continental arc

474

terrane is an allochthon that originated in northeastern Gondwana, similar to the

475

Khanka-Jiamusi block (Wilde et al. 2000; Yang et al. 2014). This hypothesis is

476

supported by the findings of Jia (1995) based on comparisons of palaeomagnetic data

477

and fossil assemblages between the upper Carboniferous Shanxiuling Formation and

478

lower Permian Miaoling Formation in the Yanbian region and adjacent areas.

479

Unfortunately, due to the absence of accurate palaeomagnetic data for the Jiangyu

480

continental arc terrane, the exact location of the Jiangyu block with respect to

481

northeastern Gondwana is difficult to determine. However, based on the existence of

482

the detrital zircon ages of 562-657 Ma (with peaks at 564 and 622; Fig. 9d) and

483

palaeogeographic reconstructions (Li et al. 2001), we suggest that the Jiangyu

484

continental arc terrane rifted from the margin of northeastern Gondwana after 564 Ma

Page 23 of 62

485

and drifted to the northern NCC (Fig.12). Additionally, age information on the late

486

Pan-African events is widely recorded in the eastern XMOB, as supported by previous

487

research (Wilde et al. 2000, 2010; Zhou et al. 2010b, 2011, 2012; Yang et al. 2014;

488

2017). However, evidence of Pan-African events is not present in the Jiangyu Group,

489

indicating that the Jiangyu continental arc terrane may have been part of the

490

structural fabric of the southeastern section of the XMOB since the Early Ordovician

491

(at approximately 476 Ma; Fig.12).

492

Previous studies have shown that an accretion zone related to multiple arc-continent

493

collisions existed along the eastern segment of the northern margin of the NCC in the

494

Early to Middle Paleozoic (Fig.13; Jiang et al. 2014; Zhang et al. 2014; Pei et al. 2015;

495

Wang et al. 2016; Han et al. 2018). This subduction-accretion process may have

496

extended eastward to the Yanbian area and continued through the Early Devonian based

497

on the continental arc depositional setting of the meta-sedimentary rocks in the upper

498

Silurian-Lower Devonian Jiangyu Group. Therefore, based on the presence of

499

meta-ophiolites with two different ages within the upper Carboniferous Shanxiuling

500

Formation overlying the Jiangyu Group (Shao and Tang 1995), an early Palaeozoic

501

accretion zone may have existed in the Yanbian area, and an arc-continent collision

502

may have occurred after the Early Devonian.

503

Conclusions

504

1. The protoliths of the Jiangyu Group meta-sedimentary rocks were deposited

505

during the late Silurian-early Devonian and not during the Precambrian, Cambrian or

506

Permo-Carboniferous, as previously suggested. Additionally, the protoliths of the

Page 24 of 62

507

meta-sedimentary rocks from the Jiangyu Group were graywackes.

508

2. The U-Pb and Hf isotopic results for detrital zircons from the Jiagyu Group

509

suggest that the protolith sediments of the meta-sedimentary units were mainly sourced

510

from juvenile crust in the eastern XMOB, with minor ancient clastic material possibly

511

derived from Precambrian rocks with a tectonic affinity to northeastern Gondwana, the

512

NCC or the eastern XMOB.

513

3. The Jiangyu terrane is an allochthon that originated in northeastern Gondwana,

514

and it has participated in the tectonic evolution of the eastern XMOB since the Early

515

Ordovician (approximately 476 Ma).

516

4. The meta-sedimentary rocks of the upper Silurian-Lower Devonian Jiangyu

517

Group were deposited in a continental arc setting. An early Palaeozoic accretion zone

518

may have existed in the Yanbian area and may have continued until the Early Devonian,

519

and an arc-continent collision may have occurred after the Early Devonian.

520 521

Acknowledgements

522

We thank the staff of the State Key Laboratory of Continental Dynamics, Northwest

523

University, Xi’an, China, for their advice and assistance during the zircon U-Pb and Hf

524

isotopic analyses. We appreciate the Supervision and Inspection Center of Mineral

525

Resources, the Ministry of Land and Resources of Jinan, China, for their assistance

526

with the major and trace element analysis. This work was financially supported by the

527

National Natural Science Foundation of China (grant no. 41372108 and 41602110),

528

Taishan Scholar Talent Team Support Plan for Advanced & Unique Discipline Areas),

Page 25 of 62

529

Major Scientific and Technological Innovation Projects of Shandong Province (grants

530

no. 2017CXGC1602 and 2017CXGC1603) and the SDUST Research Fund (grant no.

531

2015TDJH101).

532 533

References

534

AlbarÉde, F., Scherer, E.E., Blichert-Toft, J., Rosing, M., Simionovici, A., and Bizz-

535

arro, M. 2006. γ- ray irradiation in the early Solar System and the conundrum of the

536

176 Lu decay constant. Geochimica Et Cosmochimica Acta, 70: 1261-1270.

537

doi:10.1016/j.gca.2005.09.027.

538 539 540

Andersen, T. 2002. Correction of common lead in U-Pb analyses that do not report 204 Pb. Chemical Geology, 192: 59-79. doi:10.1016/S0009-2541(02)00195-X. BiÉvre, P.D., and Taylor, P.D.P. 1993. Table of the isotopic compositions of the elem-

541

ent☆. International Journal of Mass Spectrometry & Ion Processes, 123: 149-166.

542

doi:10.1016/0168-1176(93)87009-H.

543 544

Bhatia, M.R. 1983. Plate tectonics and geochemical composition of sandstones. The Journal of Geology, 91: 611-627. doi:10.1086/628922.

545

Bhatia, M.R. 1985. Rare Earth Element geochemistry of Australian Paleozoic gray-

546

wacks and mudrocks: provenance and tectonic control. Sedimentary Geology, 45:

547

97-113. doi:10.1016/0037-0738(85)90025-9.

548

Bhatia, M.R., and Crook, k.a.w. 1986. Trace element characteristics of graywackes and

549

tectonic setting discrimination of sedimentary basins. Contributions to Miner -

550

alogy and Petrology, 92: 181-193. doi:10.1007/BF00375292.

Page 26 of 62

551

Bruguier, O., Lancelet, J.R., and Malavieille, J. 1997. U-Pb dating on single detrital

552

zircon grains from the Triassic Songpan-Ganze flysch (Central China): provenanc-

553

e and tectonic correlations. Earth and Planetary Science Letters, 152: 217-231. doi:

554

10.1016/S0012-821X(97)00138-6.

555

Bouvier, A., Vervoort, J.D., and Patchett, P.J. 2008. The Lu-Hf and Sm-Nd isotopic

556

composition of CHUR: Constraints from unequilibrated chondrites and implica -

557

tions for the bulk composition of terrestrial planets. Earth and Planetary Science

558

Letters, 273: 48-57. doi:10.1016/j.epsl.2008.06.010.

559

Cao, H.H., Xu, W.L., Pei, F.P., Wang, Z.W., Wang, F., and Wang, Z.J. 2013. Zircon

560

U-Pb geochronology and petrogenesis of the Late Paleozoic-Early Mesozoic intr-

561

usive rocks in the eastern segment of the northern margin of the north China Block.

562

Lithos, 170-171: 191-207. doi:10.1016/j.lithos.2013.03.006.

563

Carter, A., and Steve, J.M. 1999. Combined detrital-zircon fission-track and U-Pb

564

dating: a new approach to understanding hinterland evolution. Geology, 27: 235-

565

238. doi:10.1130/0091-7613(1999)0272.3.CO;2.

566

Chen, B., Jahn, B.M., and Tian, W. 2009. Evolution of the Solonker suture zone:

567

Constraints from zircon U-Pb ages, Hf isotopic ratios and whole-rock Nd-Sr

568

isotope compositions of subduction- and collision-related magmas and forearc

569

sediments. Journal of Asian Earth Sciences, 34: 245-257. doi:10.1016/j.jseaes.

570

2008.05.007.

571 572 573

Cherniak, D.J., and Watson, E.B. 2000. Pb diffusion in zircon. Chemical Geology, 172: 5-24. doi:10.1016/S0009-2541(00)00233-3. Chu, N.C., Taylor, R.N., Chavagnac, V., Nesbitt, R.W., Boella, R. M., and Milton, J.A.

Page 27 of 62

574

2002. Hf isotope ratio analysis using multi-collector inductively coupled plasma

575

mass spectrometry: an evaluation of isobaric interference corrections. Journal of

576

Analytical Atomic Spectrometry, 17: 1567-1574. doi:10.1039/b206707b.

577

Cope, T, Ritts, B.D., Darby, B.J., Fildani, A., and Graham, S.A. 2005. Late Paleozoic

578

Sedimentation on the Northern Margin of the North China Block: Implications for

579

Regional Tectonics and Climate Change. International Geology Review, 47:

580

270-296. doi:10.2747/0020-6814.47.3.270.

581

Condie, K.C., Belousova, E., Griffin, W.L., and Sircombe, K.N. 2009. Granitoid even-

582

ts in space and time: Constraints from igneous and detrital zircon age spectra.

583

Gondwana Research, 15: 228-242. doi:10.1016/j.gr.2008.06.001.

584

Dickinson, W.R., and Gehrels, G.E. 2009. Use of U-Pb ages of detrital zircons to infer

585

maximum depositional ages of strata: a test against a Colorado Plateau Mesozoic

586

database. Earth and Planetary Science Letters, 288: 115-125. doi:10.1016/j.epsl.

587

2009.09.013.

588

Fang, W.C. 1992. The Granitoids and their Mineralizations in Jilin Province.

589

Changchun: Jilin Publishing House of Science and Technology, 271 pp (in

590

Chinese).

591 592

Fedo, C.M. 2003. Detrital Zircon Analysis of the Sedimentary Record. Reviews in Mineralogy and Geochemistry, 53: 277-303. doi:10.2113/0530277.

593

Gehrels, G. 2014. Detrital Zircon U-Pb geochronology applied to tectonics. Annual

594

Review of Earth & Planetary Sciences, 42(1):127-149. doi:10.1146/annurev-earth-

595

050212-124012.

Page 28 of 62

596

Gladkochub, D.P., Donskaya, T.V., Wingate, M.T.D., Poller, U., Kröner, A., Fedorovs-

597

ky, V.S., Mazukabzov, A.M., Todt, W., and Pisarevsky, T.S. 2008. Petrology,

598

geochronology, and tectonic implications of c. 500 Ma metamorphic and igneous

599

rocks along the northern margin of the Central Asian Orogen (Olkhon terrane, Lake

600

Baikal, Siberia). Journal of the Geological Society, 165: 235-246. doi:10.-

601

1144/0016-76492006-125.

602

Goodge, J.W., Williams, I.S., and Myrow, P. 2004. Provenance of Neoproterozoic and

603

lower Paleozoic siliciclastic rocks of the central Ross orogen, Antarctica: Detrital

604

record of rift-, passive-, and active-margin sedimentation. Geological Society of

605

America Bulletin, 116: 1253- 1279. doi:10.1130/B25347.1.

606

Guo, F., Fan, W.M., Li, C.W., Miao, L.C., and Liang, Z. 2009. Early Paleozoic

607

subduction of the Paleo-Asian Ocean: Geochronological and geochemical evidence

608

from the Dashizhai basalts, Inner Mongolia. Science China Earth Sciences, 52:

609

940-951. doi:10.1007/s11430-009-0083-2.

610

Guo, X.D., Zhou, J.B., and Zhang, X.Z. 2011. The detrital zircon LA-ICP-MS U-Pb

611

ages and its significance of Benbatu Formation in Xiwuzhumuqinqi, Inner Mong

612

-olia, China. Geological Bulletin of China, 30: 278-290 (in Chinese with English

613

abstracts).

614

Han, Z.Z., Song, Z.G., Han, C., Zhong, W.J., Han, M., Yan, J.L., Liu, H., Du, Q.X., Gao,

615

L.H., and Li., J.J. 2018. U-Pb ages and Hf isotopic composition of zircons and

616

whole rock geochemistry of volcanic rocks from the Fangniugou area: Implications

617

for early-middle Paleozoic tectonic evolution in Jilin Province, NE China. Journal

Page 29 of 62

618

of Mineralogical and Petrological Sciences, 113: 10-23. doi:10. 2465/jmps.170708

619

Ireland, T.R., Flöttmann, T., Fanning, C.M., Gibson, G.M., and Preiss, W.V. 1998.

620

Development of the early Paleozoic Pacific margin of Gondwana from detrital-

621

zircon ages across the Delamerian orogen. Geology, 26: 243-246. doi:10.1130/

622

0091-7613(1998)0262.3.CO;2.

623

Jahn, B.M. 2004. The Central Asian Orogenic Belt and growth of the continental crust

624

in the Phanerozoic. Geological Society London Special Publications, 226: 73-100.

625

doi:10.1144/GSL.SP.2004.226.01.05.

626

JBGMR (Jilin Bureau of Geology and Mineral Resources). 1988. Regional Geology of

627

Jilin Province. Beijing: Geological publishing House 698 pp (In Chinese with

628

English abstracts).

629 630 631 632

JBGMR (Jilin Bureau of Geology and Mineral Resources). 2000. Geological Map of Zhixin town. Regional Geological Survey Report(1:50000)(in Chinese). Jia, D.C.1995. A preliminary study on the geologic features of the Yanji terrain and its structura evolution. Jilin Geology, 14: 40-44 (in Chinese with English abstracts).

633

Jia, D.C., and Guo, L. 1995. The Paleozoic granitic rocks evolutionary stages in the

634

northern part of Jilin Province and their tectonic setting. Jilin Geology, 14: 64-70 (in

635

Chinese with English abstracts).

636

Jia, D., Hu, R., Yan, L., and Qiu, X. 2004. Collision belt between the Khanka block and

637

the North China block in the Yanbian Region, Northeast China. Journal of Asian

638

Earth Sciences, 23: 211-219. doi:10.1016/S1367-9120(03)00123-8.

639

Jian, P., Liu, D., Kröner, A., Windley, B.F., Shi, Y., Zhang, F., Shi, G.H., Miao, L.C.,

Page 30 of 62

640

Zhang, W., Zhang, Q., Zhang, L.Q., and Ren, J.S. 2008. Time scale of an early to

641

mid-Paleozoic orogenic cycle of the long-lived Central Asian Orogenic Belt, Inner

642

Mongolia of China: Implications for continental growth. Lithos, 101: 233-259. doi:

643

10.1016/j.lithos.2007.07.005.

644

Jiang, Z.L., Qiu, H.J., Peng, Y.J., Zhang, W.M. and Liang, S. 2014. Zircon SHRIMP

645

U-Pb dating for island arc volcanic rocks of Fangniugou area in Yitong region of

646

Jilin Province. Journal of Central South University, 21: 2877-2884.

647

Kemp, A.I.S., Hawkesworth, C.J., Paterson, B.A., and Kinny, P. 2006. Episodic growth

648

of the Gondwana Supercontinent from hafnium and oxygen isotopes in zircon.

649

Nature, 439: 580-583. doi:10.1038/nature04505.

650

Khain, E.V., Bibikova, E.V., Kröner, A., Zhuravlev, D.Z., Sklyarov, E.V., Fedotova,

651

A.A., and Kravchenko-Berezhnoy, I.R. 2002. The most ancient ophiolite of the

652

Central Asian fold belt: U-Pb and Pb-Pb zircon ages for the Dunzhugur Complex,

653

Eastern Sayan,Siberia, and geodynamic implications. Earth and Planetary Science

654

Letters, 199: 311-325. doi:10.1016/S0012-821X(02)00587-3.

655

Koschek, G. 1993. Origin and significance of the sem cathodoluminescence from zir-

656

con. Journal of Microscopy, 171: 223-232. doi:10.1111/j.1365-2818.1993.tb033-

657

79.x.

658

Li, J.Y., Niu, B.G. Song, B., and Zhao, Z.R. 1999. Crustal Formation and Evolution of

659

Northern Changbai Mountains, Northeast China. Beijing: Geological Publishing

660

House 137 pp (in Chinese with English abstracts).

661

Li, Z.X., Mca, C., and Powell. 2001. An outline of the palaegeographic evolution of the

Page 31 of 62

662

Australian region since the beginning of the Neoproterozoic. Earth-Science

663

Reviews, 53: 237-277.

664

Li, Q., Liu, S., Han, B., Zhang, J., and Chu, Z. 2005. Geochemistry of metasedime-

665

ntary rocks of the Proterozoic Xingxingxia complex: implications for provenance

666

and tectonic setting of the eastern segment of the Central Tianshan Tectonic Zone,

667

northwestern China. Canadian Journal of Earth Sciences, 42: 287-306. doi:10.11 -

668

39/e05-011.

669

Li, J.Y. 2006. Permian geodynamic setting of Northeast China and adjacent regions:

670

closure of the Paleo-Asian Ocean and subduction of the Paleo-Pacific Plate. Journal

671

of Asian Earth Sciences, 26: 207-224. doi:10.1016/j.jseaes.2005.09. 001.

672

Li, H., Xu, Y., Huang, X., He, B., Luo, Z., and Yan, B. 2009. Activation of northern

673

margin of the North China Craton in Late Paleozoic: Evidence from U-Pb dating

674

and Hf isotopes of detrital zircons from the Upper Carboniferous Taiyuan

675

Formation in the Ningwu-Jingle basin.Chinese Science Bulletin, 54: 677-686. doi:

676

10.1007/s11434-008-0444-9.

677

Li, W.M., Takasu, A., Liu, Y.J., and Guo, X.Z. 2010. Newly discovered garnet-

678

barroisite schists from the Heilongjiang Complex in the Jiamusi Massif,

679

Northeastern China. Journal of Mineralogical and Petrological Sciences, 105:

680

86-91. doi:10.2465/jmps.091015d.

681

Li, D., Chen, Y., Wang, Z., Hou, K., and Liu, C. 2011a. Detrital zircon U-Pb ages, Hf

682

isotopes and tectonic implications for Palaeozoic sedimentary rocks from the

683

Xing-Meng Orogenic Belt, middle-east part of Inner Mongolia, China. Geological

Page 32 of 62

684

Journal, 46: 63-81. doi:10.1002/gj.1257.

685

Li, Y., Xu, W.L., Wang, F., Tang, J., Pei, F.P., and Wang, Z.J. 2014. Geochronology and

686

geochemistry of late Paleozoic volcanic rocks on the western margin of the

687

Songnen-Zhangguangcai Range Massif, NE China: Implications for the amalga-

688

mation history of the Xing'an and Songnen-Zhangguangcai Range massif -

689

s. Lithos, 205: 394-410. doi:10.1016/j.lithos.2014.07.008.

690

Liu, J.F., Chi, X.G., Dong, C.Y., Zhi, Z., and Li, G.R. 2008. Discovery of Early

691

Paleozoic granites in the eastern Xiao Hinggan Mountains, Northeastern China and

692

their tectonic significance. Geological Bulletin of China, 27: 534-544.

693

Liu, J., Liu, F., Ding, Z., Yang, H., Liu, C. ,Liu, P., Xiao, L., Zhao, L., and Geng, J. 2013.

694

U-Pb dating and Hf isotope study of detrital zircons from the Zhifu Group, Jiaobei

695

Terrane, North China Craton: Provenance and implications for Precambri - an

696

crustal growth and recycling. Precambrian Research, 235: 230-250. doi:10.101-

697

6/j.precamres.2013.06.014.

698

Long, X., Yuan, C., Sun, M., Zhao, G., Xiao, W., Wang, Y., Yang, Y., and Hu, A. 2010.

699

Archean crustal evolution of the northern Tarim Craton, NW China: zircon U-Pb

700

and Hf isotopic constraints. Precambrian Research, 180: 272-284. doi:10.1016/j.-

701

precamres.2010.05.001.

702

Lu, S., Li, H., Zhang, C., and Niu, G. 2008. Geological and geochronological evidence

703

for the precambrian evolution of the Tarim Craton and surrounding continental

704

fragments. Precambrian Research, 160: 94-107. doi:10.1016/j. preca- mres.

705

2007.04.025.

Page 33 of 62

706 707

Ludwig, K.R. 2003. User's manual for ISOPLOT 3.00: a geochronological toolkit for Microsoft Excel. Berkeley Geochronology Center Special Publication no. 4.

708

Maynard, J.B., Valloni, R., and Yu, H.S. 1982. Composition of modern deep-sea sands

709

from arc-related basins. Geological Society of London Special Publications, 10:

710

551-561. doi:10.1144/GSL.SP.1982.010.01.36.

711

McLennan, S.M., Hemming, S., McDaniel, D.K., and Hanson, G.N. 1993. Geochem-

712

ical approaches to sedimentation, provenance, and tectonics. Special Paper of the

713

Geological Society of America, 284:21-40. doi:10.1130/SPE284-p21.

714

Meng, E., Xu, W.L., Pei, F.P., Yang, D.B., Yu, Y., and Zhang, X.Z. 2010. Detrital-

715

Zircon Geochronology Of Late Paleozoic Sedimentary Rocks In Eastern Heilong-

716

jiang Province, NE China: Implications For The Tectonic Evolution Of The Eastern

717

Segment Of The Central Asian Orogen. Tectonophysics, 485: 42-51. doi:

718

10.1016/j.tecto.2009.11.015.

719

Miao, L.C., Liu, D.Y., and Zhang, F.Q. 2007. Zircon SHRIMP U-Pb ages of the “Xing

720

-huadukou Group” in Hanjiayuanzi and Xinlin areas and the “Zhalantun Group” in

721

Inner Mongolia, Da Hinggan Mountains. Chinese Science Bulletin, 52: 1112- 1134.

722

doi:10.1007/s11434-007-0131-2.

723

Myrow, P. M., Hughes, N. C., Paulsen, T. S., Williams, I. S., Parcha, S. K., Thompson,

724

K. R., Bowring, S.A., Peng, S.C., and Ahluwalia, A.D. 2003. Integrated tectono-

725

stratigraphic analysis of the Himalaya and implications for its tectonic reconstruc -

726

tion. Earth and Planetary Science Letters, 212: 433-441. doi:10.1016/S0012-821-

727

X(03)00280-2.

Page 34 of 62

728

Nelson, D. R. 2001. An assessment of the determination of depositional ages for pre-

729

cambrian clastic sedimentary rocks by U-Pb dating of detrital zircons. Sedimen-

730

tary Geology, 141-142: 37-60. doi:10.1016/S0037-0738(01) 00067-7.

731

Pei, F.P., Xu, W.L., Yang, D.B., Zhao, Q.G., Liu, X.M., and Hu, Z.C. 2007. Zircon U-

732

Pb geochronology of basement metamorphic rocks in the Songliao Basin. Chines

733

e Science Bulletin, 52: 942-948. doi:10.1007/s11434-007-0107-2.

734

Pei, F.P., Wang, Z. W., Cao, H.H., Xu, W.L., and Wang, F. 2014. Petrogenesis of the

735

Early Paleozoic tonalite in the central Jilin Province: evidence from zircon U-Pb

736

chronology and geochemistry. Acta Petrologica Sinica, 30: 2009-2019 (in Chinese

737

with English abstracts).

738

Pei, F.P., Zhang, Y., Wang, Z.W., Cao, H.H., Xu, W.L., Wang, Z.J., Wang, F., and Yang,

739

C. 2015. Early-Middle Paleozoic subduction-collision history of the south-eastern

740

Central Asian Orogenic Belt: Evidence from igneous and metasedimentary rocks of

741

central Jilin Province, NE China. Lithos, 261: 164-180. doi:10.1016/j.lithos.

742

2015.12.010.

743

Peng, Y.J., Liu, A., Li, W.G., and Zhao, C.B. 1999. Three types of the Permian floras

744

and old continental margin reconstruction in the Yanbian area, Jilin Province. Jilin

745

Geolgy, 18: 1-12 (in Chinese ).

746

Peng, Y., and Zhao, C. 2001. The evolution of the Paleo Jihei Orogenic Belt and accr-

747

etion of the continental crust. Jilin Geolgy, 20: 1-9 (in Chinese with English abstr-

748

acts).

749

Pettijohn, F.J., Potter, P.E., and Siever, R. 1987. Sand and Sandstone. Springer New

Page 35 of 62

750

York, 547 pp.

751

Rashid, S.A. 2002. Geochemical characteristics of Mesoproterozoic clastic sedimen-

752

tary rocks from the Chakrata Formation, Lesser Himalaya: implications for crustal

753

evolution and weathering history in the Himalaya. Journal of Asian Earth Sciences,

754

21: 283-293. doi:10.1016/S1367-9120(02)00071-8.

755

Ravikant, V., Wu, F.Y., and Ji, W.Q. 2011. U-Pb age and Hf isotopic constraints of

756

detrital zircons from the Himalayan foreland Subathu sub-basin on the Tertiary

757

palaeogeography of the Himalaya. Earth and Planetary Science Letters, 304:

758

356-368. doi:10.1016/j.epsl.2011.02.009.

759

Richard, Jongens, John, D., Bradshaw, and Andrew, P.Fowler. 2003. The balloon

760

Melange, northwest Nelson: Origin, structure, and emplacement. New Zealand

761

Journal of Geology and Geophysics, 46: 437-448. doi:10.1080/00288306.2003.

762

9515019.

763

Rojas-Agramonte, Y., Kröner, A., Demoux, A., Xia, X., Wang, W., Donskaya, T., Liu,

764

D., and Sun, M. 2011. Detrital and xenocrystic zircon ages from Neoproterozoic to

765

Palaeozoic arc terranes of Mongolia: Significance for the origin of crustal frag-

766

ments in the Central Asian Orogenic Belt. Gondwana Research, 19: 751-763. doi:

767

10.1016/j.gr.2010.10.004.

768

Roser, B.P., and Korsch, R.J. 1986. Determination of Tectonic Setting of Sandstone-

769

Mudstone Suites Using, Content and, Ratio. Journal of Geology, 94: 635-650.

770

doi:10.1086/629071.

Page 36 of 62

771

Rosen, O.M., Levskii, L.K., Zhuravlev, D.Z., Rotman, A.Y., Spetsius, Z.V., Makeev,

772

A.F., Zinchuk, N.N., Manakov, A.V., and Serenko, V.P. 2006. Paleoproterozoic

773

accretion in the Northeast Siberian craton: Isotopic dating of the Anabar collision

774

system. Stratigraphy and Geological Correlation, 14: 581-601. doi:10.1134/S0-

775

869593806060013.

776 777

Rudnick, R., and Gao, S. 2003. Composition of the continental crust. Treatise Geo chem, 3:1-64.

778

Sal’nikova, E.B., Kotov, A.B., Levitskii, V.I., Reznitskii, L.Z., Mel’nikov, A.I.,

779

Kozakov, I.K., Kovach, V.P.,Barash, I.G., and Yakovleva, S.Z. 2007. Age

780

constraints of high-temperature metamorphic events in crystalline complexes of the

781

Irkut block, the Sharyzhalgai ledge of the Siberian platform basement: Results of

782

the U-Pb single zircon dating. Stratigraphy and Geological Correlation, 15:

783

343-358. doi:10.1134/S0869593807040016.

784

SengÖr, A.M.C., and B.A. Natal'in. 1996. Paleotectonics of Asia: Fragment of a synth

785

esis. In Yin, A., Harrison, T.M. (Eds.) The tectonic Evolution of Asia. Cambridge

786

University Press, Cambridge UK, pp. 486-640.

787 788

Shao, J.K.1991. Crustal Evolution in the Middle Part of the Northern Margin of the Sino-Korean Plate. Beijing: Peking University Press 135 pp (in Chinese).

789

Shao, J.A., and Tang, K.D.1995. The Ophiolite Melange in Kaishantun, Jinn Province,

790

China. Acta Petrologica Sinica, 11: 212-20 (in Chinese with English abstracts).

791

Shaw, D.M. 1972. The origin of the Apsley gneiss, Ontario. Canadian Journal of Earth

792

Sciences, 9:18-35. doi:10.1139/e72-002.

Page 37 of 62

793

Simonen, A.1953. Stratigraphy and sedimentation of the svecofennidic, Early Archean

794

supracrustal rocks in southwestern Finland. Bulletin of the Geological Society of

795

Finland, 160: 1-64.

796

Squire, R.J., Campbell, I.H., Allen, C.M., and Wilson, C.J.L. 2006. Did the transgon-

797

dwanan supermountain trigger the explosive radiation of animals on earth?. Earth

798

and Planetary Science Letters, 250: 116-133. doi:10.1016/j.epsl. 2006.07.032.

799

Stern, J.R. 2008. Neoproterozoic crustal growth: the solid Earth system during a critical

800

episode of Earth history. Gondwana Research, 14: 33-50. doi:10.1016/j.-

801

gr.2007.08.006.

802

Sun, S.S., and Mcdonough, W.F. 1989. Chemical and isotopic systematics of oceanic

803

basalts; implications for mantle composition and processes. Geological Society

804

London Special Publications, 42: 313-345. doi:10.1144/GSL.SP.1989.042.01.19.

805

Sun, D.Y., Gou, J., Wang, T.H., Ren, Y. S., Liu, Y. J., Guo, H.Y., Liu, X.M., and Hu, Z.

806

C. 2013a. Geochronological and geochemical constraints on the Erguna massif

807

basement, NE China-subduction history of the Mongol-Okhotsk oceanic crus-

808

t. International Geology Review, 55: 1801-1816. doi:10.1080/00206814.2013.

809

804664.

810

Sun, Y., Li, M., Ge, W., Zhang, Y., and Zhang, D. 2013b. Eastward termination of the

811

Solonker-Xar Moron River Suture determined by detrital zircon U–Pb isotopic

812

dating and Permian floristics. Journal of Asian Earth Sciences, 75: 243-250. doi:

813

10.1016/j.jseaes.2013.07.018.

814

Tang, K.D. 1990. Tectonic development of Paleozoic foldbelts at the north margin of

Page 38 of 62

815

the Sino-Korean Craton. Tectonics, 9: 249-260. doi:10.1029/TC009i002p00249.

816

Tang, K.D., and Zhao, A.L. 2007. New evidence of palaeozoic stratigraphy in the

817

kaishantun area, Yanbian,Jilin. Journal of stratigraphy, 2: 141-149 (in Chinese with

818

English abstracts).

819

Tang, J., Xu, W.L., Wang, F., Wang, W., Xu, M.J., and Zhang, Y.H. 2014. Geochrono-

820

logy and geochemistry of Early-Middle Triassic magmatism in the Erguna Massif,

821

NE China: Constraints on the tectonic evolution of the Mongol-Okhotsk

822

Ocean. Lithos, 184-187: 1-16. doi:10.1016/j.lithos.2013.10.024.

823

Tarrey, J., Dalziel,I., and Witt, M. 1976. Marginal basin Rocas Verdes complex form S.

824

Chile: A model for Archaean green stone belt formation. Windley, B.F. The Early

825

History of Earth. London: Woley pp.131-146.

826

Vervoort, J.D., Patchett, P.J., Blichert-Toft, J., and AlbarÉde, F. 1999. Relationships

827

between Lu-Hf and Sm-Nd isotopic systems in the global sedimentary system. Ea-

828

rth and Planetary Science Letters, 168:79-99. doi:10.1016/S0012-821X(99)0004-

829

7-3.

830

Wang, Y.Q., Su, Y.Z., and Liu, E.Y. 1997. Regional Stratigraphy in Northeastern Chi -

831

na. Wuhan: Chinese Geology University Press 175 pp (in Chinese with English

832

abstracts).

833

Wang, Z. 1998. A preliminary study on the evolutionary characteristics of the preme-

834

sozoic main metamorphic rocks of the Yanbian area, Jilin province. Jilin Geolgy, 17:

835

31-41 (in Chinese with English abstracts).

836

Wang, F., Xu, W.L., Meng, E., Cao, H.H., and Gao, F.H. 2012a. Early Paleozoic amal-

Page 39 of 62

837

gamation of the Songnen-Zhangguangcai range and Jiamusi massifs in the eastern

838

segment of the Central Asian Orogenic Belt: geochronological and geochemical

839

evidence from granitoids and rhyolites. Journal of Asian Earth Sciences, 49: 234-

840

248. doi:10.1016/j.jseaes.2011.09.022.

841

Wang, F., Xu, W.L., Gao, F.H., Meng, E., Cao, H.H., Zhao, L., and Yang,Y. 2012b.

842

Tectonic history of the Zhangguangcailing Group in eastern Heilongjiang

843

Province, NE China: Constraints from U-Pb geochronology of detrital and mag-

844

matic zircons. Tectonophysics, 566-567:105-122. doi:10.1016/j.tecto.2012.07.018.

845

Wang, F., Xu, W.L., Gao, F.H., Zhang, H.H., Pei, F.P., Zhao, L., and Yang, Y. 2014.

846

Precambrian terrane within the Songnen-Zhangguangcai range massif, NE china:

847

evidence from U-Pb ages of detrital zircons from the Dongfengshan and Tadong

848

groups. Gondwana Research, 26: 402-413. doi:10.1016/j.gr.2013.06.017.

849

Wang, Z.J., Xu, W.L., Pei, F.P., Wang, Z.W., and Li, Y. 2015a. Geochronology and

850

provenance of detrital zircons from late Palaeozoic strata of central Jilin Province,

851

Northeast China: implications for the tectonic evolution of the eastern Central As

852

ian Orogenic Belt. International Geology Review, 57: 211-228. doi:10.1080

853

/00206814.2014.1002118.

854

Wang, Z.W., Xu, W.L., Pei, F.P., Wang, F., and Guo, P. 2015b. Geochronology and

855

geochemistry of early Paleozoic igneous rocks of the Lesser Xing’an Range, NE

856

China: Implications for the tectonic evolution of the eastern Central Asian Oro-

857

genic Belt. Lithos, 15:1-15. doi:10.1016/j.lithos.2015.11.006.

858

Wang, Z.W., Pei, F.P., Xu, W.L., Cao, H.H., and Wang, Z.J. 2015c. Geochronology and

Page 40 of 62

859

geochemistry of Late Devonian and early Carboniferous igneous rocks of cen- tral

860

Jilin Province, NE China: Implications for the tectonic evolution of the easte- rn

861

Central Asian Orogenic Belt. Journal of Asian Earth Sciences, 97: 260-278. doi:

862

10.1016/j.jseaes.2014.06.028.

863

Wang, Z.W., Pei, F.P., Xu, W.L., Cao, H.H., Wang, Z.J., and Zhang, Y. 2016. Tectonic

864

evolution of the eastern Central Asian Orogenic Belt: Evidence from zircon U-Pb-

865

Hf isotopes and geochemistry of early Paleozoic rocks in Yanbian region, NE Chi-

866

na. Gondwana Research, 38: 334-350. doi:10.1016/j.gr.2016.01.004.

867

Wilde, S.A., Zhang, X.Z., and Wu, F.Y. 2000. Extension of a newly-identified 500 Ma

868

metamorphic terrain in Northeast China: further U-Pb SHRIMP dating of the Ma-

869

shan Complex, Heilongjiang Province, China. Tectonophysics, 328: 115-130.

870

doi:10.1016/S0040-1951(00)00180-3.

871

Wilde, S.A., Wu, F.Y., and Zhang, X.Z. 2003. Late Pan-African magmatism in North-

872

eastern China: SHRIMP U-Pb zircon evidence for igneous ages from the Mashan

873

Complex. Precambrian Research, 122: 311-327. doi:10.1016/S0301-9268(02)00

874

217-6.

875

Wilde, S.A., Wu, F.Y., and Zhao, G. 2010. The Khanka Block, NE China, and its sign-

876

ificance for the evolution of the Central Asian Orogenic Belt and continental accr-

877

etion. Geological Society London Special Publications, 338: 117-137. doi:10.114-

878

4/SP338.6.

879

Windley, B.F., Alexeiev, D., Xiao, W.J., Kröner, A., and Badarch, G.2007. Tectonic

880

model for accretion of the Central Asian Orogenic Belt. Journal of the Geological

Page 41 of 62

881

Society of London, 164: 31-47. doi:10.1144/0016-76492006-022.

882

Wu, F.Y., Yang, Y.H., Xie, L.W., Yang, J.H., and Xu, P. 2006. Hf isotopic compo-

883

sitions of the standard zircons and baddeleyites used in U-Pb geochronology.

884

Chemical Geology, 234: 105-126. doi:10.1016/j.chemgeo.2006.05. 003.

885

Wu, F.Y., Zhao, G.C., Sun, D.Y., Wilde, S.A., and Yang, J.H. 2007. The Hulan Group:

886

Its role in the evolution of the Central Asian Orogenic Belt of NE China. Journal of

887

Asian Earth Sciences, 30: 542-556. doi:10.1016/j.jseaes.2007.01.003.

888

Wu, F.Y., Sun, D.Y., Ge, W.C., Zhang, Y.B., Grant, M.L., and Wilde, S.A. 2011. Geo-

889

chronology of the phanerozoic granitoids in northeastern china. Journal of Asian

890

Earth Sciences, 41:1-30. doi:10.1016/j.jseaes.2010.11.014.

891

Xiao, W.J., Windly, B.F., Hao, J., and Zhai, M.G. 2003. Accretion leading to collision

892

and the Permian Solonker suture,Inner Mongolia,China:Termination of the Central

893

Asian Orogenic Belt. Tectonics, 22: 1069 -1089. doi:10.1029/2002TC001484.

894

Xiao, W.J., Windley, B.F., Huang, B.C., Han, C.M., Yuan, C., Chen, H.L., Sun, M., Sun,

895

S., and Li, J.L. 2009. End-Permian to mid-Triassic termination of the accre- tionary

896

processes of the southern Altaids: implications for the geodynamic evolu- tion,

897

Phanerozoic continental growth, and metallogeny of Central Asia. Interna- tional

898

Journal of Earth Sciences, 98: 1189-1217. doi:10.1007/s00531-008- 0407-z.

899

Xu, W.L., Wang, F., Pei, F.P., Meng, E., Tang, J., Xu, M.J., and Wang, W. 2013. Meso-

900

zoic tectonic regimes and regional ore-forming background in NE China: constra-

901

ints from spatial and temporal variations of Mesozoic volcanic rock associa-

902

tions. Acta Petrologica Sinica, 29: 339-353 (in Chinese with English ab- stracts)

Page 42 of 62

903

Yang, J.H., Wu, F.Y., Shao, J.A., Wilde, S.A., Xie, L.W., and Liu, X.M. 2006. Constr-

904

aints on the timing of uplift of the Yanshan Fold and Thrust Belt, North China. Ea-

905

rth and Planetary Science Letters, 246: 336-352. doi:10.1016/j.epsl.2006.04. 029.

906

Yang, H., Ge, W.C., Zhao, G.C., Dong, Y., Bi, J.H., Wang, Z.H., Yu, J.J., and Zhang,

907

Y.L. 2014. Geochronology and geochemistry of Late Pan-African intrusive rocks in

908

the Jiamusi-Khanka Block, NE China: Petrogenesis and geodynamic implica-

909

tions. Lithos, 208-209: 220-236. doi:10.1016/j.lithos.2014.09.019.

910

Yang, H., Ge, W.C., Zhao, G.C., Bi, J.H., Wang, Z.H., Dong, Y., and Xu, W.L. 2017

911

Zircon U-Pb ages and geochemistry of newly discovered Neoproterozoic orthogn-

912

eisses in the Mishan region, NE China: Constraints on the high-grade metamorph-

913

ism and tectonic affinity of the Jiamusi-Khanka Block. Lithos, s 268-271: 16-31.

914

doi: 10.1016/j.lithos.2016.10.017.

915

Ying, J.F., Zhou, X.H., Zhang, L.C., Wang, F., and Zhang, Y.T. 2008. Geochronologic-

916

al and geochemical investigation of the late mesozoic volcanic rocks from the

917

northern great xing’an range and their tectonic implications. International Journal

918

of Earth Sciences, 99: 357-378.

919

Yuan, H., Gao, S., Liu, X., Li, H., Günther, D., and Wu, F. 2004. Accurate U-Pb age and

920

trace element determinations of zircon by laser ablation-inductively coupled

921

plasma-mass spectrometry. Geostandards and Geoanalytical Research, 28: 353-

922

370. doi:10.1111/j.1751-908X.2004.tb00755.x.

923

Yuan, H.L., Gao, S., Dai, M.N., Zong, C.L., Günther, D., Fontaine, G.H., Liu, X.M., and

924

Diwu, C.R. 2008. Simultaneous determinations of U-Pb age, Hf isotopes and trace

Page 43 of 62

925

element compositions of zircon by excimer laser-ablation quadrupole and

926

multiple-collector ICP-MS. Chemical Geology, 247: 100-118. doi:10.1016/j.che-

927

mgeo.2007.10.003.

928

Yu, J.J., Wang, F., Xu, W.L., Gao, F.H., and Pei, F.P. 2012. Early Jurassic mafic

929

magmatism in the Lesser Xing'an-Zhangguangcai Range, NE China, and its

930

tectonic implications: Constraints from zircon U-Pb chronology and geochemistry.

931

Lithos, 142-143: 256-266. doi:10.1016/j.lithos.2012.03.016.

932

Zhai, M., Guo, J., and Liu, W. 2005. Neoarchean to Paleoproterozoic continental

933

evolution and tectonic history of the North China Craton: a review. Journal of Asian

934

Earth Sciences, 24: 547-561. doi:10.1016/j.jseaes.2004.01.018.

935

Zhang, Y.B., Wu, F.Y., Wilde, S.A., Zhai, M., Lu, X., and Sun, D. 2004. Zircon U-Pb

936

ages and tectonic implications of ‘Early Paleozoic’ granitoids at Yanbian, Jilin

937

Province, northeast China. Island Arc, 13: 484-505. doi:10.1111/j.1440-1738.2004.

938

00442.x.

939

Zhang, S.H., Zhao, Y., Ye, H., Liu, J.M., and Hu, Z.C. 2014. Origin and evolution of the

940

bainaimiao arc belt: implications for crustal growth in the southern Central Asian

941

Orogenic Belt. Geological Society of America Bulletin, 126: 1275-1300.

942

doi:10.1130/B31042.1.

943

Zhao, C.J., Peng, Y.J., Dang, Z.X., and Zhang, Y.P. 1996. Tectonic Framework and

944

Crust Evolution of Eastern Jilin and Heilongjiang Provinces. Shenyang: Liaoning

945

University Press 186 pp (in Chinese with English abstracts).

946

Zhao, G.C, Cawood, P.A., Li, S., Wilde, S.A., Sun, M., Zhang, J., He, Y.H., and Yin,

Page 44 of 62

947

C.Q. 2012a. Amalgamation of the North China Craton: Key issues and discussion.

948

Precambrian Research, 222-223:55-76. doi: 10.1016/j.precamres.2012.09.016.

949

Zhao, G.C., and Guo, J.H. 2012b. Precambrian geology of China: preface. Precam-

950

brian Research, 222-223: 1-12. doi:10.1016/j.precamres.2012.09.018.

951

Zhou, J.B, Wilde, S.A., Zhao, GC. Zhang, X.Z., Wang, H., and Zeng, W.S. 2010a. Was

952

the easternmost segment of the Central Asian Orogenic Belt derived from

953

Gondwana or Siberia: An intriguing dilemma? Journal of Geodynamics, 50: 300-

954

317. doi:10.1016/j.jog.2010.02.004.

955

Zhou, J.B., Wilde, S. A., Zhao, G., Zhang, X., Zheng, C., and Zeng, H.W.W. 2010b.

956

Pan-african metamorphic and magmatic rocks of the Khanka massif, NE China:

957

further evidence regarding their affinity. Geological Magazine, 147: 737-749. doi:

958

10.1017/S0016756810000063.

959

Zhou, J.B., Wilde, S.A., Zhang, X.Z., Ren, S.M., and Zheng, C.Q. 2011. Early Paleoz-

960

oic metamorphic rocks of the Erguna block in the Great Xing'an Range, NE China:

961

Evidence for the timing of magmatic and metamorphic events and their tectonic

962

implications. Tectonophysics, 499: 105-117. doi:10.1016/j.tecto.2010.12.009.

963

Zhou, J.B., Wilde, S.A., and Zhang, X.Z. 2012. Detrital Zircons from Phanerozoic

964

Rocks of the Songliao Block.NE China:Evidence and Tectonic Implications.

965

Journal of Asian Earth Sciences, 47: 21-34. doi:10.1016/j.jseaes.2011.05.004.

966

Zhou, Z.B., Pei, F.P., Wang, Z.W., Cao, H.H., Xu, W.L., Wang, Z.J., and Zhang, Y. 2017.

967

Detrital zircons from late Permian to Triassic sedimentary rocks of Jilin Province,

968

NE China: Constraints on the timing of final closure of the Paleo-Asian Ocean.

Page 45 of 62

969

Journal of Asian Earth Sciences, 144:82-109. doi: 10.1016/j.jseaes.2016. 12.007.

970

Zhu, W., Zheng, B., Shu, L.Ma, D., Wu, H., and Li, Y. 2011. Neoproterozoic tectonic

971

evolution of the Precambrian Aksu blueschist terrane, northwestern Tarim, China:

972

Insights from LA-ICP-MS zircon U-Pb ages and geochemical data. Precambrian

973

Research, 185: 215-230. doi:10.1016/j.precamres.2011.01.012.

974 975

Figure captions

976

Fig. 1. Tectonic sketch maps of NE China, modified from Wu et al. (2007). The inset (a)

977

shows the tectonic setting of NE China. DAK: Dashanzui-Antu-Kaishantun suture belt,

978

GFC: Gudonghe-Fuerhe-Chongjin Fault, and WH: Wangqing-Hunchun suture belt.

979

Fig. 2. Detailed geological map of the southern Yanbian region in eastern Jilin Province,

980

NE China.

981

Fig. 3. Field photograph and photomicrographs of the meta-sedimentary rocks from the

982

Jiangyu Group of the southern Yanbian region, eastern Jinlin Province, NE China (b, e

983

= cross-polarized light; c, f = plane-polarized light). (a) Field location of the

984

biotite-plagioclase gneiss sample HC-1. (b-c) Photomicrographs of the biotite-

985

plagioclase gneiss sample HC-1. (d) Field location of the two-mica schist sample HC-9.

986

(e-f) Photomicrographs of the two-mica schist sample HC-9. Ser: sericite, Bi: biotite,

987

Gt: garnet, Mus: muscovite, Pl: plagioclase, and Qtz: quartz.

988

Fig. 4. Cathodoluminescence (CL) images of selected zircons from the

989

meta-sedimentary rocks of the Jiangyu Group. These zircons were analysed in the

990

present study. Note: Solid and dashed circles represent U-Pb dating and Lu-Hf analysis

Page 46 of 62

991

positions, respectively. The numbers show the ages of the zircons and the ƐHf(t) values,

992

respectively.

993

Fig. 5. (a) U-Pb concordia diagram of all zircon data for sample HC-1; (b) U-Pb

994

concordia diagram of zircon data for sample HC-1 showing the young age population

995

with the weighted mean age of the youngest zircons, which was used to calculate the

996

maximum depositional age; (c) relative probability plot of zircon U-Pb ages for sample

997

HC-1; (d) U-Pb concordia diagram of all zircon data for sample HC-9; (e) U-Pb

998

concordia diagram of zircon data for sample HC-9 showing the young age population

999

with the weighted mean age of the youngest zircons, which was used to calculate the

1000

maximum depositional age; and (f) relative probability plot of zircon U-Pb ages for

1001

sample HC-9.

1002

Fig. 6. Chondrite-normalized REE patterns and upper continental crust-normalized

1003

spider diagrams of meta-sedimentary rocks from the Jiangyu Group in the southern

1004

Yanbian region, eastern Jinlin Province, NE China. The chondrite data are from Sun

1005

and McDonough (1989), and the upper continental crust data are from Rudnick and

1006

Gao (2003). The UCC (Rudnick and Gao 2003) and PAAS patterns (McLennan et al.

1007

1993) are shown for comparison.

1008

Fig. 7. Correlations between zircon Hf isotopic compositions and ages of the

1009

meta-sedimentary rocks in the Jiangyu Group, XMOB: Xing’an-Mongolia orogenic

1010

Belt, and YFTB: Yanshan Fold and Thrust Belt (Yang et al. 2006). The sedimentary

1011

rock data from northeastern Gondwana (i.e. Australia and Antarctica) are from Kemp et

1012

al. (2006) and Ravikant et al. (2011) and the references therein. The data shown in

Page 47 of 62

1013

dashed circles are from Wang et al. (2016).

1014

Fig. 8. Protolith reconstruction discrimination diagrams for meta-sedimentary rocks in

1015

the Jiangyu Group. (a) TiO2-SiO2 diagram (after Tarrey et al. 1976). (b)

1016

Si-(al+fm)-(c+alk) diagram (after Simonen 1953). (c) log(Na2O/K2O)- log(SiO2/Al2O3)

1017

diagram (after Pettijohn et al. 1987).

1018

Fig. 9. Relative probability plot of zircon data from the Jiangyu Group (d), compared

1019

with zircon ages from the eastern XMOB (a), northern NCC (b) and northeastern

1020

Gondwana (c). The data in (a) are from Sun et al. (2013b); the data in (b) are from Sun

1021

et al. (2013b); and the data in (c) are from Rojas-Agramonte et al. (2011).

1022

Fig. 10. Major element discrimination diagrams for meta-sedimentary rocks from the

1023

Jiangyu Group. (a) K2O/Na2O-SiO2 diagram (after Roser and Korsch 1986) and (b)

1024

SiO2/Al2O3-K2O/Na2O diagram (after Maynard et al. 1982). OIA: oceanic island arc,

1025

ACM: active continental margin, PM: passive continental margin, A1: island arc, and

1026

A2: evolved island arc.

1027

Fig. 11. Tectonic setting discrimination diagrams for the meta-sedimentary rocks from

1028

the Jiangyu Group. (a) La-Th-Sc, (b) Th-Sc-Zr/10, and (c) Ti/Zr-La/Sc diagrams from

1029

Bhatia and Crook (1986). The symbols are the same as those in Fig. 10.

1030

Fig. 12. Simplified geological map of the potential positions and tectonic evolution of

1031

the Jiangyu continental arc terrane (modified from Li and Powell, 2001; Wang et al.

1032

2016). NCC: North China Craton, SCC: South China Craton, and JT: Jiangyu

1033

continental arc terrane.

1034

Fig. 13. Simplified geological map of central-eastern Jilin with the locations of the

Page 48 of 62

1035

early to middle Paleozoic igneous rocks along the eastern segment of the northern

1036

margin of the NCC (modified after Han et al. 2018).

Page 49 of 62

Table 1. Comparison of the geochemical characteristics of the Jiangyu Group sedimentary rocks to those of rocks from various tectonic settings Sample

tectonic setting

number

La

Ce

∑REE

La/Yb

(La/Yb)N

∑LREE/∑HREE

δEu

1

Oceanic island arc

9

8±1.7

19±3.7

58±10

4.2±1.3

2.8±0.9

3.8±0.9

1.04±0.11

2

Continental island arc

9

27±4.5

59±8.2

146±20

11.0±3.6

7.5±2.5

7.7±1.7

0.79±0.13

3

Active continental margin

2

37

78

186

12.5

8.5

9.1

0.60

4

Passive continental margin

2

39

85

210

15.9

10.8

8.5

0.56

5

Jiangyu Group

14

31.44

62.41

157.44

9.64

6.92

6.89

0.69

Note: Data for samples 1-4 are from Bhatia (1985). Sample 5 data are averages for the Jiangyu Group.

Page 50 of 62

130°

110° 40

100 140 160

60

180

(a)

(b)

180

Baltic 60 Craton es lid ra U

Omolon Massif and its suroundings

170 60 160

Siberian Craton

Erg

50 150

50

C A O B

40

XMOB

Tarim

Fig.1b

North China Craton 30

Xin

140 30

Tibet block

M una

ass

1

40

Sutures and Faults 1 : Xiguitu-Tayuan 2 : Hegenshan-Heihe 3 : Solonker-Xra Moron - Changchun 4 : Jiayin-Mudanjiang 5 : Yitong-Yilan 6 : Dunhua-Mishan

Russia

n ga

Ma

if

50°

Heihe

if ss

Nadanhada Terrane

SE China

ne Song

To Solonker

n-Zh

130

uan angg

gcai

R

nge

2

Hegenshan

sif M a s Songliao basin ange

r M o ro n 3 Xa

Fig.13

Changchun

i Ra

120

gca

Mongolia

Erlianhot

40°

110

5

uan

100

Jiamusi Massif

4

ngg

45°

90

Zha

80

45°

6 Khanka Massif WH

continental margin accretionary belt DAK GFC

North China Craton

N.Korea 115°

125°

Study area 0

100 200 km

135°

Page 51 of 62

42° 40´

129°30´

+ + + Legend + +++ Cenozoic + + Zhixin +++ P1 Early + + K1 K1 Cretaceous P3 + ++ ++ Late Triassic T3 +++ + + + Early Permian P1 ++ + + + + + + Cpb Carboniferous + ++ + + + + + Cpd + + -Permian + + + + + + + + + + + + + + + Late + + ++ + ++ + ++ + + + + C Carboniferous + + + + + + ++ ++ + + + + + + + + + + 42° + + 35´ + + + C + Jiangyu + + + + + + + + ++ JG + + + Group + + ++ + + + + + + + + + + ++ + + + + Late Permian + ++ + + + + ++ + +++ + ++ + + P3 + utramafic rocks + ++ ++ + + + ++ + + + + + + + T3 + Mesozoic + + + + + + + + + + + + + + granite JG + + + + + + ++ ++ + + + + + + + + + + + + Fault + + + + ++ + + ++ + + + + + + + + ++ + + + + ++ + + + National + + + + + + + + ++ + + + + + + + boundary + + + + + + + + + + + + + + + + + + ++ ++ + + + + + Sample + + + + + + + + + + + + + + + + + + + + + + + + + + + + ++ location + + + + + + + + + + + + + + + ++ + + + + + + + + + + + + + + + + + + + + + + + + + + + + + + + + + ++ + + + + + + + ++ + + + + + + + + + + + + + + + + ++ ++ + + + + + ++ 42° 30´ 129°30´

129°45´

42° 40´

T3 Kedao + + + ++ + ++ + + + ++ ++ +++ + + + ++ +

N

42° 35´

Jiangyu

Beixing

0 129°45´

1

2Km 42° 30´

Page 52 of 62

a

d

HC-9

HC-1

Bi

b

e Mus

Gt

Bi Mus

Pl

Mus Qtz

Qtz

Ser

Qtz Qtz

Mus

Qtz 200µm

200µm

Bi

c

f Gt

Mus

Bi Mus

Pl Bi

Mus Qtz Ser

Qtz Qtz

Mus 200µm

Qtz

200µm

Page 53 of 62

100 µm

(a) HC-1 (+11.5)

(-3.0) 75

63

3

419±7

427±6

451±5

5

31

453±7

1130±21

1770±14

(-6.5)

62

23

29

634±9

42

2591±14

494±8

474±7

(-3.6)

43

32

36

438±5

(+0.8)

563±8

562±6 (+0.1)

19

14

1060±17

(b) HC-9

(+9.9)

1442±46

4

27 (+1.9)

38

2439±12

(-6.9)

(+6.7)

(-7.0)

2658±12 100 µm

29 31

28 37

3

417±6

428±6

(-0.1)

(+5.4)

12

11

27

434±7

(+6.6)

455±7 1843±14

498±7 (-3.0)

70

567±6

613±7

2636±12 66

75

1138±20 933±13

451±4

57

1096±18

15

1648±14

36 (+10.1)

2

2408±12

13 (+1.8)

2926±28

Page 54 of 62



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Page 55 of 62

1000

Sample/Chondrite

(a)

Jiangyu Group PAAS UCC

100

10 La Ce Pr Nd

Sm Eu Gd Tb Dy Ho Er TmYb Lu

10

Sample/ UCC

(b)

1

0.1

Rb Th

K Nb Ce Pr Nd Hf Tb Ti

Er Lu

Ba U Ta La Pb Sr Zr Sm Eu Dy Yb Y

Page 56 of 62

20 D e p le te

Hf(t)

10

(a) d m a n tl

XMOB

e

a .8G

1 t us C r Chondrite

0

ε

Cr -10

-20

Ga

3.

us

500

1000

a

t

Australia

0

0G

t

Cr

YFTB

-30

us

2.5

HC-1 HC-9

2000

1500

2500

3000

t(Ma) 20

D e p le te

Hf(t)

10

XMOB rus

(b) d m a n tl

1.8

t

e

Ga

2.5

C Chondrite

0

ε

Cr

-10

us

3.

0G

a

t

Cr

YFTB

Ga

us

t

Antarctica

-20

-30 0

500

1000

1500

t(Ma)

2000

2500

3000

Page 57 of 62 2.0

(a)

Jiangyu Group

TiO 2 (wt.%)

1.5

Sedimentary rocks

1.0

Igneous rocks 0.5

0.0 40

50

70

60

90

80

SiO 2 (wt.%) 70

(b) Pelite

(al+fm)-(c+alk)

60 50 40 Sandstone 30 Volcanics

20 Carbonate

10

sediments

0 0

100

300

200

400

500

Si

(c)

0.5

it e Quart

Arkose

z aren

Sub

-0.5

a r e n it e

ark

th

0.0

S u b li th

ar

ose

en

ite

Graywacke

Li

log(Na 2 O/k 2 O)

1.0

-1.0 0.0

0.5

1.0

log(SiO 2 /Al 2 O 3 )

1.5

2.0

Page 58 of 62 (a) Relative probability

Eastern XMOB N=662

(b) Relative probability

Northern NCC N=347

Relative probability

(c)

1860

NE Gondwana N=176

590

2520

970

Relative probability

(d)

455 Jiangyu Group N=186

428 476 564 622 9351124 200

1676 1979 2288 2649 1816 2423 2926

600 1000 1400 1800 2200 2600 3000

Age(Ma)

Page 59 of 62

100

(a)

江域岩组

K 2 O/Na 2 O

10 PM 1

ACM

0.1 OIA 0.01 40

50

70

60

80

90

SiO 2 (wt.%) 10

(b)

江域岩组

SiO 2 /Al 2 O 3

8 ACM

6

PM

4

2 0 0.01

A1

0.10

A2

1.00

K 2 O/Na 2 O

10.00

100

Page 60 of 62









  



 









 











 



   







 















Page 61 of 62

(a)

late Neoproterozoic SCC

Tarim JT NCC

Paleo-Pacific Ocean

Gondwanaland

early Ordovician

(b) NCC Paleo-Asian Ocean

JT

scc Paleo-Pacific Ocean Tarim

Gondwanaland

late Silurian- early Devonian

(c )

Paleo-Pacific Ocean Paleo-Asian Ocean JT

NCC

SCC

Tarim

Gondwanaland

Page 62 of 62

124°

125°

126°

127°

128°

129°

Legend + + Permian-Jurissic intrusive rocks

SXCYS-Solonker-Xar Moron-Changchun-Yanji suture YYF-Yitong-Yilan fault DMF-Dunmi-Mishan fault KSF-Kaiyuan-Shanchengzhen fault 44°

SX

Changchun CY

biotite schist 414-457 Ma Jiang et al. 2014

granodiorites 414&419 Ma Pei et al. 2016

S

acidic ignimbrite 392-449 Ma Jiang et al. 2014

Y

F

124°

+

125°

Early-middle Paleozoic igneous rocks

Y Jilin

DM Jiaohe

tonalite 443 Ma Pei et al. 2016 meta-diabase

+ +493+Ma + Pei+et+al. 2016 + ++ + monzogranite ++ ++ + + ++ 400 Ma + ++++ Pei et al. 2016 + + + Siping + + + + + + + + + + rhyolitic tuff + + + + + + + + + + + 410&403 Ma + + + + ++ + + + + + + + + +Pei + et al. +2016 + + ++ + + + + + + + + + + + + ++ + + ++ + + 43° ++ +++ ++ + + + + ++ + + + + + + + + + + Huadian + + ++ + + + + + + + + + + + + + Panshi+ + + ++ +++ ++ + + + + + +++ + monzogranite + ++ ++ + ++ + + + + + + + + + 396 Ma + ++ + Kaiyuan + + Pei+et al. 2016 + + + + + + + ++++ ++ ++ +++ + + ++++ ++ ++ +++ + + ++ +++ ++ ++ + ++++ ++ + K S+F+ rhyolitic rocks 390&425 Ma Han et al. 2018

Permian-Early Triassic mélange

metarhyolite 360Ma Wang et al. 2015c

126°

127°

F

++

+++ ++ ++ ++++ ++ + + Dunhua ++++ + ++ + ++ ++ + +++++ ++ + + + + + + +++ +++ ++ + + + + + + + ++ +++ + + + + + + + + ++ + + + + +++ + + + + + + + + + + ++ + + + + ++ + + + +++++ ++ +++ + + + ++ + + + +++++ ++ ++++ ++ + +++ ++ ++++++ + 43° + + ++ + + +++ ++ Yanji + + + + + + + + + ++ + + + + ++ + + ++++ + + + + tonalites Hunchun ++ ++ + + 422&423 Ma + + + Wang et al. 2016 ++ + + + ++ + + + ++ ++ + Helong + + ++ + + + ++ + + + ++ ++++ + Jiangyu + + ++ +++++++ Group ++ ++++++ ++ +++ + ++ 0 10 20km ++

128°

129°

130°

131°