Detrital zircon U-Pb geochronology and Hf isotopes of the Liaohe Group, Jiao-Liao-Ji Belt: Implications for the Paleoproterozoic tectonic evolution

Journal Pre-proofs Detrital zircon U-Pb geochronology and Hf isotopes of the Liaohe Group, JiaoLiao-Ji Belt: Implications for the Paleoproterozoic tectonic evolution Fang Wang, Fulai Liu, Hans-Peter Schertl, Wang Xu, Pinghua Liu, Zhonghua Tian PII: DOI: Reference:

S0301-9268(19)30533-9 https://doi.org/10.1016/j.precamres.2020.105633 PRECAM 105633

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Precambrian Research

Received Date: Revised Date: Accepted Date:

19 September 2019 18 January 2020 21 January 2020

Please cite this article as: F. Wang, F. Liu, H-P. Schertl, W. Xu, P. Liu, Z. Tian, Detrital zircon U-Pb geochronology and Hf isotopes of the Liaohe Group, Jiao-Liao-Ji Belt: Implications for the Paleoproterozoic tectonic evolution, Precambrian Research (2020), doi: https://doi.org/10.1016/j.precamres.2020.105633

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Detrital zircon U-Pb geochronology and Hf isotopes of the Liaohe Group, Jiao-Liao-Ji Belt: Implications for the Paleoproterozoic tectonic evolution Fang Wanga*, Fulai Liua, Hans-Peter Schertl

b,c,

Wang Xua, Pinghua Liua,

Zhonghua Tiana Corresponding author. E-mail address: [email protected] a

Key Laboratory of Deep-Earth Dynamics of Ministry of Natural Resources,

Institute of Geology, Chinese Academy of Geological Science, Beijing 100037, China b

Ruhr-University Bochum, Faculty of Geosciences, Institute of Geology,

Mineralogy & Geophysics, 44780 Bochum, Germany c

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

Technology, Qingdao, 266590, China Abstract The Jiao-Liao-Ji Belt (JLJB) is one of the most important Paleoproterozoic orogenic belts, which is intervening between the Longgang and Nangrim-Liaonan blocks. The Liaohe Group is an important research subject for understanding the Paleoproterozoic tectonic setting and evolution of the JLJB. However, the relationship of depositional spatial and chronological distributions between the North and South Liaohe groups are still under debates. In this paper, we present geochronological and zircon Lu-Hf isotopic results of meta-sedimentary rocks from the Liaohe Group to decipher their provenance depositional ages and environment, as well as their tectonic significance on the JLJB. The detrital zircons from the corresponding formations, including the Li’eryu, Gaojiayu and Dashiqiao formations of the North and South

Liaohe groups, show similarities in age patterns and Hf isotopic compositions. The detrital zircons from the Li’eryu Formation of the two groups display unimodal 207Pb/206Pb

age peaks at ca. 2.2-2.1 Ga. On the other hand, detrital zircons from the

Gaojiayu and Dashiqiao formations of the two groups, yield two dominating age peaks at ca. 2.2-2.1 and ~ 2.5 Ga. In summary, all detrital zircons with age peaks at ca. 2.2-2.1 Ga, have εHf(t) value of -6.99 to +9.41 and two-stage Hf depleted mantle ages (TDM2 model ages) of 3143 to 2137 Ma. The ~ 2.5 Ga detrital zircons however, have εHf(t) value and TDM2 model ages which widely range from -9.37 to +10.13 and from 349 to 2367 Ma, respectively. Geochronological results indicate that ca. 2.2-2.1 Ga zircons were derived from the Liaoji granitoids. The adjacent basement rocks of the Longgang and Liaonan-Nangrim blocks provide the major sources to detrital zircons that yield an age peak at ~ 2.5 Ga. Combined with previous studies, the new geochronological data suggest that the protoliths of the corresponding formations of the North and South Liaohe groups deposited their detritus progressively in a back-arc basin. The Liaoji granitoids are the main sources providing detritus for the Li’eryu Formation. Subsequently, clastic sediments transported from the Longgang and Liaonan blocks, as well as from the Liaoji granitoids, were successively deposited and provided sources to the Gaojiayu and Dashiqiao formations.

Keywords Detrital zircon; U-Pb ages; Hf isotopes; Liaohe Group; Jiao-Liao-Ji Belt

1. Introduction

The North China Craton (NCC) is an amalgamation of two distinct Archean to

Paleoproterozoic blocks, named the Western Block and the Eastern Block, separated by the Trans-North Orogen (e.g., Zhao et al., 1998, 2012; Kusky, 2001). The Eastern and Western Blocks amalgamated to form the NCC along the Trans-North Orogen at ~ 1.85 Ga during assembly of the Columbia supercontinent (Zhao et al., 2011). On the other hand, Kusky (2001) argued that the two separate blocks initially collided at ~ 2.5 Ga. Except for the Trans-North Orogen in the central region, another two Paleoproterozoic orogenic belts occur, the Khondalite Belt in the Western Block and the JLJB in the Eastern Block (Zhao et al., 1999, 2012). The JLJB recorded a long time and complex evolutionary history, and consists of greenschist-lower amphibolite facies meta-sedimentary-volcanic successions, and associated granitic and mafic intrusions (e.g., Li et al., 2005; Wu et al., 2007; Zhao et al., 2005; Luo et al., 2004, 2008; Yang et al., 2016). However, there has been a long-term and intense dispute on the tectonic setting and evolutionary history of the JLJB (e.g. Bai, 1993; Yang et al., 1988; Zhang and Yang, 1988; Liu et al., 1997; He and Ye, 1998a, b; Li et al., 2001a, b, 2005, 2006; Luo et al., 2004, 2008; Wang et al., 2011a). As noted from previous studies, several major tectonic setting models have been proposed, which referred to (a) opening and closing of an intra-continental rift (Zhang and Yang, 1988; Peng and Palmer, 1995; Li et al., 2005, 2006, 2012; Luo et al., 2004, 2008; Li and Zhao, 2007); (b) collision of continent-arc-continent (Bai, 1993; Faure et al., 2004; Li and Chen, 2014; Yuan et al., 2015; Yang et al., 2015, 2016); (c) a complex process from rifting to opening of an incipient ocean until subsequent subduction and collision (Zhao et al., 2012); (d) opening and closure of back-arc basin or retro-arc foreland basin (Wang

et al., 2011a; Meng et al., 2014; Li et al., 2017a, b; Xu et al., 2017, 2018a, 2018b). Contradictions related to the four models mainly result from disparate metamorphic P-T paths, and depositional ages and environment of the meta-sedimentary rocks of the North and South Liaohe groups. Two difference types of P-T path were reconstructed for the North and South Liaohe groups by traditional geothermobaromters estimating. A clockwise P-T-t path was reconstructed for the North Liaohe Group and indicated continental collision tectonic setting. Meanwhile, an anticlockwise P-T-t path was reconstructed for the South Liaohe Group and indicated a magmatic accretion belt in the continental margin (He and Ye, 1998b; Li et al., 2001b; Lu et al., 1996; Zhao et al., 2012). However, Liu et al. (2019) reconstructed a clockwise P-T-t path for granulites of the South Liaohe Group by combination of multi-equilibria geothermobarometers and pseudosection modeling, and suggested a continuous orogenesis from 1950 to 1800 Ma. On the other hand, depositional ages and detritus of metasedimentary rocks from the North and South Liaohe groups also contribute to different tectonic setting and evolutionary history of the JLJB. Luo et al. (2004, 2008) applied the LA-ICP-MS U-Pb zircon dating technique to determine the depositional ages of the North and South Liaohe groups in the period of 2.0 - 1.9 Ga. Moreover they focused on Hf model ages and εHf(t) values, which show striking similarities, supporting the rift model. Wang et al. (2017a) analyzed detrital zircons of the four formations of the South Liaohe Group and obtained different patterns of age spectra, leading to a reasonable analysis of the sedimentary environment.

However, the relationship of chronological and tectonic setting and the interrelation between the North and South Liaohe groups are still discussed controversially. The detrital zircons collected from meta-sedimentary rocks of the North and South Liaohe groups will provide essential objects of the current study. Due to their U-Pb dating and Hf istopic analysis depositional ages and further information related to the general sedimentary setting are expected to be uncovered. The aim of this study is to determine the formation and maximum depositional ages of equivalent formations of the North and South Liaohe groups. By interpreting the similarities and differences of the equivalent formations, this study may provide a more detailed insight into the understanding of the tectonic setting and evolution of the Liaohe Group as a whole as well as the JLJB.

2. Geological background

2.1 Regional geology of the Jiao-Liao-Ji Belt

The Precambrian basement of Eastern Block consists of the Archean Longgang block and the Liaonan-Nangrim block, distinctly separated by the JLJB (e.g. Zhao et al., 2012; Liu et al., 2015). The JLJB extends from the southern Jilin Province across the northern Yellow Sea into the Eastern Shandong Complex; it is up to 1000 km long and 50-300 km wide (Zhao et al., 2001a, 2005; Li et al., 2005, 2006, 2012; Li and Zhao, 2007). This belt is composed of greenschist to lower amphibolite facies sedimentary and volcanic successions, and associated with large-scale granitic and mafic intrusions (Zhao et al., 2005; Li et al., 2005, 2006, 2007; Luo et al., 2004,

2008). It can be subdivided into the Wuhe Group in Anhui province, Fenzishan and Jingshan groups in eastern Shandong, the South and North Liaohe groups in eastern Liaoning, the Ji’an and Laoling groups in southern Jilin and, possibly, the Macheonryeong group in North Korea (Zhao et al., 2005, 2012). In view of their respectively similar nature of lithologies, metamorphic grade and ages, these groups were allocated into a northern and a southern belt. The northern belt is composed of the Fenzishan, North Liaohe and Laoling groups, and the Southern belt consists of the Jingshan, South Liaohe and Ji’an groups (Wang et al., 1997).

2.2 Regional geology of the Liaohe Group

Rocks of the NE-trending Liaohe Group crop out in Haicheng, Dashiqiao and Gaixian in the southwest, through Fengcheng in the central, to Hunjiang in the northeast. This group mainly consists of quartzite, slate, schist, phyllite and marble in the north, as well as graphite-bearing biotite gneiss, sillimanite-garnet biotite gneiss, garnet-staurolite schist and marble in the south. The two groups are separated by faults, which are aligned along the belt that is defined by the towns of Gaixian-Ximucheng-Taziling-Jiangcaodianzi -Aiyang (Wang et al., 2011a). Previous studies have shown that rocks of the North Liaohe Group recorded clockwise P-T paths, whereas rocks of the South Liaohe Group have experienced counterclockwise P-T paths (He and Ye, 1998b). However, recent petrological and geochronological studies of granulites of the South Liaohe and Ji’an groups also document clockwise P-T paths (Cai et al., 2017; Liu et al., 2019). Due to this new establishment of

clockwise P-T paths of granulites from the South Liaohe and Ji’an groups, the tectonic evolution of the JLJB is open to question.

2.3 Stratigraphy and lithologies of the Liaohe Group

The Liaohe Group is subdivided into the North and South Liaohe groups, which represent significant lithostratigraphic units of the JLJB. They consist of sedimentary and volcanic sequences metamorphosed from greenschist to granulitic facies (e.g., Zhang and Yang, 1988; Yang et al., 1988; Wang et al., 1997; Liu et al., 1997; Li et al., 2001b, 2005, 2006, 2007). The North and South Liaohe groups are traditionally subdivided into the Liangzishan, Li’eryu, Gaojiayu, Dashiqiao and Gaixian formations, from lowermost to uppermost. The Langzishan Formation consisting of conglomerate, quartzite, garnet-bearing schist and phyllite, only occurs in the North Liaohe Group and unconformably overlies the late Archean Anshan Complex by a normal fault (Tian et al., 2017). The remaining four formations, from bottom to top, are the Li’eryu and Gaojiayu formations which mainly consist of meta-volcanic rocks, gneiss, garnet- and magnetite-bearing schist, amphibolite, and locally marble, the Dashiqiao Formation that consists of marble, tremolitite, diopsidite, a large magnesite deposit, and occasionally pelitic schists, and finally the Gaixian Formation, which contains meta-sandstone and meta-siltstone (Tian et al., 2017).

3. Description of samples

Detrital zircons separated from meta-sedimentary rocks from the Li’eryu,

Gaojiayu and Dashiqiao formations of the North and South Liaohe Group were chosen for LA-ICP-MS U-Pb and Hf isotopic analyses (Table 1). The samples within the North Liaohe Group include a marble (sample LEY1), three Ms-bearing monzogneisses (sample LEY2, LEY4 and EY6) and two Mag-bearing felsic rocks (sample LEY3 and LEY5) from the Li’eryu Formation, two marbles (sample GJY1 and GJY2) and a slate (sample GJY3) from the Gaojiayu Formation, and four marbles (sample DSQ1, DSQ2, DSQ3 and DSQ4) from the Dashiqiao Formation (Fig. 1a). The South Liaohe Group samples include an Ms-bearing felsic rock (18GJY01) and a Grt-bearing Ms-Bt quartz schist (18GJY03) from the Gaojiayu Formation. Mineral abbreviations are after Whitney and Evans (2010).

3.1 The North Liaohe Group

3.1.1 The Li’eryu Formation

Samples from the Li’eryu Formation for our study were collected from the adjacent areas of Gaojiapuzi village and Helan town (Fig. 1a). Marble (sample LEY1) collected from the western of Helan town is white or light-grey in color, fine-grained, and contains calcite (80-90 vol%), quartz + K-feldspar + phlogopite (5-10 vol%), and accessory zircon + opaque minerals (1-5 vol%) (Fig. 2a). Ms-bearing monzogneiss (samples LEY2, LEY4 and LEY6) was collected from the area adjacent to the Gaojiapuzi Village. The samples are light grey in color, medium- to coarse-grained, and have a gneissic structure defined by muscovite flakes.

They mainly consist of K-feldspar + plagioclase + quartz (60-70 vol%), with muscovite (20-30 vol%), and accessory ilmenite + magnetite + zircon + monazite + apatite (5-10 vol%) (Fig. 2b, d, f). Garnet grains are present in local domains. Mag-bearing felsic rock (samples LEY3 and LEY5) selected for this study are located NE of Gaojiapuzi Village. These samples are grey-colored, medium-grained, and show a massive structure. They have a mineral assemblage of K-feldspar + plagioclase + quartz (80-90 vol%), with magnetite (5-10 vol%), and

accessory

tourmaline + monazite + apatite + zircon (1-5 vol%) (Fig. 2c, e).

3.1.2 The Gaojiayu Formation

There are two marbles and one slate of the Gaojiayu Formation collected adjacent to the Helan town (Fig. 1a). Marble (samples GJY1 and GJY2) occurs as blocks, is white- or grey-colored, fine-grained and massive (Fig. 3a, b). The primary mineral in marble is calcite (80-90 vol%); accessories are quartz (5-10 vol%), zircon + opaque minerals (1-5 vol%) (Fig. 3a, b). Slate (sample GJY3) is grey-black in color, and displays a well preserved porphyroblastic texture. Two generations of plagioclase and quartz are observed. One generation is represented by porphyroblasts and the other by fine-grained intergrowth textures in the matrix. The slate consists of 30-40 vol% plagioclase and quartz and 60-70 vol% aphanitic carbon and sericite (Fig. 3c).

3.1.3 The Dashiqiao Formation

Four samples of marble (sample DSQ1-4) from the Dashiqiao Formation were selected for the geochronology and isotope studies. Marbles are present as blocks and directly in contact with paragneiss or schist. The marble is white-colored, fine- to coarse-grained and massive (Fig. 3g) and locally strongly deformed (Fig. 3f). Three nearly pure marbles (sample DSQ1, DSQ3 and DSQ4) were chosen for the current study which are dominated by calcite (85-95 vol%), with minor quartz (2-5 vol%) or phlogopite (2-5 vol%), accessory zircons + opaque minerals (1-5 vol%) (Fig. 3d). Tremolite-bearing marble (sample DSQ2) mainly consisting of calcite (85-90 vol%) and tremolite (5-10 vol%), with accessory zircons + opaque minerals (1-5 vol%) (Fig. 3e).

3.2 The South Liaohe Group

The typical rocks from the Li’eryu, Gaojiayu, Dashiqiao and Gaixian formations of the South Liaohe Group have been dated by a previous study (Wang et al., 2017a). In order to study in detail the relationship between corresponding formations that occur in both, the North and the South Liaohe groups, two samples from the Gaojiayu Formation of the South Liaohe Group were chosen as supplementary samples in this study (Fig. 3h, 3i; compare section 3.1.2 where the respective samples from the Gaojiayu Formation of the North Liaohe Group are described). These two samples were collected from Xiuyan town (Fig. 1b). The first one, a Ms-bearing felsic rock (sample 18GJY01) is grey-colored, fine-grained and massive (Fig. 3h). Its mineral

composition is dominated by plagioclase + quartz + muscovite (85-90 vol%), with accessory graphite + tourmaline (5-10 vol%) and zircon + monazite + apatite (1-5 vol%). As a second sample, Grt-bearing Ms-Bt quartz schist (sample 18GJY03) was chosen, which is grey in color, fine- to medium-grained, and which shows a gneissic structure (Fig. 3i). It has a mineral assemblage of plagioclase + quartz + muscovite (85-95 vol%), with accessory garnet + magnetite (5-10 vol%) and zircon + monazite + apatite (1-5 vol%).

4. Analytical techniques

Zircon grains were separated using standard heavy-liquid and magnetic techniques followed by hand picking under binocular microscope in the Mineral Separation Laboratory of the Institute of Regional Geological Survey in Langfang, Hebei Province. The selected crystals were mounted onto epoxy resin discs, which were polished to expose the grain centers. Prior to LA-ICP-MS U-Pb zircon dating and Hf isotopic analyses, zircon grains were documented with transmitted light photomicrographs as well as cathodoluminescence (CL) images to reveal their internal structures. All CL images were obtained using a scanning electron microscope (SEM, TESCAN MIRA3 LMH) in Nanjing Hongchuang Exploration Technology Service Co., Ltd. Zircon U-Pb ages were analyzed using LA-ICP-MS at the Nanjing FocuMS Technology Company Limited. Teledyne Cetac Technologies Analyte Excite laser-ablation

system

(Bozeman,

Montana,

USA)

combined

with

Agilent

Technologies 7700x quadrupole ICP-MS (Hachioji, Tokyo, Japan) were used for analyzing. The 193 nm ArF excimer laser was focused on zircon surface with fluence of 6.0J/cm2. Ablation protocol employed a spot diameter of 25 um at 6 Hz repetition rate for 45 seconds. Helium was applied as carrier gas to efficiently transport aerosol to ICP-MS. Zircon 91500 was used as external standard to correct instrumental mass discrimination and elemental fractionation during the ablation process. Zircon GJ-1 was treated as quality control for geochronology. Lead abundance of zircon was externally calibrated against NIST SRM 610 with Si as internal standard, while Zr was used as an internal standard for other trace elements (Liu et al, 2010a; Hu et al., 2011). Every set of seven or eight sample analyses was follow by analysis of the zircon standard 91500 and GJ-1. Quantitative calibration for U-Pb dating was performed by ICPMSDataCal software (Liu et al., 2010a, 2010b). The age calculations together with plotting of Concordia diagrams and age histograms were carried out using Isoplot v. 3.23 (Ludwig 2003). The analytical data are summarized in Supplementary Tables S1-S3 and the errors given for individual analyses are presented within 1 sigma. Zircon Hf isotope analysis was carried out in-situ using a ESI NWR193 laser-ablation microprobe, attached to a Neptune plus multi-collector ICP-MS at Beijing CreaTech Testing International Co., Ltd., Beijing. Instrumental conditions and data acquisition were comprehensively described by Wu et al. (2006) and Hou et al. (2007). A stationary spot was used for the present analyses, with a beam diameter of 40μm depending on the size of ablated domains. Helium was used as carrier gas to

transport the ablated sample from the laser-ablation cell to the ICP-MS torch via a mixing chamber mixed with Argon. In order to correct the isobaric interferences of 176Lu

and 176Yb on 176Hf, 176Lu/175Lu =0.02658 and 176Yb/173Yb =0.796218 ratios

were determined (Chu et al, 2002). For instrumental mass bias correction Yb isotope ratios were normalized to 172Yb/173Yb of 1.35274 (Chu et al, 2002) and Hf isotope ratios to 179Hf/177Hf of 0.7325 using an exponential law. The mass bias behavior of Lu was assumed to follow that of Yb, mass bias correction protocol details were described by Wu et al. (2006) and Hou et al. (2007). Zircon GJ-1 was used as the reference standard during our routine analyses, with a weighted mean 176Hf/177Hf ratio of 0.282007 ± 0.000007 (2σ, n=36). It is not distinguishable from a weighted mean 176Hf/177Hf

ratio of 0.282000 ± 0.000005 (2σ) using the solution analysis method by

Morel et al. (2006). A decayconstant for 176Lu of 1.867 × 10−11a−1(Söderlund et al., 2004), and the present-day chondritic ratios of 176Hf/177Hf = 0.282785 and 176Lu/177Hf = 0.0336 (Bouvier et al., 2008) were adopted to calculate εHf(t) values. Single-stage Hf model ages (TDM1) were calculated by reference to depleted mantle with a present-day176Hf/177Hf ratio of 0.28325 and176Lu/177Hf ratio of 0.0384 (Griffin et al., 2000), and two-stage Hf model ages (TDM2) were calculated by assuming a mean 176Lu/177Hf

value of 0.015 (Griffin et al., 2002) for the average continental crust.

5. Zircon cathodoluminescent imaging and U-Pb ages

5.1 The North Liaohe Group

5.1.1 The Li’eryu Formaion

Zircon grains separated from six samples from the Li’eryu Formation (North Liaohe Group) including a marble, three Ms-bearing monzogneisses and two Mag-bearing felsic rocks show similar characteristics. The grains are transparent, subhedral, elongated to stubby, with grain lengths mainly of 50-200 μm and length-width ratios of 3:1 to 2:1. Based on the CL images (Fig. 4), two types of zircon domains can be distinguished, which include detrital cores and metamorphic rims. Furthermore, the detrital zircon cores can be subdivided into two groups. One group is characterized by grey-white or dark- luminescence, showing strongly or weakly oscillatory zoning which is typical for magmatic origin. The other group is homogeneous and grey-white or dark- luminescent; parts of the detrital zircon cores are surrounded by narrow grey or dark unzoned rims. U-Pb analyses of 676 detrital zircon cores from the Li’eryu Formation of the North Liaohe Group have Th/U ratios varying from 0.17 to 1.78 (expect for one spot of LEY4-100, Supplementary Table S1). The detrital cores from samples LEY1 to LEY6 yield

207Pb/206Pb

ages which scatter between 2546 ± 26 and 2079 ± 22 Ma,

2229 ± 23 and 2020 ± 22 Ma, 2256 ± 25 and 2010 ± 20 Ma, 2521 ± 17 and 2106 ± 25 Ma, 2314 ± 19 and 2103 ± 20 Ma, 2465 ± 25 and 2098 ± 27 Ma, respectively, and with pronounced unimodal age peaks at ~ 2165 Ma, ~ 2184 Ma, ~ 2180 Ma, ~ 2175

Ma, ~ 2178 Ma and ~ 2168 Ma (Fig. 6a-f). In contrast, one U-Pb analysis of a metamorphic rim of a zircon separated from sample LEY1 (marble) and eight of zircons from sample LEY2 (Ms-bearing monzogneiss) yield Th/U ratios from 0.01 to 0.05 (Supplementary Table S1); the resulting 207Pb/206Pb ages vary from 1973 ± 23 Ma to 1814 ± 20 Ma.

5.1.2 The Gaojiayu Formation

Zircon grains selected from two marbles (sample GJY1 and GJY2) and one slate (sample GJY3) of the Gaojiayu Formation are transparent, subhedral, stubby or elongated, with grain lengths mainly of 30-100 μm and length-width ratios of 3:1 to 1:1. In general, the zircon crystals from these lithological types are anhedral to subhedral (Fig. 5a-c). Most of the zircon grains have extremely narrow recrystallized rims or overgrowth domains. All detrital zircon cores are light- or dark-grey luminescent, and display a distinctly or weakly oscillatory zoning or are homogeneous. LA-ICP-MS U-Pb data of 175 detrital zircon cores from two marbles (samples GJY1 and GJY2) have Th/U ratios of 0.25-1.69 (Supplementary Table S2). These analytical spots yield variably discordant U-Pb ages from 2627 ± 22 to 2102 ± 23 Ma and 2584 ± 22 to 2113 ± 29 Ma, respectively. The

207Pb/206Pb

age histogram of

sample GYJ1 shows a primary peak at ~ 2175 Ma, with a subordinate peak at ~ 2520 Ma (Fig. 7a). Additionally, in the

207Pb/206Pb

age spectrum of sample GJY2, the

detrital zircons display a remarkable age peak at ~ 2518 Ma, as well as a minor age

peak at ~2175 Ma (Fig. 7b). Similarly, 95 detrital zircons of slate (sample GJY3) yield Th/U ratio of 0.02-1.66 (Supplementary Table S2). The 207Pb/206Pb ages of these detrital zircons scatter between 2657 ± 24 Ma and 2096 ± 24 Ma (expect for the two oldest ages of 3637 ± 17 Ma and 3000 ± 21 Ma). In addition, a striking age peak at ~ 2510 Ma with a minor peak at ~ 2185 Ma (Fig. 7c) was obtained. The homogeneously luminescent detrital cores and the oscillatory detrital cores are similar in age (~2.6 – 2.1 Ga).

5.1.3 The Dashiqiao Formation

Zircon grains selected from four typical samples of marble (samples DSQ1-4) are subhedral to anhedral, oval to stubby, and exhibit lengths and length-width ratios mainly of 50-100 μm and 3:1-1:1, respectively. Under CL, most zircon grains have irregular detrital cores and dark unzoned recrystallized rims (Fig. 5d-g). The detrital zircon cores are characterized by light- or dark-grey luminescence. Some of them display a distinctly or weakly oscillatory zoning, others are homogeneous. U-Pb analyses of detrital zircons or zircon cores of marbles from the Dashiqiao Formation have Th/U ratios of 0.52-0.93 (Supplementary Table S3). Most of them yield concordant

207Pb/206Pb

ages ranging from 2709 ± 15 to 2028 ± 21 Ma (expect

for the three oldest ages of 3587 ± 18 to 2903 ± 23 Ma). The 207Pb/206Pb age spectrum display bimodal peaks at ~ 2190 Ma and ~ 2508 Ma, ~ 2185 Ma and~ 2515 Ma, ~ 2175 Ma and ~ 2510 Ma, ~ 2170 Ma and ~ 2455 Ma, respectively (Fig. 7d-g).

5.2 The South Liaohe Group

Zircon grains from the Gaojiayu Formation (samples 18GJY01 and 18GJY03) are subhedral to anhedral, stubby to prismatic, and yield lengths of 50-100 μm and length-width ratios of 3:1-3:2, respectively (Fig. 5h-i). They show detrital cores which are light- or dark-grey luminescent, and display a distinctly or weakly concentric or sector zoning. A small number of zircon grains are featureless and display only a faint luminescence. The CL images document that most detrital grains have dark- or grey-colored, narrow recrystallized rims or overgrowth domains. LA-ICP-MS U-Pb data of 118 detrital zircon grains or cores from Ms-bearing felsic rock (sample 18GJY01) yielded variable Th/U ratios of 0.14-3.16 (Supplementary Table S4). These types of zircon or zircon domains show variable 207Pb/206Pb

ages of 2928 ± 18 to 2039 ±19 Ma, with an evident age peak of 2500 Ma

in the 207Pb/206Pb age spectrum (Fig. 7h). 107 spots have been analyzed on detrital zircon grains or domains of Grt-bearing Ms-Bt quartz schist (sample 18GJY03). These spots have variable Th/U ratios of 0.22-2.28 (Supplementary Table S4). All these U-Pb studies yielded

207Pb/206Pb

ages

between 3592 ± 15 and 1994 ± 24 Ma, and show a prominent age peak at 2165 Ma in the 207Pb/206Pb age spectrum (Fig. 7i).

6. Zircon Hf isotopic results

The zircon Lu-Hf isotopic analyses can provide crust formation ages for the igneous source rocks, for the reason that the Lu-Hf isotope systematics may not be

affected by later tectonothermal events (Kinny et al., 1991, 2003; Stevenson et al., 1990; Hoskin et al., 2003; Yang et al., 2006). Based on the analytical results of zircon U-Pb dating, those grains with concordant or nearly concordant 207Pb/206Pb ages from the Li’eryu, Gaojiayu and Dashiqiao formations within both the North and South Liaohe Group were selected for Lu-Hf isotopic analyses. While the U-Pb dating results of Li’eryu (sample SJZ09-1, SJZ14-1 and SJZ18-2), Gaojiayu (sample SJZ22-3) and Dashiqiao (sample SJZ25-1 and SJZ46-1) formations of the South Liaohe Group have been published (Wang et al., 2017a), in the framework of the current paper equivalent data from the North Liaohe Group have been performed. All data are visualized in Figs. 8-10 and the respective values are listed in Supplementary Tables S5-S10.

6.1 The North Liaohe Group

Detrital zircon grains or cores from six typical samples of the Li’eryu Formation yield 207Pb/206Pb ages that gather between 2546 ± 26 and 2010 ± 20 Ma, and display a striking unimodal age peak at ~ 2176 Ma (Fig. 10e). One hundred and fifty-five zircon grains with

207Pb/206Pb

ages of 2256-2100 Ma possess εHf(t) values that range

from -2.78 to 5.23, and TDM2 model ages of 2898-2434 Ma (Supplementary Table S5, Fig. 8e, 9e). Detrital zircon grains or cores from three samples of the Gaojiayu Formation show evident bimodal 207Pb/206Pb age peaks at ~ 2513 Ma and ~ 2175 Ma (Fig. 10c). Lu-Hf isotopic analysis was performed on 126 selected detrital zircon grains or cores, whose

207Pb/206Pb

ages were located close to the two age peaks shown in Fig. 10c. The

207Pb/206Pb

ages on these zircon fractions scatter between 2627 and 2461 Ma, the

respective εHf(t) values range from 1.65 to 7.77 (expect for one grain with a εHf(t) value of -0.02), and the TDM2 model ages are between 2977 and 2547 Ma (Supplementary Table S6, Fig. 8c, 9c). Detrital zircon grains or cores with 207Pb/206Pb ages of 2269-2096 Ma, had εHf(t) values ranging from -2.90 to 5.92, and TDM2 model ages of 2896-2328 Ma (Supplementary Table S6, Fig. 8b, 9b). Also, the detrital zircon grains or cores from four samples of the Dashiqiao Formation display two

207Pb/206Pb

age peaks; they are located at ~ 2510 Ma and ~

2180 Ma (Fig. 10a). One hundred and forty-two detrital zircon grains or cores, whose 207Pb/206Pb

ages were located close to the two age peaks, were selected for Lu-Hf

isotopic analysis. The results of Lu-Hf isotopic analysis show that εHf(t) values and TDM2 model ages also gather around two groups, respectively (Supplementary Table S7, Fig. 8a, 9a). Zircon grains or cores with 207Pb/206Pb age peak at ~ 2180 Ma yield εHf(t) values and TDM2 model ages that range from -3.53 to 9.41 and 2820 to 2543 Ma, respectively. The other zircon grains or cores with 207Pb/206Pb age peak at ~ 2510 Ma yield εHf(t) values range from -2.54 to 8.87, and TDM2 model ages from 3131 to 2427 Ma.

6.2 The South Liaohe Group

In a similar way compared to the results on detrital zircon from the North Liaohe Group, 456 detrital zircon grains or cores from the Li’eryu Formation of the South

Liaohe Group, display an evident unimodal age peak at 2130 Ma in the

207Pb/206Pb

age spectrum (Fig. 10f; after Wang et al., 2017a). Eighty-three spots on zircon from three typical samples (SJZ09-1, SJZ14-1 and SJZ18-2) were analyzed for Lu-Hf isotopes (Supplementary Table S8). These spots yield εHf(t) values ranging between -2.68 and 3.67, and TDM2 model ages of 2861-2467 Ma (Fig. 8f, 9f). All these data gathered around in one specific age group as shown in Fig. 10f. In the

207Pb/206Pb

age spectrum, 332 detrital zircon grains or cores from the

Gaojiayu Formation show a bimodal distribution with age peaks at ~ 2500 Ma and ~ 2170 Ma (Fig. 10d; after Wang et al., 2017a and this study). Among them, 124 spots on zircon were chosen for Lu-Hf isotopic analyses. The data gathered around in two groups. The detrital zircon grains or cores with

207Pb/206Pb

ages of 2592-2426 Ma

yield εHf(t) values between -7.07 and 7.16, and TDM2 model ages of 3437-2590 Ma (Supplementary Table S9, Fig. 8d, 9d). On the other hand, zircon grains or cores with 207Pb/206Pb

ages in the range of 2211-2065 Ma yield εHf(t) values and TDM2 model

ages ranging from -5.42 to 6.73 and 3079 to 2347 Ma (Supplementary Table S9, Fig. 8d, 9d). On 125 detrital zircon grains or cores from the Dashiqiao Formation two main 207Pb/206Pb

age groups can be distinguished with peaks at ~ 2500 Ma and ~ 2160 Ma

(Fig. 10b; after Wang et al., 2017a). Seventy-three analytical spots on zircon domains near the two age peaks were selected for Lu-Hf isotopic analyses. The detrital zircon grains or cores with

207Pb/206Pb

ages of 2533-2422 Ma yield positive εHf(t) values

ranging from 0.06 to 10.13 (expect for one grain with εHf(t) value of -1.72), and TDM2

model ages of 2976-2367 Ma (Supplementary Table S10, Fig. 8b, 9b). On the other hand, the spots on zircon which result in 207Pb/206Pb ages between 2228 and 2028 Ma gave εHf(t) values of -3.69 to 6.24, and TDM2 model ages of 2878-2340 Ma (Supplementary Table S10, Fig. 8b, 9b).

7. Discussion

The U-Pb dating results of detrital and metamorphic zircons from the South Liaohe Group in Sanjiazi area have been published in Wang et al. (2017a). Igneous zircon cores of detrital zircons of the Li’eryu, Gaojiayu, Dashiqiao and Gaixian formations yield U-Pb age peaks at ~ 2130 Ma, ~ 2520 Ma, ~ 2160 Ma/~2500 Ma, and ~ 2040 Ma. In this study, two meta-sedimentary rocks of the Gaojiayu Formation, the South Liaohe Group in Xiuyan town were collected for zircon U-Pb dating and Hf isotopic analyses. Detrital zircons from two samples yield U-Pb age peaks at ~ 2500 Ma and ~ 2165 Ma, respectively. Previous geochronological studies suggest that the respective melts of the pre-tectonic (gneissic) and post-tectonic (porphyritic) Liaoji granitoids were mainly emplaced at 2.17-2.14 Ga (Lu et al., 2004b; Li et al., 2007) and 1.87-1.84 Ga (Li et al., 2007; Liu et al., 2017), respectively. All these dating results indicate that the Longgang and Liaonan-Nangrim blocks basement rocks and the Liaoji granitoids contributed detritus to the Gaojiayu and Dashiqiao formations. However, the detrital zircons of the Li’eryu Formation from the South Liaohe Group yield one single age peak, indicating that its main source is the Liaoji granitoids. In this paper, depositional age and mineral source of the North Liaohe Group, as well as

the tectonic significane will be discussed in detail as follows.

7.1. Depositional age of the North Liaohe Group

Abundant zircon U-Pb dating results have been reported to constrain the depositional age of meta-sedimentary rocks from the North and South Liaohe groups (Luo et al., 2004, 2008; Liu et al., 2015; Wang et al., 2017a; Liu et al., 2018). Based on the ages gathered from metamorphic and inherited zircons, the protoliths of the Liaohe groups were deposited in the time period 2.0-1.9 Ga (Luo et al., 2004, 2008; Zhao et al., 2012; Liu et al., 2018). Furthermore, the youngest age obtained by a “group” of detrital zircons (2.15-2.05 Ga), combined with the oldest metamorphic age (~ 1.95 Ga), suggested the depositional age of the North and South Liaohe groups between 2.05 and 1.95 Ga (Liu et al., 2015). Recently Wang et al. (2017a) reported maximum depositional ages of the Li’eryu, Gaojiayu, Dashiqiao and Gaixian formations from the South Liaohe Group documented by the representative youngest individual zircon U-Pb ages of 2050 Ma, 2069 Ma, 2043 Ma and 1915 Ma, respectively. Most recently, two metamorphosed sandstones from the Gaixian Formation of the South Liaohe Group in Huanghuadian-Suzigou area yielded completely different age peaks by LA-ICP-MS detrital zircon U-Pb dating (Wang et al., 2018). A metamorphosed quartz sandstone yielded age peak at 2150 Ma and suggested its primary sediments sourced from ca. 2.2-2.1 Ga monzogranitic gneisses. A metamorphosed feldspathic quartz sandstone yielded two age peaks at 2178 and 1863 Ma, suggesting its source originated from ca. 2.2-2.1 Ga monzogranitic gneisses

and ca. 1.9-1.8 Ga porphyritic monzogranites, respectively. The new dating results of metamorphosed feldspathic quartz sandstone with age peaks of 2178 and 1863 Ma constrained its depositional time after ~ 1.86 Ga (Wang et al., 2018). It is remarkable that detrital zircons from different lithologies of the Gaixian Formation in different areas documented heterogeneous ages and thus further dating works imminently required (Wang et al., 2017a; Wang et al., 2018). Recently, abundant detrital zircon ages from the South Liaohe Group have been reported (e.g. Wang et al., 2017a, 2018; Liu et al., 2018). However, the precise depositional age of the North Liaohe Group is still under debate. In this study, more than thirteen hundred analytical spots on detrital zircon grains separated from the Li’eryu, Gaojiayu and Dashiqiao formations of the North Liaohe Group were analyzed by LA-ICP-MS U-Pb dating technique. Age data of detrital zircons of the Li’eryu Formation from the North Liaohe Group, coupled with those from the South Liaohe Group, give an unimodal age peak of ~ 2176 Ma (Fig. 10e-f). Detrital zircons from Gaojiayu and Dashiqiao formations of the North Liaohe Group display bimodal age peaks at ~ 2513 and ~ 2175 Ma, ~ 2510 and ~ 2180 Ma, respectively (Fig. 10a, 10c). Moreover, recent geochronological studies of the Langzishan Formation, the lowermost sedimentary unit of the North Liaohe Group, suggested that a depositional age of ca. 2205-2170 Ma (Xu et al., 2019a). In view of all these dating results, the consistent youngest age peak at ~ 2.13 Ga was regarded to represent the maximum depositional age of the North Liaohe Group. The Paleoproterozoic meta-mafic rocks from the Liaonan area are mainly exposed

in the North Liaohe Group, whereas only small volumes are exposed in the South Liaohe Group (Liu et al., 2017a; Xu et al., 2018a). The meta-mafic rocks, which are widely distributed in the Liaohe Group, and thus their respective melt precursors that intruded rocks of the Liaohe Group also provide important information about the depositional time. Previous studies on zircons or baddeleyites separated form mafic rocks from the North Liaohe Group constrained an emplacement ages of ~ 2.1 Ga (Meng et al., 2014; Yuan et al., 2015). Combined with age data from meta-mafic rocks intrusive in the sedimentary sequence of the North and South Liaohe groups, the new geochronological data of this paper indicate a maximum depositional age of ~ 2.13 Ga for the Li’eryu, Gaojiayu and Dashiqiao formations.

7.2. Provenance studies of the North Liaohe Group

Provenance studies can gain a lot from U-Pb dating of detrital zircons (Fedo et al., 2003). In addition, Hf isotope compositions of zircon play a significant role tracing the source of host rock (Kinny et al., 2003). In this study, 1330 detrital zircon grains or cores form the meta-sedimentary rocks were analyzed which yielded reliable age. These dating results show an age range from 3637 to 2010 Ma, with two major age peaks of ca. 2.2-2.1 and 2.5 Ga (Fig. 10). In order to trace the mineral sources of the protolith, the U-Pb zircon ages and Hf isotopic signatures of different formations of the North and South Liaohe groups are in compared with respective data of the adjacent complexes (including the Longgang and Liaonan-Nangrim blocks, as well as

the Liaoji granitoids). (1) Previous studies have revealed that ~ 2.5 Ga magmatism is widespread in the Longgang block, and abundant rocks and zircon grains of > 2.5 Ga have been identified (e.g. Liu et al., 1992; Song et al., 1996; Wan et al., 2001, 2005, 2012, 2015; Wu et al., 2008; Liu et al., 2017b). The majority of Archean to Paleproterozoic zircons have positive εHf(t) values, with two-stage model ages of ~ 2.7 Ga (Geng et al., 2012). In contrast, a small amount of zircons have negative εHf(t) values, e.g., the ~ 2.5 Ga zircons with TDM2 model ages of 3.72-2.70 Ga of granites and granitoids collected from the Anshan-Benxi area (Wan et al., 2015) and the trondhjemitic gneiss from the Caozhuang area with ca. 2.9 Ga old zircons with TDM2 model ages of 3.54-3.32 Ga (Fu et al., 2019). Apparently, most zircons of the Longgang block ≥2.5 Ga have positive εHf(t) values, except for those from the Anshan-Benxi area. (2) It has been confirmed that multiple Meso-to Neoarchean magmatic events took place in the Liaonan terrane, at ca. 2.84, 2.75, 2.67-2.61, 2.54 and 2.51 Ga (Meng et al., 2013). The zircons with ages of ca. 2.54 and 2.51 Ga, mostly have positive εHf(t) values (+0.13 to +8.57) and TDM2 model ages of 3.06-2.53 Ga (Meng et al., 2013). Additionally, the 2.52 Ga Neoarchean assemblages (including mafic rocks, diorites and TTGs), together with 2.50 Ga granites, are preserved in the Liaonan terrane (Wang et al., 2017b). On the other hand, on the basis of detrital zircon U-Pb and Lu-Hf isotope data obtained from sands in three rivers (the Taedong, Chongchon and Songchon Rivers in North Korea), it is documented that the Nangrim block is mostly composed of 1.9-1.8 Ga rocks, with a little component of Archean material, which is

in marked contrast to the nearby North China Craton (Wu et al., 2007, 2016). In view of these geochronological results, Wu et al. (2016) proposed that the Nangrim block is not an Archean massif, but of Paleoproterozoic age like that of the Liaoji belt, even though Archean magmatic events (e.g. at 2.57 to 2.51 Ga) in the Nangrim block indeed exist (Zhao et al., 2016). By contrast, to date, there’s only little evidence to ages prior to 2.8 Ga in the Nangrim block and the Liaonan terrane (Meng et al., 2013; Wang et al., 2017b). Therefore, it is suggested that detrital zircons of ages prior to 2.8 Ga might be derived from the adjacent Longgang Block. (3) The 2.2-2.1 Ga monzogranitic gneisses (the Liaoji granitoids) are in tectonic contact with the North and South Liaohe groups (e.g., Lu et al., 2004a; Li et al., 2017b). However, these monzogranitic gneisses were initially defined to be S-type granites (Liu et al., 1989; Zhao and Hu, 1989), later considered as A-type (Lu et al., 2004b) and A2-type granites (Li et al., 2017b), or I-type granites (Yang et al., 2015, 2016). Most recently, 590 reliable U-Pb crystallization ages from the Liaoji granitoids were performed by Xu et al. (2019c) and yielded U-Pb ages concentrating between 2190 and 2160 Ma with an age peak at ~ 2180 Ma. Although the petrogenesis of monzogranitic gneisses, and the spatial and chronological interrelation between the Liaoji granitoids and the North and South Liaohe groups are still under debate, the zircon group representing the age population of 2.2-2.1 Ga of the North and South Liaohe groups is considered to be equivalent to the group of the monzogranitic gneisses (the Liaoji granitoids) (Lu et al., 2004a; Luo et al., 2004, 2008; Li et al., 2015a, b; Wang et al., 2017a; Liu et al., 2018).

In summary, the detrital zircons from Li’eryu Formation of the North Liaohe Group with one dominating age peak at ca. 2.2-2.1 Ga, most possibly sourced from the Liaoji granitoids. On the other hand, two remarkable age populations of ca. 2.5 Ga and 2.2-2.1 Ga, as well as several minor older ones, characterize the detrital zircons from the Gaojiayu and Dashiqiao formations, and suggest heterogeneous and complex sources. Similarly, ages of 2.2-2.1 Ga corresponds to crystallization ages of the Liaoji granitoids. However, the ~ 2.5 Ga detrital zircons probably originate from the basement rocks of the adjacent block (the Longgang and Liaonan-Nangrim blocks). Notably, the ~ 2.5 Ga detrital zircons with negative εHf(t) values likely derived from Anshan-Benxi area in the Longgang block. As mentioned earlier, abundant rocks and zircon grains of > 2.5 Ga have been identified in the Longgang block. The detrital zircons prior to 2.5 Ga, especially those prior to 2.8 Ga, logically sourced from the Longgang block basement rocks.

7.3. Constraints on the tectonic setting of the North and South Liaohe groups

As mentioned in introduction section, the tectonic setting and evolution of the Jiao-Liao-Ji belt is still discussed controversially. To solve these debates, in this study, we focused on the relationship of depositional spatial and chronological distribution between the South and North Liaohe groups. Combined with pervious geochronological data, the age populations and zircon Hf isotope compositions of corresponding formations from the North and South Liaohe groups are similar (Fig. 10). The age patterns of detrital zircons from the Li’eryu Formation of two Liaohe

groups are in strict conformity and display unimodal age peaks. Cawood et al. (2012) proposed that detrital zircon ages could provide constrains on the original basin setting. The cumulative proportion vs. 207Pb/206Pb age diagram (Fig. 11) indicates that meta-sedimentary rocks from the Li’eryu Formation formed in a convergent basin. These meta-sedimentary rocks have unimodal detrital zircon spectra with ages close to the depositional ages, the age patterns further point to a formation in a back arc basin (Cawood et al., 2012). However, the TDM2(Ma) model ages of the relative probability plots of zircon from the Gaojiayu Formation of the North and South Liaohe groups are different (Fig. 8c, d); the zircon Hf isotope compositions of the Gaojiayu Formation from the South Liaohe Group however are similar to those of the North Liaohe Group, but document a broader distribution (Fig. 9c-d). Almost all ~ 2.5 Ga zircons from the Gaojiayu Formation of the North Liaohe Group have positive εHf(t) values, and their TDM2 ages concentrated between 2977 and 2547 Ma. By contrast, contemporary zircons from the same formation of the South Liaohe Group partly have negative εHf(t) values and more older TDM2 ages (TDM2 ages = 3437-2509 Ma), indicating Anshan-Benxi area derived material (Wan et al., 2015). Despite slight distinction existing, detrital zircons from the Gaojiayu and Dashiqiao formations of both the North and South groups, have two identical age peaks (Fig.10a-d), which suggest mixed origin of the adjacent basement rocks and Liaoji granitoids. Their younger age peaks are closer to the depositional age, and these age patterns are consistent with a collisional basin setting (Fig. 11). On the basis of previous studies, the lowermost Langzishan Formation mainly sourced from basement rocks in the

Longgang block (e.g., the Anshan-Benxi area), and is deposited between 2205 and 2170 Ma in passive continental margin setting (Xu et al., 2019a). The uppermost Gaixian Formation contains heterogeneous rock sources. A part of the meta-sedimentary rocks shows significantly different age peak at ~ 1.86 Ga, and indicates to be different from the North and South Liaohe groups (Wang et al., 2018). Whereas, detrital zircons separated from the Gaixian Formation of the South Liaohe Group, which show an age peak at ~ 2040 Ma (data from Wang et al., 2017a), indicate that their rocks originate from younger arc magma (Xu et al., 2019c; and reference therein). In summary, it seems reasonable to settle the rocks of the North and South Liaohe Group (except those of the Langzishan Formation) in a tectonic setting of a back arc basin. In view of our new data on zircon U-Pb ages and Hf isotope composition, the provenance and depositional setting of the North and South Liaohe Group can now be reconstrained. Considering in addition the geochronological data as well as the provenance and depositional results of the Langzishan and Gaixian formations of Xu et al. (2019a) and Wang et al (2017), respectively, the formation scenario of the North and South Liaohe groups is as follows (Fig. 12): (a) In the period of ca. 2205 to 2170 Ma, the protolith of the Langzishan Formation deposited its detritus in an extensional basin, a passive continental margin. Subsequently between ca. 2205 Ma and 2170 Ma, the tectonic setting transformed from a passive continental margin into an active continental margin (Xu et al., 2019a, Fig. 12a).

(b) Since ~ 2130 Ma, the

monzogranitic gneisses (the Liaoji granitoids) were weathered, and provided the

source material to form the Li’eryu Formation of the North and South Liaohe groups (Fig. 12b). (c) Contemporaneously, detritus from the Longgang and Liaonan blocks basement rocks and the Liaoji granitoids was transported and deposited forming the Gaojiayu and Dashiqiao formations of the North and South Liaohe groups. (d) Younger granites and basement rocks from the Longgang block constituted the protoliths of the traditionally considered Gaixian Formation, and later superimposed by rocks of the Dashiqiao Formation. Therefore, the protolith of the North and South Liaohe Group was deposited in the back arc basin (Fig. 12c). (e) In the period of 1.95 to 1.85 Ga, the collisional orogeny between the Longgang and Liaonan-Nangrim blocks occurred, and meta-sedimentary rocks form both northern and southern belt experienced upper amphibolite- to granulite-facies metamorphism with clockwise P-T-t paths (eg. Tam et al., 2012a, 2012b; Liu et al., 2017a, 2019; Chen et al., 2018; Li et al., 2018). The final event that indicates the termination of the orogenic cycle refers to the 1.88 ~ 1.85 Ga post-tectonic magmatic intrusions forming porphyritic monzogranite, granite and alkaline syenite (Hao et al., 2004; Lu et al., 2004a; Fig. 12d).

7. Conclusions

(1) In the North Liaohe Group, the detrital zircons from the Li’eryu Formation yield an unimodal

207Pb/206Pb

age peak of ~ 2176 Ma, and are interpreted to source

from the Liaoji granitoids. The detrital zircons from the Gaojiayu and Dashiqiao formations yield

207Pb/206Pb

age peaks at ~2513 and ~2175 Ma and at ~2510 and

~2180 Ma, respectively, and the main sources to their protoliths were the basement rocks from the Longgang and Liaonan-Nangrim blocks, as well as the Liaoji granitoids. (2) The detrital zircons from the corresponding formations of the North and South Liaohe groups have similar Hf isotopic compositions, some minor differences solely exist in the Gaojiayu Formation. Almost all detrital zircons of ~ 2.5 Ga from the Gaojiayu Formation of the North Liaohe Group have positive εHf(t) values, and their TDM2 ages concentrated between 2896 and 2325 Ma. These zircons probably originate from the basement rocks of the Longgang and Liaonan-Nangrim blocks. However, zircons from the Gaojiayu Formation of the South Liaohe Group partly have negative εHf(t) values and TDM2 ages ranging from 3437 to 2590 Ma, which possibly derive from Anshan-Benxi area in the Longgang block. (3) The protoliths of corresponding formations of the North and South Liaohe groups contemporaneously deposited clastic material into back-arc basin. The Liaoji granitoids provided the source materials for the Li’eryu Formation. Subsequently, sediments transported from the Longgang and Liaonan blocks as well as from the Liaoji granitoids were deposited, and formed the Gaojiayu and Dashiqiao formations.

Acknowledgements

We thank for the editor and reviewers for their careful reviews and constructive comments that significantly improved the quality of this paper. We thank Dr. Lei Ji, and Lishuang Liu for their helpful assistance during field work. We also thank Liang

Li for laboratory assistance. This research was funded by National Natural Science Foundation of China (Grant nos. 41430210, 41890833), the China Geological Survey Bureau project (Grant no. DD20160121).

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Research Highlights

► Rocks of North and South Liaohe Groups show similar detrital zircon age patterns ►Rocks of North and South Liaohe Groups have similar Hf isotope compositions ► Liaoji Grantiods and adjacent Archean basement serve as source for the Liaohe Groups ► Back-arc basin deposition occurred for corresponding formations of the Liaohe

Groups

Conflict of interest We declare that we do not have any commercial or associative interest that represents a conflict of interest in connection with the work submitted.

Group

the North Liaohe Group

the South Liaohe Group

Formtion

Sample DSQ1 DSQ2 the Dashiqiao Formation DSQ3 DSQ4 GJY1 GJY2 the Gaojiayu Formation GJY3 LEY1 LEY2 LEY3 the Li'eryu Formation LEY4 LEY5 LEY6 18GJY01 the Gaojiayu Formation 18GJY03

Rock type marble marble marble marble marble marble slate marble Ms-bearing monzogneiss Mag-bearing felsic rock Ms-bearing monzogneiss Mag-bearing felsic rock Ms-bearing monzogneiss Ms-bearing felsic rock Grt-bearing Ms-Bt quartz schist