Petrogenesis and tectonic implications of two types of Liaoji granitoid in the Jiao–Liao–Ji Belt, North China Craton

Precambrian Research 331 (2019) 105369

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Petrogenesis and tectonic implications of two types of Liaoji granitoid in the Jiao–Liao–Ji Belt, North China Craton

T

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Kai Zhua, Zhenghong Liub, , Zhongyuan Xub, Xing'an Wangc, Weilong Cuib, Yujie Haob,d a

College of Geo-exploration Science and Technology, Jilin University, Changchun 130061, China College of Earth Sciences, Jilin University, Changchun 130061, China c College of Geographical Sciences, Northeast Normal University, Changchun 130024, China d Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of Natural Resources of China, Changchun 130026, Jilin, China b

A R T I C LE I N FO

A B S T R A C T

Keywords: Paleoproterozoic Liaoji granitoids Jiao–Liao–Ji Belt A2-subtype granitoids Adakitic rocks Arc–continent collision model

Two types of granitoid (monzogranite and granodiorite) are recognized within the Paleoproterozoic Liaoji granitoids of the Jiao–Liao–Ji Belt (JLJB) in the Hupiyu and Simenzi areas, North China Craton. We conducted zircon U–Pb geochronological, geochemical, and Hf isotopic analyses of these granitoids. Zircon U–Pb dating indicates an emplacement age of 2180 ± 14 Ma for the monzogranite (Hupiyu granitoids) and ages of 2130 ± 24 and 2173 ± 11 Ma for the Fangjiaweizi and Dadingzi granodiorites at Simenzi, respectively. The Hupiyu monzogranite samples are enriched in Zr, Ga, and Y, and depleted in Nb and Ti. Low Nb/Y ratios and high Zr saturation temperatures (849–884 °C) indicate that the Hupiyu monzogranites have an affinity with A2subtype granitoids. The Fangjiaweizi and Dadingzi granodiorites have high Sr/Y and low K2O/Na2O ratios, indicating an affinity with adakitic rocks. Geochemical compositions and wide variation in εHf(t) values suggest that the monzogranites and granodiorites were derived from thinned and thickened lower crust, respectively, and that magmatism was accompanied by input of mantle material. This study represents the first identification of pre-tectonic adakitic rocks in the JLJB. The assemblage of pre-tectonic A2-type granitoids and adakitic rocks indicates a continental back-arc basin as the initial tectonic setting of the JLJB. These new data, combined with results of previous studies, support an arc–continent collision model for the JLJB.

1. Introduction The North China Craton (NCC) is one of the oldest cratons on Earth (Liu et al., 1992; Wan et al., 2005, 2012). On the basis of lithological, structural, metamorphic, and geochronological investigations, the NCC can be divided into four micro-continental blocks: the Yinshan and Ordos blocks in the west and the Longgang and Rangnim blocks in the east (Fig. 1). Three Paleoproterozoic mobile belts, namely, the Khondalite Belt, Trans-North China Orogen, and Jiao–Liao–Ji Belt (JLJB), have been recognized as separating the four micro-continental blocks (Zhao et al., 1998, 1999, 2000, 2001, 2002, 2005, 2012). The Khondalite Belt resulted from collision between the Yinshan and Ordos blocks, forming the Western Block at ∼1.95 Ga (Zhao et al., 2005, 2012; Wan et al., 2006; Xia et al., 2006a,b), whereas the Trans-North China Orogen formed by amalgamation of the Western and Eastern blocks at ∼1.85 Ga (Zhao et al., 2001, 2005, 2012). However, the tectonic nature and evolution of the JLJB are still disputed (Zhang and Yang, 1988; Bai, 1993; Lu et al., 2006; Wang et al., 2015).

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The JLJB is situated between the Longgang and Liaonan–Rangnim blocks (Fig. 2). It formed at 2.2–1.8 Ga and has undergone a complex tectonic evolution involving simultaneous and multi-stage magmatism and metamorphism (Zhang and Yang, 1988; He and Ye, 1998; Hao et al., 2004; Lu et al., 2005, 2006; Li and Zhao, 2007; Zhao et al., 2012; Li and Chen, 2014, 2016; Li et al., 2015a,b, 2016, 2017, 2019; Liu et al., 2015; Wang et al., 2015; Yang et al., 2015; Song et al., 2016; Ren et al., 2017; Liu et al., 2018). Various models have been proposed to describe the evolution of this belt. Although there is broad consensus that the JLJB underwent an orogenic event at ∼1.9 Ga, its initial tectonic setting remains uncertain. The debate centres on whether the JLJB was a rift (Zhang and Yang, 1988; Li et al., 2004a,b, 2005, 2006, 2012; Luo et al., 2004, 2008; Li and Zhao, 2007; Zhao et al., 2012; Wang et al., 2017c; Liu et al., 2018) or an arc–continent collisional belt (Bai, 1993; Faure et al., 2004; Li and Chen, 2014, 2016; Meng et al., 2014, 2017a,b,c; Li et al., 2015a,b, 2016, 2017; Wang et al., 2015, 2017a; Yuan et al., 2015). The presence of bimodal volcanics (Zhang and Yang, 1988), the low pressure and anticlockwise metamorphic P–T–t paths of

Corresponding author. E-mail address: [email protected] (Z. Liu).

https://doi.org/10.1016/j.precamres.2019.105369 Received 9 June 2018; Received in revised form 4 June 2019; Accepted 11 June 2019 Available online 12 June 2019 0301-9268/ © 2019 Elsevier B.V. All rights reserved.

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Fig. 1. Tectonic subdivision of the North China Craton (after Zhao et al., 2005, 2012). The black square shows the locations of Fig. 2.

Fig. 2. Map of the Paleoproterozoic Jiao–Liao–Ji Belt showing the distribution of the Liaoji granitoids (modified after Li and Zhao, 2007).

2016, 2019). The pre-tectonic granitoids (also known as the Liaoji granitoids) are important constituents of the JLJB, and the tectonic nature of these granitoids is the key to define the initial tectonic setting of the JLJB. The Liaoji granitoids comprise mainly magnetite and hornblende/biotite monzogranitic gneisses, showing A-type granitoid affinities (Zhang and Yang, 1988; Sun et al., 1993; Hao et al., 2004; Lu et al., 2004a; Li and Zhao, 2007; Wang et al., 2015; Ren et al., 2017).

Liaohe Group rocks (He and Ye, 1998), and the existence of voluminous pre-tectonic A-type granitoids (Zhang and Yang, 1988; Sun et al., 1993; Hao et al., 2004; Lu et al., 2004a; Li and Zhao, 2007) provide important evidence for the intra-continental rift model. However, high-fieldstrength element (HFSE) depletions of ∼2.15 Ga mafic rocks most likely indicate that these units have subduction affinities, reflecting a collisional environment (Liu et al., 2013; Chen et al., 2016; Li et al., 2

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2.2. Fangjiaweizi and Dadingzi plutons

Recently, some pre-tectonic granodiorites have been identified in the Simenzi pluton (Yang et al., 2015; Song et al., 2016). These granodiorites are characterized by Na-rich geochemistry and complex zircon compositions, indicating a different origin from that of the traditional Liaoji granitoids. However, these granodiorites have not yet been further investigated. In this study, we undertook petrological, zircon U–Pb geochronological, geochemical, and Hf isotopic analyses of the Liaoji granitoids in the Hupiyu and Simenzi areas of the JLJB (Fig. 2). These new data provide insight into the petrogenesis of different Liaoji granitoid types. By combining the new data with existing geochemical, geochronological, and metamorphic data, we establish important constraints on the tectonic setting and evolution of the JLJB.

The association of Paleoproterozoic lithologies in the Simenzi area is similar to that in the Hupiyu area. The Simenzi area contains the Paleoproterozoic Simenzi, Fangjiaweizi, and Dadingzi plutons (Fig. 4). The Simenzi pluton is a complex pluton comprising 2157 Ma granodiorite (Song et al., 2016) and 2205 Ma A-type granitoids (Yang et al., 2015). Xenoliths of the Lieryu Formation are found in the southern part of the Simenzi pluton, suggesting an intrusive contact between this pluton and the lower Liaohe Group. The Fangjiaweizi and Dadingzi plutons are composed of granodiorite and lie to the west of Simenzi town. The Dadingzi pluton is located about 1.5 km from the Fangweizi pluton. K–Ar dating has yielded ages of 1624 Ma for the Fangjiaweizi pluton and 1565 Ma for the Dadingzi pluton (GSILP, 2003). The Fangjiaweizi and Dadingzi plutons intrude the Gaojiayu and Dashiqiao formations, and numerous faults and related Indosinian/Yanshanian gold deposits occur around these plutons (Liu and Ai, 2000). Gneissosity is common in the Simenzi pluton but is observed only around fault zones in the Fangjiaweizi and Dadingzi plutons. In the regional geological map (GSILP, 2003), the Fangjiaweizi and Dadingzi plutons are shown to intrude the Gaixian Formation. However, a faulted contact between the Dadingzi pluton and Gaixian Formation was observed during our field investigation (Fig. 5). The Dadingzi granitoids and Gaixian Formation are fractured around the faulted contact.

2. Geological setting The JLJB trends NE–SW and extends from eastern Shandong Province northeastwards through eastern Liaoning Province and to southern Jilin Province (Fig. 1). This belt separates the Eastern Block of the NCC into the Longgang and Liaonan–Rangnim blocks. The Archean basement materials of the Longgang Block include a series of 3.8–3.0 Ga tonalite–trondhjemite–granodiorite (TTG) gneisses and voluminous ∼2.5 Ga granitoids (Liu et al., 1992, 2008a, Liu et al., 2017a b; Wan et al., 1997, 2005, 2007, 2012, 2015; Wang et al., 2016). According to recent research, the Liaonan–Rangnim Block is composed of ∼2.5 Ga TTGs and Paleoproterozoic units (Kim et al., 2008; Meng et al., 2013; Wu et al., 2016; Zhai, 2016; Zhang et al., 2016a,b; Zhao et al., 2016). The JLJB comprises voluminous meta-sedimentary and volcanic successions (e.g., the Liaohe Group, Fenzishan and Jingshan groups, and Laoling and Ji’an groups) with associated granitic and mafic intrusions. Rocks in this belt underwent greenschist- to granulite-facies metamorphism at ∼1.9 Ga. Paleoproterozoic rocks in the study area consist mainly of the Liaohe Group and various granitoids. The Liaohe Group comprises the Langzishan, Lieryu, Gaojiayu, Dashiqiao, and Gaixian formations (Luo et al., 2004, 2008; Li et al., 2005). The Paleoproterozoic granitoids can be subdivided into two groups: pre-tectonic granitoids and post-tectonic granitoids (Zhang and Yang, 1988; Li and Zhao, 2007). Most previous studies have considered the Liaoji granitoids as gneissic A-type granitoids formed in an extensional environment, such as a rift or back-arc basin (Zhang and Yang, 1988; Sun et al., 1993; Hao et al., 2004; Lu et al., 2004a; Wang et al., 2015; Liu et al., 2018). However, other studies have concluded that the Liaoji granitoids are highly fractionated I-type granitoids that formed in a continental arc (Yang et al., 2015).

3. Sample descriptions The Hupiyu granitoids consist of 45%–50% alkali feldspar (microcline and perthite), 30% quartz, 15%–20% plagioclase, and minor biotite and aegirine (Fig. 6a–d). Accessory minerals include magnetite, titanite, apatite, and zircon. Most zircons occur in interstices between feldspar and quartz crystals (Fig. 6c and d). There is a lack of melanocratic minerals in some samples (e.g., DHP-3 and DHP-5). These granitoids are classified as monzogranite or syenogranite. The Fangjiaweizi and Dadingzi granitoids have similar mineral compositions. They are composed of 50% plagioclase, 25% quartz, 20% alkali feldspar, and minor biotite (Fig. 6e and f). Plagioclase crystals are larger and more euhedral than those of alkali feldspar. Melanocratic alkaline minerals are absent from the Fangjiaweizi and Dadingzi granitoids. Accessory minerals include magnetite, allanite, apatite, and zircon. Zircons of the Fangjiaweizi and Dadingzi granitoids are smaller and less abundant than those of the Hupiyu granitoids. In addition, most zircons in the Fangjiaweizi and Dadingzi granitoids are located within feldspar and quartz crystals. The Fangjiaweizi and Dadingzi granitoids have granodioritic compositions.

2.1. Hupiyu pluton

4. Analytical methods

The Hupiyu area contains the Paleoproterozoic Hupiyu, Housongshugou, and Nantaizi plutons (Fig. 3). The Hupiyu pluton, north of Hupiyu village, occupies the core of a WNW-plunging anticline. In the Hupiyu area, the anticline comprises rocks of the Lieryu, Gaojiayu, Dashiqiao, and Gaixian formations of the Liaohe Group, and the Hupiyu pluton intrudes the first three of these formations. The thickness of the Liaohe Group is constant along its boundary with the Hupiyu pluton, and the gneissosity of the pluton is parallel to the bedding of the Liaohe Group rocks. These observations are consistent with the emplacement model of granitoid magmas (Li et al., 1996, 1997). The 1.90–1.85 Ga Housongshugou and Nantaizi plutons (Ren et al., 2017) also intrude the Dashiqiao Formation. The contact between the Housongshugou and Hupiyu plutons is obscured by Quaternary rocks. The Housongshugou and Nantaizi plutons are composed of granodiorite and quartz monzonite, respectively. No gneissosity is observed in these two plutons. NE–SW- and NW–SE-trending faults are developed in the Hupiyu area and crosscut the Hupiyu pluton and Liaohe Group.

Whole-rock major and trace element analyses were performed at ALS Chemex Labs in Guangzhou, China. Major element compositions were determined by X-ray fluorescence (XRF) using a PANalytical Axios Advanced PW4400 XRF spectrometer. Trace element compositions were determined by inductively coupled plasma mass spectrometry (ICP–MS; X-series). Zircons from samples NHP-11 (Hupiyu pluton; 40°27′45″N, 122°50′02″E), DD-1 (Dadingzi pluton; 40°42′17″N, 123°41′20″E), and DTY-8 (Fangjiaweizi pluton; 40°43′54″N, 123°44′17″E) were separated using conventional magnetic and heavy liquid techniques at Langfang Regional Geological Survey, Hebei Province, China. Zircons were handpicked under a binocular microscope. Zircons were imaged using transmitted- and reflected-light optical microscopy, as well as by cathodoluminescence (CL) techniques, to identify internal textures. Euhedral, fracture-free, inclusion-free zircons were selected for isotope analysis. Zircon U–Pb dating of NHP-11 and DTY-8 by laser ablation (LA)–ICP–MS was performed at the MRL Key Laboratory of Metallogeny 3

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Fig. 3. Geological sketch map of the Hupiyu area (modified after Zhao and Hu, 1989). 1, Quaternary; 2, Gaixian Formation; 3, Dashiqiao Formation; 4, Gaojiayu Formation; 5, Lieryu Formation; 6, Nantaizi quartz monzonite; 7, Housongshugou granodiorite; 8, Hupiyu granitoids; 9, Thrust fault; 10, Inferred fault; 11, Sampling site; 12, Town.

Fig. 4. Geological sketch map of the Simenzi area. 1, Quaternary; 2, Cretaceous volcanics; 3, Neoproterozoic Qingbaikouan System; 4, Gaixian Formation; 5, Dashiqiao Formation; 6, Gaojiayu Formation; 7, Lieryu Formation; 8, Cretaceous granitoids; 9, Fangjiaweizi granodiorite; 10, Dadingzi granodiorite; 11, Simenzi granitoids; 12, Thrust fault; 13, Normal fault; 14, Strike-slip fault; 15, Inferred fault; 16, Sampling site; 17, Outcrop location (Fig. 5); 18, Town or village.

analysed and plotted using Isoplot version 3.0 (Ludwing, 2001). Common Pb was corrected following procedures developed by Andersen (2002). Uncertainties on individual LA–ICP–MS analyses are quoted at the 1σ level, and pooled uncertainties of weighted-mean ages are quoted at the 95% (2σ) confidence level. LA–ICP–MS U–Pb zircon dating of sample DD-1 was carried out at the Key Laboratory of Mineral Resources Evaluation in Northeast Asia,

and Mineral Assessment, Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing, China. Analyses used a 35 μm laser diameter, with a pit depth of 20–40 μm, and an ablation time of 45 s. Reference zircon GJ-1 was used for external age calibration, and NIST SRM 610 silicate glass was used for instrument optimization. Details of the parameters and procedures used during these analyses can be found in Hou et al. (2007, 2009). The resulting data were 4

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Fig. 5. Photograph and geological section showing the contact between the Gaixian Formation and Dadingzi pluton. (a) Faulted contact between the Gaixian Formation and Dadingzi pluton. (b) Contact zone detail. (c) Geological section of the outcrop in (a).

magmatic origin is indicated by fine-scale oscillatory growth zoning and Th/U ratios of 0.28–0.71. Narrow grey–black rims around some of the grains in CL images are interpreted as syntaxial metamorphic overgrowths. 207Pb/206U concordia ages of 20 zircons from sample NHP-11 range from 2292 ± 40 to 2117 ± 43 Ma, yielding a weighted-mean age of 2180 ± 14 Ma (MSWD = 1.04) (Fig. 8a and b). Zircons from sample DTY-8 have a uniform grain size of ∼100 μm and length/width ratios of 1.5–3.0 (Fig. 7b). Most zircons from this sample are subhedral to euhedral, display low luminescence, and have concentric oscillatory zoning. Th/U ratios range from 0.17 to 0.94. Twenty analyses have a wide range of 207Pb/206Pb ages between 3111 and 1869 Ma. These results can be divided into three groups: inherited zircons (n = 3), primary magmatic zircons (n = 14), and metamorphic zircons (n = 3). Ages of the inherited zircons in the sample are 3111 ± 17, 2524 ± 16, and 2428 ± 22 Ma. Ages of the metamorphic zircons range from 1921 to 1818 Ma, with Th/U ratios of 0.17–0.49. Ages of 12 primary magmatic zircons range from 2185 to 2029 Ma (two magmatic zircons have a concordance of < 95% and are not shown in the diagrams), yielding a weighted-mean age of 2130 ± 24 Ma (MSWD = 1.8) (Fig. 8c and d). Zircon U–Pb ages from sample DTY-8 therefore support a Paleoproterozoic crystallisation age for the Fangjiaweizi pluton. Zircons from sample DD-1 has a similar age composition to that of sample DTY-8. Most zircons from sample DD-1 have a uniform grain size of ∼100 μm with fine-scale oscillatory growth zoning (Fig. 7c). Zircons with an inherited core and overgrowth are common in sample DD-1. Sixty analyses show a wide range of 207Pb/206Pb ages between 3058 and 1872 Ma. The concordance of seven zircons is < 95%, and the remaining zircons (concordance > 95%, n = 53) can be divided into three groups: inherited zircons (n = 10), primary magmatic zircons (n = 38), and metamorphic zircons (n = 5). Ages of the inherited and metamorphic zircons range from 2800 to 2328 Ma (Th/U = 0.14–0.82) and 2031 to 1872 Ma (Th/U = 0.16–0.40), respectively. Ages of the primary magmatic zircons range from 2294 to 2072 Ma, with Th/U

Ministry of Natural Resources of China, Changchun, China. The analysis spots were 25 μm in diameter. U, Th, and Pb concentrations were calibrated using 29Si as an internal standard. Standard zircon 91,500 (Wiedenbeck et al., 1995) was used as an external standard to normalize isotopic fractionation during analysis. Reference zircon GJ-1 was used for external age calibration. Details of the parameters and procedures used during these analyses are given by Yuan et al. (2007). Raw data were processed using the ICPMSData Cal program (Version 6.7) (Liu et al., 2008b). Uncertainties on individual analyses are reported as 1σ errors, and weighted-mean ages are given at the 2σ confidence level. The resulting data were plotted using Isoplot version 3.0 (Ludwing, 2001). In situ zircon Lu–Hf isotope analyses were also undertaken at the Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing, China, using a New Wave UP213 laser coupled to a Neptune multi-collector ICP–MS instrument. Instrumental conditions and data acquisition followed the methods developed by Hou et al. (2007). These analyses used a stationary spot with a laser beam diameter of either 40 or 55 μm, depending on the size of the ablated domains. Reference zircon GJ-1 was used as the external standard. Analyses of GJ-1 yielded a 176Hf/177Hf ratio of 0.282007 ± 0.000007 (2σ), which is indistinguishable from the weighted-mean 176Hf/177Hf ratio of 0.282000 ± 0.000005 (2σ) determined using solution analysis by Morel et al. (2008).

5. Results 5.1. Zircon U–Pb dating Three samples collected from the Hupiyu (sample NHP-11; Table 1), Fangjiaweizi (sample DTY-8; Table 2) and Dadingzi (sample DD-1; Table 3) plutons were dated using zircon U–Pb methods. Zircons from sample NHP-11 are mainly subhedral, have dimensions of 100–200 μm, and length/width ratios of 1.5–2.0 (Fig. 7a). A 5

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Fig. 6. Photomicrographs of the Liaoji granitoids. (a–d) Photomicrographs of the Hupiyu granitoids. (e) Photomicrograph of a Dadingzi granitoid. (f) Photomicrograph of a Fangjiaweizi granitoid. Ae, aegirine–augite; Bi, Biotite; Mc, Microcline; Ms, Muscovite; Mt, Magnetite; Pl, plagioclase; Pth, Perthite; Q, quartz; Zrn, Zircon.

5.3. Major and trace element data

ratios of 0.24–0.66, yielding a weighted-mean age of 2173 ± 11 Ma (MSWD = 1.1) (Fig. 8e and f). Zircon U–Pb ages from sample DD-1 therefore indicate that the Dadingzi pluton has a very similar crystallisation age to that of the Fangjiaweizi pluton.

Major and trace element compositions of five Hupiyu granitoid samples (DHP-3, DHP-4, DHP-5, DHP-6, and DHP-11), four Fangjiaweizi granitoid samples (DTY-5, DTY-7, DTY-8, and DTY-9), and two Dadingzi granitoid samples (DTY-10 and DTY-11) from the JLJB are listed in Table 6.

5.2. Zircon Lu–Hf isotope data In situ zircon Lu–Hf isotopic compositions are listed in Table 4. Hf/177Hf ratios of zircons from the Hupiyu granitoids (sample NHP11) range from 0.281429 to 0.281693. Sixteen analyses yielded εHf(t) values of −1.77 to +7.17 (Fig. 9a). Two-stage Hf depleted mantle model ages (TDM2) of these zircons range from 2790 to 2305 Ma. In situ zircon Lu–Hf isotopic analysis was also performed on sample DTY-8. Ten analyses yielded initial 176Hf/177Hf ratios of 0.281073 to 0.281690 and εHf(t) values of −13.04 to +6.72 (Fig. 9b; Table 5). TDM2 values of these zircons vary from 3518 to 2260 Ma. 176

5.3.1. Hupiyu pluton Geochemical analyses indicate that the Hupiyu monzogranites have high SiO2 (73.0–75.8 wt%), K2O (3.93–6.04 wt%), Na2O (2.88–4.51 wt %), Fe2O3T (2.46–4.09 wt%), and Al2O3 (11.90–12.45 wt%) contents and low MgO (0.02–0.13 wt%), CaO (0.08–0.90 wt%), TiO2 (0.16–0.26 wt%), and P2O5 (0.01–0.04 wt%) contents. According to a SiO2 vs. K2O diagram (Fig. 10a), the Hupiyu monzogranites belong to the high-K calc-alkaline series. The samples are weakly peraluminous 6

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Table 1 LA–ICP–MS U–Pb zircon age datas for Hupiyu granitoids. NHP-11

Contents (ppm)

Spots

Th

U

1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20

234.14 329.08 159.64 391.85 471.22 500.50 103.38 347.41 116.54 205.90 236.63 227.12 96.51 217.54 356.13 83.56 81.59 159.77 177.62 73.69

438.39 645.11 262.52 1051.22 1664.08 1934.81 209.58 809.66 405.75 290.96 418.91 2650.11 205.10 380.98 613.68 134.50 192.18 360.16 298.79 172.71

Th/U

Isotopic ratios 207

Pb/

0.53 0.51 0.61 0.37 0.28 0.26 0.49 0.43 0.29 0.71 0.56 0.09 0.47 0.57 0.58 0.62 0.42 0.44 0.59 0.43

206

Pb

0.1388 0.1359 0.1377 0.1376 0.1372 0.1321 0.1362 0.1377 0.1314 0.1345 0.1338 0.1355 0.1394 0.1350 0.1359 0.1453 0.1374 0.1362 0.1340 0.1363

Ages (Ma) 1σ

207

235

0.00289 0.00255 0.00274 0.00225 0.00222 0.00212 0.00267 0.00247 0.00364 0.00300 0.00277 0.00241 0.00319 0.00259 0.00219 0.00335 0.00285 0.00226 0.00252 0.00282

7.5598 7.2978 7.4540 7.4735 7.5181 7.1114 7.3809 7.0564 7.1199 7.1635 7.2260 7.3609 7.6534 7.1934 7.3391 7.7810 7.7531 7.4111 7.4819 7.4801

Pb/

U

1σ

206

0.16319 0.14879 0.16247 0.14114 0.14942 0.14135 0.17716 0.15258 0.27368 0.19131 0.18267 0.15900 0.18644 0.15054 0.13640 0.20234 0.17404 0.14846 0.17366 0.16474

0.3919 0.3861 0.3891 0.3908 0.3947 0.3878 0.3909 0.3705 0.3914 0.3853 0.3904 0.3926 0.3984 0.3849 0.3886 0.3850 0.4085 0.3928 0.4016 0.3946

Pb/

238

U

1σ

207

Pb/206Pb

1σ

207

Pb/235U

1σ

206

Pb/238U

0.00573 0.00545 0.00512 0.00526 0.00582 0.00544 0.00624 0.00579 0.01216 0.00642 0.00648 0.00595 0.00635 0.00522 0.00448 0.00544 0.00730 0.00698 0.00707 0.00571

2213 2176 2198 2198 2192 2126 2189 2198 2117 2157 2148 2170 2220 2165 2176 2292 2195 2179 2151 2180

36 33 34 28 28 28 34 30 43 39 31 36 40 33 29 40 37 29 33 37

2180 2149 2167 2170 2175 2125 2159 2119 2127 2132 2140 2156 2191 2136 2154 2206 2203 2162 2171 2171

19 18 20 17 18 18 21 19 34 24 23 19 22 19 17 23 20 18 21 20

2132 2105 2119 2126 2144 2113 2127 2032 2129 2101 2125 2135 2161 2099 2116 2100 2208 2136 2176 2144

1σ 27 25 24 24 27 25 29 27 56 30 30 28 29 24 21 25 33 32 33 26

contents, higher Na2O (5.10–5.61 wt%), Al2O3 (14.90–16.80 wt%), MgO (0.22–0.49 wt%), and CaO (0.58–2.50 wt%) contents, and similar P2O5 (0.01–0.04 wt%) contents. The Fangjiaweizi and Dadingzi granodiorites fall into the calc-alkaline series (Fig. 10a) and have A/CNK values of 1.00–1.13 (Fig. 10b). Total REE concentrations of the Fangjiaweizi and Dadingzi granodiorites vary between 15.19 and 33.14 ppm, with ratios of light to heavy REEs of 3.15–4.15. Chondrite-normalized REE patterns show relative enrichment in light REEs, as indicated by high (La/Yb)N values of 7.55–15.04, and (La/Sm)N values of 3.34–4.76 (Fig. 11a). All samples have small negative Eu anomalies (Eu/Eu* = 0.41–0.90). On a primitive-mantle-normalized trace element diagram, data for the Fangjiaweizi and Dadingzi samples are enriched in large-ion lithophile elements (LILEs; e.g., Cs, K, Ba, and Sr) and depleted in HFSEs (e.g., Th, Nb, and Ti) (Fig. 11b). Sr and Y contents indicate that the Fangjiaweizi and Dadingzi samples are high-Sr, low-Y granitoids.

with A/CNK (molar ratio of Al2O3/[CaO + Na2O + K2O]) values of 1.00–1.13 (Fig. 10b). These features indicate that the Hupiyu monzogranites are K-rich. Total rare earth element (REE) contents of the Hupiyu monzogranites vary from 65.09 to 337.51 ppm. Chondrite-normalized REE patterns show that the samples are enriched in light REEs and depleted in heavy REEs, with (La/Yb)N ranging from 0.68 to 7.62 (Fig. 11a). These patterns illustrate a strong REE fractionation in the Hupiyu monzogranites. The monzogranites also have clear negative Eu anomalies, with Eu/Eu* values of 0.27–0.55. In primitive-mantle-normalized diagrams, data for these samples exhibit enrichment in Rb, K, Th, and U, but depletion in Nb and Ti (Fig. 11b). These features suggest that the Hupiyu samples are low-Sr, high-Y granitoids. 5.3.2. Fangjiaweizi and Dadingzi plutons Compared with the Hupiyu monzogranites, the Fangjiaweizi and Dadingzi granodiorites have lower SiO2 (69.9–72.9 wt%), K2O (1.78–2.69 wt%), Fe2O3T (1.23–1.50 wt%), and TiO2 (0.10–0.12 wt%) Table 2 LA–ICP–MS U–Pb zircon age datas for Fangjiaweizi granitoids. DTY-8

Contents (ppm)

Spots

Th

U

1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20

197.12 331.31 142.81 124.35 688.94 237.84 416.39 160.96 96.75 114.51 423.87 591.56 140.89 164.15 182.25 460.12 189.47 201.59 76.49 116.13

240.97 490.54 229.66 162.95 1184.38 383.96 856.70 239.93 583.69 423.70 452.32 1035.09 413.53 228.84 320.96 1077.79 261.38 253.98 416.92 211.14

Th/U

Isotopic ratios 207

0.82 0.68 0.62 0.76 0.58 0.62 0.49 0.67 0.17 0.27 0.94 0.57 0.34 0.72 0.57 0.43 0.72 0.79 0.18 0.55

Pb/

206

0.1351 0.1332 0.1351 0.1221 0.1329 0.1250 0.1143 0.1301 0.1177 0.1665 0.1284 0.1366 0.2386 0.1326 0.1315 0.1111 0.1321 0.1574 0.1334 0.1482

Pb

Ages (Ma) 1σ

207

235

0.00324 0.00294 0.00311 0.00732 0.00216 0.00268 0.00196 0.00222 0.00181 0.00156 0.00226 0.00129 0.00253 0.00190 0.00172 0.00190 0.00221 0.00200 0.00212 0.02168

6.8424 7.0368 6.7901 7.4699 6.8564 7.0847 5.3952 7.1995 5.2563 9.1516 7.1165 6.6613 18.3359 7.1388 6.4944 5.1629 6.9624 10.1279 7.0878 7.9201

Pb/

U

1σ

206

0.24040 0.22217 0.22507 0.51447 0.15568 0.17513 0.13443 0.13777 0.08874 0.12221 0.13024 0.06983 0.25290 0.10915 0.12036 0.07610 0.13290 0.17068 0.18264 0.87805

0.3681 0.3840 0.3647 0.4429 0.3718 0.4066 0.3381 0.3963 0.3191 0.3920 0.3953 0.3483 0.5496 0.3877 0.3544 0.3357 0.3809 0.4665 0.3799 0.3903

7

238

Pb/

U

1σ

207

Pb/206Pb

0.00879 0.00884 0.00852 0.02605 0.00606 0.00602 0.00771 0.00556 0.00335 0.00445 0.00525 0.00257 0.00662 0.00537 0.00478 0.00414 0.00570 0.00814 0.00572 0.01995

2165 2140 2165 1987 2136 2029 1869 2099 1921 2524 2076 2185 3111 2132 2118 1818 2128 2428 2144 2325

1σ

207

Pb/235U

1σ

206

Pb/238U

41 44 41 112 28 43 30 30 28 16 26 21 17 25 24 31 29 22 28 258

2091 2116 2084 2169 2093 2122 1884 2136 1862 2353 2126 2068 3008 2129 2045 1847 2107 2447 2123 2222

31 28 29 62 20 22 21 17 14 12 16 9 13 14 16 13 17 16 23 100

2021 2095 2004 2364 2038 2200 1878 2152 1785 2132 2147 1927 2823 2112 1955 1866 2081 2468 2076 2124

1σ 41 41 40 116 28 28 37 26 16 21 24 12 28 25 23 20 27 36 27 92

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Table 3 LA–ICP–MS U–Pb zircon age datas for Dadingzi granitoids. DD-1

Contents (ppm)

Spots

Th

U

1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60

174.15 131.95 217.49 120.44 117.09 294.75 174.24 98.47 440.06 100.74 164.21 122.73 127.51 87.55 36.60 415.20 228.40 3085.37 182.22 370.64 504.07 198.35 229.91 187.19 77.79 330.51 171.92 455.01 458.77 170.33 418.05 172.71 148.50 191.26 1805.05 151.43 276.01 116.51 112.57 63.05 110.69 180.29 113.44 200.36 210.65 102.67 113.97 312.35 354.63 152.57 227.76 102.97 79.22 115.31 90.33 155.46 91.14 555.40 476.07 94.84

281.35 231.99 586.66 227.40 844.37 544.27 687.79 223.48 1144.53 227.76 1007.59 363.58 225.39 157.59 152.15 1490.52 815.95 7372.27 727.41 1182.14 1273.32 299.07 445.41 335.90 170.93 611.65 267.08 1359.57 794.12 305.81 964.87 209.71 610.79 975.95 5133.14 298.51 663.41 237.81 231.21 114.23 208.43 279.36 232.02 309.14 429.34 198.53 230.38 1753.76 484.59 238.89 427.74 204.68 149.95 259.94 192.89 282.89 184.64 1133.51 1193.98 209.42

Th/U

Isotopic ratios 207

0.62 0.57 0.37 0.53 0.14 0.54 0.25 0.44 0.38 0.44 0.16 0.34 0.57 0.56 0.24 0.28 0.28 0.42 0.25 0.31 0.40 0.66 0.52 0.56 0.46 0.54 0.64 0.33 0.58 0.56 0.43 0.82 0.24 0.20 0.35 0.51 0.42 0.49 0.49 0.55 0.53 0.65 0.49 0.65 0.49 0.52 0.49 0.18 0.73 0.64 0.53 0.50 0.53 0.44 0.47 0.55 0.49 0.49 0.40 0.45

206

Pb/

0.1358 0.1344 0.1648 0.1455 0.1622 0.1348 0.1145 0.1389 0.1306 0.1329 0.1155 0.1281 0.1354 0.1483 0.2309 0.1991 0.1548 0.1384 0.1429 0.1189 0.1251 0.1407 0.1377 0.1380 0.1395 0.1396 0.1385 0.1179 0.1571 0.1335 0.1282 0.1661 0.1333 0.1319 0.1821 0.1629 0.1330 0.1345 0.1332 0.1354 0.1333 0.1358 0.1353 0.1341 0.1337 0.1326 0.1343 0.1267 0.1575 0.1316 0.1328 0.1323 0.1667 0.1331 0.1369 0.1347 0.1368 0.1736 0.1379 0.1392

Pb

Ages (Ma) 1σ

207

0.002877 0.002679 0.002923 0.002695 0.002608 0.002241 0.002008 0.002696 0.002539 0.002883 0.002393 0.002478 0.002600 0.003645 0.014025 0.007925 0.002805 0.005469 0.002829 0.002376 0.002756 0.002915 0.002665 0.002611 0.002651 0.002394 0.002502 0.002007 0.002841 0.002688 0.002641 0.003408 0.002469 0.003793 0.012555 0.002814 0.002363 0.002585 0.002809 0.003411 0.003092 0.002799 0.002681 0.002466 0.002364 0.002398 0.002367 0.002143 0.002701 0.002610 0.002632 0.002546 0.003049 0.002320 0.002346 0.002279 0.002560 0.003980 0.002580 0.003035

7.6024 7.6626 10.9747 8.0256 10.6151 7.9263 5.3665 7.6448 5.9377 7.1395 4.8904 6.7501 7.3745 9.2005 16.9753 9.1419 9.2593 3.4977 7.7786 5.4359 5.7473 7.7320 7.8410 7.8976 7.8816 8.2873 7.8575 5.5959 9.3927 7.9983 6.9478 11.6240 7.2797 4.9413 5.5035 11.0481 7.9836 7.5768 7.5681 7.7822 7.7809 7.4099 7.8336 7.6065 7.6399 7.2543 7.8582 4.2984 10.0014 7.2682 7.6223 7.6245 10.8042 7.3586 7.7368 7.9212 7.6159 10.9234 7.5466 7.6508

Pb/

235

U

1σ

206

0.167417 0.153833 0.201652 0.160662 0.178420 0.139256 0.102585 0.140760 0.175404 0.143624 0.102862 0.128469 0.138023 0.283807 1.555340 0.549209 0.198287 0.188999 0.149200 0.177350 0.131532 0.168964 0.152919 0.151750 0.164455 0.170633 0.143242 0.107023 0.203375 0.175729 0.137611 0.264032 0.132693 0.123886 0.604307 0.200922 0.165018 0.150660 0.151894 0.215710 0.200790 0.176188 0.164246 0.141391 0.141251 0.137606 0.167019 0.137081 0.182190 0.153232 0.163661 0.160078 0.204879 0.126977 0.141417 0.140086 0.140256 0.358272 0.185528 0.171023

0.4040 0.4112 0.4804 0.3976 0.4715 0.4235 0.3376 0.3969 0.3289 0.3868 0.3044 0.3792 0.3929 0.4444 0.4903 0.3191 0.4307 0.1787 0.3938 0.3298 0.3323 0.3973 0.4117 0.4138 0.4085 0.4290 0.4098 0.3428 0.4310 0.4320 0.3912 0.5042 0.3938 0.2730 0.2011 0.4889 0.4323 0.4060 0.4097 0.4135 0.4216 0.3938 0.4184 0.4097 0.4135 0.3963 0.4228 0.2462 0.4596 0.3998 0.4156 0.4174 0.4689 0.3997 0.4084 0.4249 0.4017 0.4502 0.3948 0.3962

6. Discussion

238

Pb/

U

1σ

207

Pb/206Pb

0.005287 0.004542 0.005830 0.005127 0.005139 0.004978 0.004372 0.004901 0.009201 0.004382 0.003845 0.004084 0.004970 0.006856 0.014906 0.008836 0.005252 0.003612 0.004278 0.008825 0.003774 0.004484 0.004218 0.004540 0.005460 0.006434 0.004215 0.004651 0.006163 0.005731 0.004784 0.006799 0.004006 0.005457 0.005436 0.005277 0.005747 0.004407 0.004163 0.005411 0.007475 0.006775 0.005754 0.004541 0.005327 0.005550 0.006083 0.007647 0.005040 0.004597 0.004950 0.005367 0.004617 0.003749 0.004904 0.004825 0.003920 0.008192 0.008038 0.005605

2174 2167 2505 2294 2480 2162 1872 2214 2106 2137 1889 2072 2169 2328 3058 2820 2800 2209 2262 1940 2031 2236 2198 2202 2221 2222 2209 1924 2424 2144 2073 2520 2143 2124 2672 2487 2139 2158 2143 2169 2142 2176 2169 2154 2147 2132 2155 2054 2429 2120 2135 2129 2524 2140 2191 2161 2187 2592 2211 2218

1σ

207

Pb/235U

1σ

206

Pb/238U

37 35 30 32 27 29 31 34 33 39 37 33 34 42 98 65 31 69 34 35 39 37 34 33 33 30 31 30 30 40 36 35 32 50 115 29 31 33 36 44 41 36 35 32 30 31 31 31 29 35 34 34 30 31 30 30 33 39 33 33

2185 2192 2521 2234 2490 2223 1880 2190 1967 2129 1801 2079 2158 2358 2933 2352 2364 1527 2206 1891 1939 2200 2213 2219 2218 2263 2215 1915 2377 2231 2105 2575 2146 1809 1901 2527 2229 2182 2181 2206 2206 2162 2212 2186 2190 2143 2215 1693 2435 2145 2187 2188 2506 2156 2201 2222 2187 2517 2179 2191

20 18 17 18 16 16 16 17 26 18 18 17 17 28 88 55 20 43 17 28 20 20 18 17 19 19 16 17 20 20 18 21 16 21 94 17 19 18 18 25 23 21 19 17 17 17 19 26 17 19 19 19 18 15 17 16 17 31 22 20

2188 2221 2529 2158 2490 2277 1875 2155 1833 2108 1713 2073 2136 2371 2572 1785 2309 1060 2141 1837 1849 2157 2223 2232 2208 2301 2214 1900 2310 2315 2129 2632 2141 1556 1181 2566 2316 2196 2214 2231 2268 2141 2253 2213 2231 2152 2273 1419 2438 2168 2241 2249 2479 2168 2208 2283 2177 2396 2145 2152

1σ 24 21 25 24 23 23 21 23 45 20 19 19 23 31 64 43 24 20 20 43 18 21 19 21 25 29 19 22 28 26 22 29 19 28 29 23 26 20 19 25 34 31 26 21 24 26 28 40 22 21 23 24 20 17 22 22 18 36 37 26

depletion in Ba and Sr, high Ga/Al ratios, and marked negative Eu anomalies. These features are typical of A-type granitoids (Collins et al., 1982; Whalen et al., 1987; Zhang et al., 2012; Jin and Shen, 2015). In geochemical discrimination diagrams, data for the Hupiyu monzogranites plot in the field of A-type granitoids (Fig. 12). However, it is difficult to distinguish A-type granitoids from highly fractionated S- and I-type granitoids. King et al. (1997) proposed that highly fractionated Stype granitoids have high P2O5 contents (average = 0.14 wt%). However, P2O5 contents of the Hupiyu monzogranites are substantially

6.1. Granitoid types 6.1.1. Hupiyu pluton Most zircons are interspersed between feldspar and quartz, indicating a high crystallisation temperature. The Hupiyu monzogranites are enriched in SiO2 and alkalis and are depleted in CaO, MgO, and Al2O3. In addition, these rocks have enrichment in Th, Zr, Y, Rb, and U, 8

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Fig. 7. CL images and laser ablation analysis sites of representative zircons from the Liaoji granitoids.

lower (only 0.01–0.03 wt%). High FeOT (> 1 wt%), Zr + Nb + Ce + Y (> 350 ppm), and magma temperatures (> 800 °C; Section 6.2) of the Hupiyu monzogranites further support their A-type affinities (Whalen et al., 1987; Eby, 1990; Wang et al., 2000; Wu et al., 2007a). A/CNK ratios and mineral compositions provide additional evidence that the Hupiyu samples are peraluminous A-type granitoids. In summary, the Hupiyu monzogranites are typical Liaoji granitoids and share characteristics with most of these granitoids. They are A-type granitoids, are widespread in the JLJB, and reflect an extensional setting.

6.1.2. Fangjiaweizi and Dadingzi plutons Although the Fangjiaweizi, Dadingzi, and Hupiyu plutons formed at similar times, they have marked differences in geochemical composition. In particular, SiO2 and total REE contents of the Fangjiaweizi and Dadingzi granodiorites are substantially lower than those of the Hupiyu monzogranites. In geochemical discrimination diagrams, all of the Fangjiaweizi and Dadingzi granodiorites plot in the I- and S-type fields (Fig. 11). Variation in the P2O5 content of the Fangjiaweizi and Dadingzi granodiorites is consistent with the evolutionary trend of I-type granitoids in a SiO2 vs. P2O5 diagram (Fig. 13) (Harrison and Watson, 1984; Bea et al., 1992; Tao et al., 2013). These features suggest that 9

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Fig. 8. (a, c, e) Zircon U–Pb concordia diagrams and (b, d, f) weighted-mean age diagrams for the Liaoji granitoids.

monzogranitic gneisses) have not been further pursued. The discovery of adakitic rocks in the present study is crucial for determining the initial tectonic setting of the JLJB. A-type granitoids can occur in various extensional settings, including rift, post-orogenic, and post-collisional stages. An assemblage of A-type and adakitic granitoids should place further constraints on the tectonic nature and evolution of the JLJB (Section 6.4).

these granodiorites are I-type granitoids. High Sr and low Rb contents and small negative Eu anomalies imply that large-scale differentiation of plagioclase did not occur during crystallisation of these rocks. High Sr/Y (115.5–381.5) and low K2O/Na2O (0.32–0.52), Mg# (26.35–41.53), and total REE contents (15.19–33.14 ppm) suggest that the Fangjiaweizi and Dadingzi granodiorites are similar to high-alumina TTG rocks, reflecting an affinity with adakitic rocks (Fig. 14). Most of the known adakitic rocks in the JLJB are post-tectonic rocks, such as the Qinghe, Housongshugou, and Nantaizi plutons (Lu et al., 2005; Ren et al., 2017). Although granodiorites have been identified in the Simenzi pluton (Yang et al., 2015), the difference between those granodiorites and typical Simenzi granitoids (hornblende

6.2. Magma geochronology and temperature The Fangjiaweizi and Dadingzi plutons have been dated previously by K–Ar methods and yielded ages of ∼1.6 Ga (GSILP, 2003). However, 10

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Table 4 Hf isotopic composition of zircons from Hupiyu granitoids. Spots

Ages

176

176

176

2σ

εHf (t)

2σ

tDM1 (Ma)

tDM2 (Ma)

fLu/Hf

NHP11-1 NHP11-2 NHP11-3 NHP11-4 NHP11-5 NHP11-7 NHP11-8 NHP11-9 NHP11-11 NHP11-12 NHP11-13 NHP11-14 NHP11-15 NHP11-17 NHP11-19 NHP11-20

2213 2176 2198 2198 2126 2189 2198 2117 2148 2170 2220 2165 2176 2195 2151 2180

0.036764 0.198348 0.077842 0.092803 0.085720 0.082878 0.058241 0.097956 0.055345 0.129469 0.062232 0.103773 0.064158 0.118809 0.094286 0.048742

0.000795 0.003497 0.001447 0.001684 0.001488 0.001541 0.001107 0.001785 0.001054 0.002220 0.001166 0.001908 0.001175 0.002217 0.001693 0.000907

0.281528 0.281534 0.281488 0.281490 0.281467 0.281500 0.281466 0.281456 0.281429 0.281693 0.281469 0.281519 0.281461 0.281525 0.281561 0.281472

0.000023 0.000024 0.000023 0.000025 0.000023 0.000022 0.000012 0.000020 0.000021 0.000024 0.000023 0.000018 0.000016 0.000020 0.000024 0.000017

4.35 −0.23 1.64 1.35 −0.75 1.71 1.38 −1.77 −0.98 7.17 1.86 1.34 0.59 1.74 2.83 1.47

0.83 0.84 0.83 0.88 0.81 0.78 0.41 0.71 0.74 0.84 0.80 0.65 0.58 0.71 0.85 0.62

2399 2570 2495 2508 2526 2485 2502 2563 2550 2257 2503 2482 2515 2495 2410 2482

2512 2764 2667 2685 2758 2655 2683 2814 2790 2305 2670 2660 2714 2658 2557 2663

−0.98 −0.89 −0.96 −0.95 −0.96 −0.95 −0.97 −0.95 −0.97 −0.93 −0.96 −0.94 −0.96 −0.93 −0.95 −0.97

Yb/177Hf

Lu/177Hf

Hf/177Hf

(Fig. 8c and e). CL images of DD-1 zircons provide further evidence for the origins of the different zircons (Fig. 7c). The ∼2.15 Ga zircons show high luminescence and have concentric oscillatory zoning, whereas the ∼1.85 Ga zircons display low luminescence and have weak or no oscillatory zoning. Compared with the ∼2.15 Ga zircons, the ∼1.85 Ga zircons are scarcer and have more fissures. All ∼1.85 Ga ages of sample DD-1 were obtained from overgrowths of zircons that have ancient cores. In other words, no zircon grains formed independently at ∼1.85 Ga. Therefore, we infer that the ∼1.85 Ga zircons are either overgrowths of protolith zircon or products of recrystallization of magmatic zircon under solid state and/or fluid conditions. The ∼1.85 Ga ages suggest that the Fangjiaweizi and Dadingzi plutons were metamorphosed during the 1.9–1.8 Ga JLJB orogeny. Other gneissic granitoids (e.g., the Mafeng and Simenzi granitoids) also record this metamorphic event (Li and Zhao, 2007; Song et al., 2016). These new data demonstrate the existence of ∼2.15 Ga granodiorites, and the Liaoji granitoids contain at least two types of granitoid, which are A-type and adakitic granitoids. This result represents the first report of pre-tectonic adakitic granitoids in the JLJB. The A-type granitoids, which are the most common Liaoji granitoids, are hightemperature granitoids with highly consistent zircon ages. In comparison, the adakitic granitoids show low-temperature characteristics and complex zircon compositions, and these granitoids occur only in the Simenzi area. The A-type granitoids are easily recognizable on account of their highly consistent zircon ages, whereas the adakitic granitoids have previously been misidentified as post-tectonic rocks (GSILP, 2003). Pre-tectonic granitoids with complex zircon compositions are also found in the Mafeng pluton (Li and Zhao, 2007). However, there

the K–Ar system has a low closure temperature, making it unsuitable for dating ancient rocks. A more robust method is U–Pb dating. Our zircon U–Pb dating shows that the Hupiyu (2180 ± 14 Ma), Fangjiaweizi (2130 ± 24 Ma), and Dadingzi (2173 ± 11 Ma) granitoids are Paleoproterozoic in age, consistent with ages of 2205–2143 Ma for the Liaoji granitoids (Lu et al., 2004a,b, 2005, 2006; Li and Zhao, 2007; Yang et al., 2015; Song et al., 2016; Ren et al., 2017). Inherited zircons are common in samples DTY-8 (Fangjiaweizi granodiorite) and DD-1 (Dadingzi granodiorite), whereas they are scarce in sample NHP-11 (Hupiyu monzogranite). The difference may originate from differences in the magmatic temperatures and chemical compositions of the rocks. Zirconium saturation temperatures (Watson and Harrison, 1983) reveal that the magma temperature of the monzogranites (849–884 °C) was substantially higher than that of the granodiorites (726–740 °C). The magma temperature of the Hupiyu monzogranites was sufficiently high that inherited zircons could not be preserved. In addition, the Hupiyu monzogranites (A-type granitoids) are characterized by being anhydrous, and therefore metamorphic zircons would have been hard to form. All of the Paleoproterozoic granodiorites in the JLJB were once considered to be post-tectonic granitoids, including the Fangjiaweizi and Dadingzi granodiorites (Lu et al., 2005; Song et al., 2016; Ren et al., 2017). Compared with zircons of typical ∼1.85 Ga granitoids in the JLJB (Lu et al., 2005, 2006; Liu et al., 2014; Song et al., 2016; Ren et al., 2017), ∼1.85 Ga zircons from samples DTY-8 and DD-1 are scarce and span a wide range of ages (1921–1818 Ma for DTY-8 and 2031–1872 Ma for DD-1). In addition, most age ellipses of the ∼1.85 Ga zircons from these two samples lie beneath the concordia line

Fig. 9. εHf(t) vs. age plots for zircons from the (a) Hupiyu and (b) Fangjiaweizi granitoids. 11

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Table 5 Hf isotopic composition of zircons from Fangjiaweizi granitoids. Spots

Ages

176

Yb/177Hf

DTY-8-2 DTY-8-3 DTY-8-5 DTY-8-8 DTY-8-11 DTY-8-12 DTY-8-14 DTY-8-15 DTY-8-17 DTY-8-19

2140 2165 2136 2099 2076 2185 2132 2118 2128 2144

0.076278 0.091029 0.024306 0.055746 0.059317 0.091035 0.077786 0.191208 0.154680 0.169156

176

176

2σ

εHf (t)

2σ

tDM1 (Ma)

tDM2 (Ma)

fLu/Hf

0.001334 0.001569 0.000456 0.000998 0.001044 0.001541 0.001216 0.003973 0.003165 0.002808

0.281467 0.281478 0.281073 0.281431 0.281690 0.281505 0.281456 0.281525 0.281486 0.281531

0.000020 0.000021 0.000019 0.000021 0.000018 0.000023 0.000019 0.000030 0.000030 0.000020

−0.20 0.39 −13.04 −1.91 6.72 1.81 −0.61 −2.41 −2.46 0.00

0.71 0.74 0.67 0.76 0.63 0.81 0.69 1.06 1.06 0.70

2516 2517 2988 2543 2191 2478 2524 2618 2617 2526

2736 2719 3518 2809 2260 2646 2755 2854 2865 2726

−0.96 −0.95 −0.99 −0.97 −0.97 −0.95 −0.96 −0.88 −0.90 −0.92

Lu/177Hf

Hf/177Hf

are no geochronological data for this pluton. The ∼2.15 Ga adakitic granitoids may be much more widespread in the JLJB than previously thought.

6.3. Magma sources 6.3.1. Hupiyu pluton A-type granitoids have been suggested to be variously derived from (1) differentiation of mantle-derived magma or the partial melting of

Table 6 Major (%) and trace elements (10−6) compositions for gneissic granitoids. Pluton

Hupiyu

Fangjiaweizi

Sample No.

DHP-3

DHP-4

DHP-6

DHP-5

NHP-11

DTY-5

DTY-7

DTY-8

DTY-9

DTY-10

DTY-11

SiO2 TiO2 Al2O3 Fe2O3T MnO MgO CaO Na2O K2O P2O5 LOI Total K2O/Na2O A/CNK Mg# Ba Rb Sr Zr Nb Cr Y Cs Ta Hf V U Th Ga La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu ΣREE LREE/HREE (La/Yb)N (La/Sm)N Eu/Eu*

75.8 0.16 11.9 2.46 0.01 0.02 0.08 4.51 3.93 0.01 0.09 98.97 0.87 1.01 1.60 123 88.1 18.6 333 27.0 10 50.1 0.37 1.5 9.6 7 4.45 26.7 18 6.5 12.9 1.94 9.1 3.57 0.36 4.81 1.15 8.05 2.03 6.40 1.02 6.40 0.86 65.09 1.12 0.68 1.15 0.27

73.2 0.25 12.4 3.74 0.03 0.07 0.48 3.75 4.82 0.02 0.26 99.02 1.29 1.01 3.61 971 121.0 56.5 443 21.9 20 38.5 0.64 1.1 11.3 5 2.59 20.7 21.1 46.9 101 10.75 36.9 7.41 1.23 6.88 1.24 7.48 1.60 4.73 0.73 5.10 0.70 232.65 7.17 6.20 3.98 0.53

73.3 0.26 12.5 4.09 0.04 0.13 0.20 3.28 4.87 0.03 0.64 99.34 1.48 1.13 5.98 962 148.5 55.3 421 20.9 20 55.3 1.24 1.2 10.9 <5 2.39 21.6 23.6 70.3 147 15.75 55.3 10.65 1.64 9.38 1.66 9.72 2.04 6.16 0.91 6.22 0.78 337.51 8.15 7.62 4.15 0.50

73.2 0.24 12.3 3.86 0.03 0.10 0.21 2.88 6.04 0.02 0.26 99.14 2.1 1.05 4.93 1030 205 51.7 309 18.5 10 46.9 0.95 1.3 8.6 6 2.11 21.3 21.5 14.3 42.2 4.62 20.3 5.57 1.03 5.98 1.20 8.01 1.86 5.68 0.94 5.63 0.79 118.11 2.93 1.71 1.61 0.55

73 0.24 12.4 3.73 0.05 0.12 0.90 3.55 4.49 0.02 0.98 99.48 1.26 1.00 6.05 931 141.5 73.4 356 22.0 20 57.4 1.17 1.3 10.1 5 2.63 18.6 22.2 51.0 110 12.50 45.1 9.50 1.21 8.93 1.66 10.2 2.18 6.52 0.94 6.14 0.89 266.77 6.12 5.60 3.38 0.40

72.9 0.10 15.0 1.37 0.02 0.45 0.71 5.33 2.66 0.03 0.71 99.28 0.5 1.16 39.65 1500 143.5 658 80 3.3 30 2.8 2.13 0.2 2.7 15 0.75 1.73 18.2 2.8 7.9 0.53 1.8 0.37 0.05 0.37 0.07 0.47 0.12 0.33 0.08 0.25 0.05 15.19 7.73 7.55 4.76 0.41

72.3 0.11 14.9 1.38 0.02 0.49 1.37 5.21 2.47 0.03 0.53 98.81 0.47 1.08 41.53 1460 125 756 78 3.5 30 2.5 2.16 0.2 2.5 16 0.6 1.59 18.8 3.4 7.4 0.72 2.5 0.59 0.13 0.46 0.08 0.50 0.08 0.27 0.07 0.22 0.04 16.46 8.57 10.42 3.62 0.76

72.4 0.10 15.0 1.40 0.02 0.48 0.58 5.16 2.69 0.01 0.97 98.81 0.52 1.2 40.68 1340 117.5 462 77 2.7 20 4 1.83 0.2 2.7 10 0.9 1.62 17.4 7.7 13.0 1.64 6.2 1.26 0.19 1.06 0.16 0.82 0.13 0.51 0.06 0.37 0.04 33.14 9.52 14.03 3.84 0.50

72.7 0.10 15.2 1.23 0.01 0.22 1.11 5.10 2.65 0.02 0.83 99.17 0.52 1.14 26.35 1220 124.5 595 70 2.6 20 3 2.27 0.2 2.4 12 0.79 1.37 17.9 3.5 8.3 0.73 2.5 0.66 0.10 0.60 0.10 0.50 0.10 0.25 0.05 0.25 0.05 17.69 8.31 9.44 3.34 0.49

69.9 0.12 16.8 1.50 0.03 0.48 2.50 5.61 1.78 0.04 0.39 99.15 0.32 1.07 39.03 1305 88.1 992 82 1.5 20 2.6 4.42 0.1 2.3 15 0.43 0.65 18.6 3.7 5.8 0.82 2.8 0.51 0.16 0.58 0.08 0.47 0.08 0.29 0.06 0.28 0.05 15.68 7.30 8.91 4.56 0.90

71.3 0.10 16.2 1.41 0.03 0.44 1.75 5.49 2.06 0.03 0.56 99.37 0.38 1.12 38.43 1235 87.9 805 78 1.6 20 2.6 2.47 0.1 2.3 13 0.59 1.02 18.4 5.8 12.7 1.27 4.8 1.07 0.15 0.74 0.11 0.50 0.10 0.25 0.06 0.26 0.04 27.85 12.52 15.04 3.41 0.52

12

Dadingzi

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Fig. 10. (a) K2O vs. SiO2 and (b) aluminosity index diagrams for the Liaoji granitoid samples obtained from the Hupiyu and Simenzi areas.

mantle materials (Pearce et al., 1984; Kleemann and Twist, 1989; Eby, 1990, 1992; Kerr and Fryer, 1993; Han et al., 1997; Xu et al., 1998), (2) the mixing of crust and mantle materials (Dickin et al., 1991; Dickin, 1994; Xue et al., 2009), or (3) the partial melting of crustal material (Collins et al., 1982; Landenberger and Collins, 1996; Yang et al., 2007; Zhang et al., 2012). A-type magma has a high temperature, meaning that it is impossible that A-type granitoids are derived from differentiation of mantle-derived magma or the partial melting of mafic rocks (Wu et al., 2007a). Creaser et al. (1991) showed that it is difficult to form A-type granitoids through the partial melting of residual material. A model involving the partial melting of lower crust and crust–mantle mixing for generating A-type granites is currently the most popular (Wang et al., 2000; Su and Tang, 2005; Li et al., 2009; Zhou, 2011). Previous studies have concluded that peraluminous A-type granitoids are most likely derived from the partial melting of felsic crust (King et al., 1997; Chen et al., 1998; Bao and Zhao, 2003; Wu et al., 2007b; Jia et al., 2009; Zhou, 2011). Plagioclase and orthopyroxene are the main residual source minerals during this process (Zhang et al., 2006). According to the experiments of Patino Douce (1997), the dehydrated partial melting of felsic rocks at low pressure can produce A-type granitic magmas. Low Sr/Y ratios also imply that the Hupiyu monzogranites formed in a low-pressure environment (Zhang et al., 2006). The εHf(t) values of zircons from the Hupiyu monzogranites range from −1.77 to +7.17. Most TDM2 ages (n = 15) for the Hupiyu monzogranites range from 2814 to 2512 Ma, revealing that they were derived from the partial melting of Archean crust. One analysis yielded a TDM2 age of 2305 Ma, with an εHf(t) value of +7.17, suggesting the addition of mantle material or the remelting of juvenile crust. Although the Hupiyu pluton was derived primarily from crustal material, Hf isotope values and the presence of fine-grained diorite xenoliths in the pluton indicate the addition of mantle material during its petrogenesis

Fig. 12. Geochemical discrimination diagrams for the Liaoji granitoids (after Whalen et al., 1987).

(Eby, 1992; Liu et al., 2003; Yang et al., 2015). Mantle-derived magmatism not only provided a heat source for the melting of crustal rocks but also directly contributed material to the magmas.

6.3.2. Fangjiaweizi and Dadingzi plutons Our results show that the Fangjiaweizi and Dadingzi granodiorites in the Simenzi area have an affinity with high-alumina TTG rocks. Although high-alumina TTG rocks belong to the adakitic rock series,

Fig. 11. (a) Chondrite-normalized REE patterns (normalization values after Boynton, 1984) and (b) primitive-mantle-normalized trace element diagrams for the Liaoji granitoids (normalization values after Sun and McDonough, 1989). 13

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partial melting of Archean igneous rocks of thickened lower crust. The youngest zircon TDM2 age of 2260 Ma (with εHf(t) = +6.72) is close to its U–Pb age (2076 Ma), indicating the addition of mantle material or remelting of juvenile crust. The maximum TDM2 age of 3518 Ma (with εHf(t) = −13.04) suggests the addition of ancient (Archean) continental crust. 6.4. Tectonic setting As defined by Loiselle and Wones (1979), A-type granitoids occur along rift zones and within stable continental blocks. Such granitoids are characterized by alkaline, anhydrous, and anorogenic affinities. An increasing volume of research has shown that the chemical characteristics and tectonic setting of A-type granitoids are more complex than originally thought. Although there is a broad consensus that A-type granitoids form in extensional environments, their geodynamic setting remains the subject of debate (Maniar and Piccoli, 1989; Gu, 1990; Jin and Shen, 2015). A-type granitoids can be divided into two subtypes: A1-subtype and A2-subtype. The A1-subtype, in association with mantle plumes and hot spots, occurs along rift zones, whereas the A2-subtype occurs in extensional environments associated with post-orogenic and post-collisional stages (Eby, 1990, 1992; Hong et al., 1995). In Y–Nb–Ce and Y–Nb–3 Ga diagrams, data for samples collected from the Hupiyu pluton plot in the A2 field (Fig. 15). A2-subtype granitoids are considered to be related to magmatism along a plate margin or island arc, and are commonly associated with ophiolite belts and calc-alkaline granitoids. These granitoids represent the partial melting of crustal material following continent–continent collision or arc magmatism (Eby, 1992; Hong et al., 1995; Li et al., 2010). Data for all of the Hupiyu samples plot in the within-plate granitoid (WPG) field in tectonic discrimination diagrams (Fig. 16a and b). In contrast, data for samples from the Fangjiaweizi and Dadingzi plutons plot in the volcanic arc granitoid (VAG) field (Fig. 16a and b). Data for all samples plot in the active continental margin (ACM) field in the Schandl and Gorton (2002) diagram (Fig. 16c). However, in the Harris et al. (1986) diagram, they plot in the VAG field (Fig. 16d). Overall, the trace element data suggest that the Hupiyu, Fangjiaweizi, and Dadingzi granitoids were related to volcanic arc magmatism. As described above, the Liaoji granitoids are composed of A2-type granitoids and adakitic rocks. Although these two sets of rocks have similar crystallisation ages, they differ greatly in terms of geochemical composition. The similarity in crystallisation age suggests that these rocks formed in the same tectonic system, but the distinct geochemical compositions imply that they originated under differing temperature and pressure conditions. A2-type granitoids are widespread in the JLJB (Li and Zhao, 2007; Yang et al., 2015; Song et al., 2016). In comparison, pre-tectonic adakitic rocks are found only in the Fangjiaweizi, Dadingzi,

Fig. 13. P2O5 vs. SiO2 plot for the Fangjiaweizi and Dadingzi granodiorites (after Chappell and White, 1992).

Fig. 14. Sr/Y vs. Y plot for the Fangjiaweizi and Dadingzi granodiorites (after Defant and Drummond, 1990).

there are some differences between high-alumina TTG rocks and typical O-type adakites (Ge et al., 2002; Zhang et al., 2004; Zhang et al., 2015). Compared with O-type adakites, high-alumina TTG rocks have higher SiO2 contents and lower Mg# values, suggesting that they may be derived from a source with residual plagioclase, with little input of mantle material. The Fangjiaweizi and Dadingzi granodiorites have high Al2O3 and Sr contents, significant heavy REE depletion, and small negative Eu anomalies. These features suggest that they were derived from thickened crust and eclogite was the residual lithology (Li and Li, 2003; Zhang et al., 2006). The εHf(t) values of zircons from sample DTY-8 range from −13.04 to +6.72 (including seven negative values and three positive values). Most TDM2 ages (n = 8) range from 2865 to 2646 Ma. These findings suggest that the Fangjiaweizi granodiorites were derived mainly by the

Fig. 15. Representative ternary plots for distinguishing between A1 and A2 granitoids, showing data for the studied Hupiyu granitoid samples (after Eby, 1992). 14

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Fig. 16. Tectonic discrimination diagrams for the Liaoji granitoids (a and b after Pearce et al., 1984; c after Schandl and Gorton, 2002; d after Harris et al., 1986). WPG = within-plate granitoids, VAG = volcanic arc granitoids, syn-COLG = syn-collisional granitoids, ORG = ocean-ridge granitoids, post-COLG = post-collisional granitoids, OA = oceanic arc, ACM = active continental margins, WPVZ = within-plate volcanic zones, MORB = mid-oceanic ridge basalts.

1950–1850 Ma (Zhou et al., 2008; Liu et al., 2010, 2011a,b, 2012, 2015; Tam et al., 2011, 2012a, b, c; Li et al., 2012; Zhao et al., 2012). In addition, the rift closed model is difficult to explain in the dynamic background (Liu et al., 2015). There is broad consensus that the JLJB underwent a ∼1.9 Ga orogenic event, as inferred from the occurrence of high-pressure granulites and clockwise P–T–t paths (Liu et al., 2010, 2011a,b, 2012, 2015; Zhao et al., 2012), but its initial tectonic setting remains indeterminate. The rift-and-collision model was proposed by Zhao et al. (2012) and emphasises the tectonic transition from an early rifting event (2.2–1.9 Ga) to a subsequent arc–continent collision (1.9–1.8 Ga). Adakitic rocks in the Huanghuadian area constrain the initiation of subduction to 2.0 Ga (Wang et al., 2017b; Liu et al., 2018). However, the rift-and-collision model is still unable to explain the lack of typical rift-related igneous rocks (e.g., alkali basalt, phonolite, and pantellerite; Michel et al., 2004; Li and Chen, 2014; Wang et al., 2015) in the JLJB. Other studies have proposed that the JLJB was an arc–continent collision belt. Bai (1993) considered that the JLJB was a N–S-trending back-arc basin that developed along the margin of the Longgang massif and that the Longgang and Rangnim blocks represent different Archean continental blocks. However, the Rangnim Block is not an Archean massif but a Paleoproterozoic unit like the Liaoji Belt (Wu et al., 2016). Faure et al. (2004) refined the arc–continent collision model, suggesting that the formation of the JLJB was related to S-directed subduction beneath the Rangnim Block and that the North and South Liaohe groups belong to discrete terranes (Li et al., 2016). However, this is inconsistent with recent U–Pb zircon ages and Hf isotope data, which suggest

and Simenzi plutons. The assemblage of A2-type granitoids and adakitic rocks was most likely generated in a back-arc basin or post-orogenic setting. Taking into account the chronology, the back-arc basin setting is more reasonable.

6.5. Implications for the evolution of the Jiao–Liao–Ji Belt The JLJB has undergone complex magmatism, multiple deformation episodes, and metamorphism (Zhao et al., 2012; Liu et al., 2015; 2018; Wang et al., 2015), and several models have been proposed to explain the evolution of this belt. The intra-continental rift model was first proposed by Zhang and Yang (1988). This model is supported by: (1) the widespread A-type granitoids (Zhang and Yang, 1988; Hao et al., 2004); (2) the existence of bimodal volcanic rocks (Sun et al., 1993); (3) similar Neoarchean TTG and mafic dyke swarms in the Longgang and Rangnim blocks (Zhang and Yang, 1988); and (4) the anticlockwise metamorphic P–T–t paths of the Jingshan, South Liaohe, and Ji’an groups (Lu, 1996). However, some studies have questioned this evidence. First, most of the Liaoji granitoids are I-type rather than A-type (Chen et al., 2016). Second, the inferred bimodal volcanic rocks are actually a continuous magmatic sequence (Chen et al., 2016). Third, the Rangnim Block is composed predominantly of 1900–1800 Ma rocks, with little Archean material (Wu et al., 2016), suggesting that this block is a Paleoproterozoic orogenic belt. Fourth, the high-pressure pelitic and mafic granulites in the Jingshan, South Liaohe, and Ji’an groups show clockwise P–T–t paths, suggesting a process of subduction–collision during 15

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Fig. 17. Tectonic evolution of the JLJB (see text for details).

South Liaohe Group contains more volcanic rocks than does the North Liaohe Group, consistent with a configuration in which the South and North Liaohe groups were located near a volcanic arc and continent, respectively (Wang et al., 2015); (5) all of the boron deposits in the JLJB are found in the southern part of the belt (Wang et al., 2015), suggesting proximity to a volcanic arc, as boron enrichment is related to the presence of subduction zone fluids (Palmer, 1991; Kistler and Helvaci, 1994; Floyd et al., 1998; Peng and Palmer, 2002; Yan and Chen, 2014; Li et al., 2017); (6) the South Liaohe, Jian, and Jingshan groups record an anticlockwise metamorphic P–T–t path that developed during magmatic accretion at a continental margin, whereas the North Liaohe, Fenzishan, and Laoling groups record a clockwise P–T–t path that developed in a continental collisional belt (He and Ye, 1998; Wang et al., 2011; Zhao et al., 2012; Liu et al., 2015). On the basis of these lines of evidence, we prefer an arc–continent collisional model and a continental back-arc basin initial tectonic setting for the JLJB.

that the protoliths of the two groups are coeval and that basement rocks underlying the groups developed on the same Archean continental block (Luo et al., 2008; Zhao et al., 2012). Wang et al. (2015) proposed that the JLJB was a back-arc basin located between an eastern active continental arc (Rangnim Block) and a western Archean block (Longgang Block). Our new data, coupled with results of recent studies, are consistent with the back-arc basin closure model. This model can reasonably explain the following features of the JLJB: (1) the widespread pre-tectonic monzogranitic gneisses are A2subtype granitoids that formed in a back-arc basin or post-orogenic setting (this study); (2) the occurrence of 2.2–2.1 Ga calc-alkaline series rocks (e.g., calc-alkaline basalt, gabbro, andesite, and granitoids) suggests subduction-related arc magmatism (Peng and Palmer, 2002; Liu et al., 2013; Li and Chen, 2014; Chen et al., 2016; Meng et al., 2017a,c); (3) the assemblage of the ∼2.15 Ga A2-type granitoids and adakitic rocks indicates a continental back-arc basin setting (this study); (4) the 16

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Basaltic underplating occurred during the initial stage of back-arc extension and resulted in the formation of the Liaoji granitoids. The A2subtype granitoids were derived from thinned lower crust, whereas the adakitic granitoids were derived from thickened lower crust. Thinning of the crust was caused by back-arc extension and thickening was caused by basaltic underplating. The tectonic evolution of the JLJB can therefore be summarized as follows: (1) The continental arc stage (before 2.2 Ga) included an arc along the eastern margin of the Eastern Block of the NCC (Fig. 17a). (2) The initial stage of back-arc extension (2.2–2.1 Ga) led to the formation of the JLJB (Fig. 17b). A2-subtype and adakitic granitoids formed during this stage. (3) In later stages (2.1–1.8 Ga), the JLJB was in a stable depositional phase from 2.1 to 1.9 Ga (Fig. 17c), which was followed by arc–continent collision at ca. 1.9 Ga and post-tectonic extension from 1.9 to 1.8 Ga (Fig. 17d).

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7. Conclusions (1) The Liaoji granitoids in the JLJB of the North China Craton comprise two types of rock. The Hupiyu monzogranites formed at 2180 ± 14 Ma and have A2-subtype geochemical affinities. The Fangjiaweizi and Dadingzi granodiorites formed at 2130 ± 24 and 2173 ± 11 Ma, respectively, and have adakitic geochemical affinities. (2) The ∼2.15 Ga Hupiyu monzogranites and Fangjiaweizi and Dadingzi granodiorites were derived from thinned and thickened lower crust, respectively. (3) The assemblage of pre-tectonic adakitic and A2-subtype granitoids indicates that the JLJB was an arc–continent collisional belt and that its initial tectonic setting was a continental back-arc basin. Acknowledgements The authors are grateful to editor G.C. Zhao and two anonymous reviewers for their insightful reviews and constructive comments that led to significant improvement of the manuscript. We thank staff of the MRL Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing, China, for their instruction and help regarding zircon U–Pb and Hf isotopic analyses. We are also grateful to staff of the ALS Minerals–ALS Chemex Labs (Guangzhou, China) for their assistance with major and trace element analyses. This study was financially supported by the 3D Geological Mapping and Deep Geological Survey of the China Geological Survey under a pilot project entitled “Deep Geological Survey of the Benxi–Linjiang Area” (Project No. 1212011220247). References Andersen, T., 2002. Correction of common lead in U-Pb analyses that do not report 204Pb. Chem. Geol. 192, 59–79. Bai, J., 1993. In: The Precambrian Geology and Pb–Zn Mineralization in the Northern Margin of North China Platform. Geological Publishing House, Beijing, pp. 47–89 (in Chinese). Bao, Z.W., Zhao, Z.H., 2003. Geochemistry and tectonic setting of the Fugang aluminous A-type granite, Guangdong Province, China—a preliminary study. Geol. Geochem. 31, 52–61 (in Chinese with English abstract). Bea, F., Fershtater, G., Corretgé, L.G., 1992. The geochemistry of phosphorus in granite rocks and the effect of aluminium. Lithos 29, 43–56. Boynton, W.V., 1984. Geochemistry of the rare earth elements: meterorite studies. In: Henderson, P. (Ed.), Rare Earth Elements Geochemistry. Elsevier, Amsterdam, pp. 63–114. Chappell, B.W., White, A.J.R., 1992. I- and S-type granites in the Lachlan Fold Belt. Earth Environ. Sci. Trans. R. Soc. Edinburgh 83, 1–26. Chen, B., Li, Z., Wang, J.L., Yan, X.L., 2016. Liaodong Peninsula～2.2Ga magmatic event and its geological significance. J. Jilin Univ. (Earth Sci. Ed.) 46, 303–320 (in Chinese with English abstract). Chen, P.R., Zhang, B.T., Kong, X.G., Cai, B.C., Ling, H.F., Ni, Q.S., 1998. Geochemical characteristics and tectonic implication of Zhaibei A-type granitic intrusives in south Jiangxi Province. Acta Petrol. Sin. 14, 289–298 (in Chinese with English abstract). Collins, W.J., Beams, S.D., White, A.J.R., Chappell, B.W., 1982. Nature and origin of Atype granites with particular reference to SE Australia. Contrib. Mineral. Petrol. 80,

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