Paleoproterozoic igneous and metamorphic activities in the Jiao-Liao-Ji Belt, North China Craton, and its tectonic implications: a review

1. Introduction

The Jiao-Liao-Ji Belt (JLJB) is one of the most important Paleoproterozoic orogenic belts in the eastern part of the North China Craton (NCC) (Zhao et al., 2005) (Fig. 1). In the belt, Paleoproterozoic sedimentation, igneous and metamorphic activities occurred during 2.2-1.8 Ga. The Paleoproterozoic sedimentary rocks in the JLJB are divided into eight groups, from northeast to southwest: the Macheonryeong, Laoling, Ji’an, North and South Liaohe, Fenzishan, Jingshan, and Wuhe Groups (Fig. 1). Felsic and mafic igneous rocks with an age of 2.2-2.1 Ga widely intruded the JLJB, and 1.87-1.84 Ga porphyritic granitoids mainly intruded the southern part of the JLJB (Hao et al., 2004; Lu et al., 2004a; Li and Zhao, 2007; Lan et al., 2015; Yang et al., 2015; Song et al., 2016; Liu et al., 2017a; Wang et al., 2017c; Xu et al., 2018a; Wang et al., 2020b, 2020c, 2020d). Previous studies suggested a clockwise P-T path in the northern part of the JLJB and a counterclockwise P-T path in the southern part of the JLJB (He and Ye, 1998; Li et al., 2001b). However, recent metamorphic studies reported a clockwise P-T path in the southern part of the JLJB (Lu et al., 1996; Wang et al., 2010, 2020b; Tam et al., 2012a, 2012b, 2012c; Liu et al., 2013a, 2017c, 2019; Cai et al., 2017, 2019; Zou et al., 2017, 2019, 2020). Although studies on the JLJB have increased, the tectonic model of the belt is still not clear, and several different tectonic models have been proposed (Zhang and Yang, 1988; Bai, 1993; Faure et al., 2004; Li et al., 2011, 2017a; Zhao et al., 2012; Li and Chen, 2014; Peng et al., 2014; Yuan et al., 2015; Xu and Liu, 2019). The tectonic model in which rifting followed by collision due to closure of the rift basin model has been suggested based on metamorphism with a counterclockwise P-T path in the southern part of the JLJB and the similarities of the Precambrian basement (the Longgang and Nangrim Blocks) on both sides of the JLJB (Zhang and Yang, 1988). Continental collision after the subduction model has also been suggested based on the discovery of subduction-related igneous activities, metamorphism with a clockwise P-T path and the existence of granulites along the southern margin of the JLJB (Bai, 1993; Faure et al., 2004). It is necessary to ascertain which tectonic model is correct.

Fig. 1.

Tectonic map of the North China Craton and Koran Peninsula (modified after Zhao et al., 2012). The squares indicate the study areas. NM, Nangrim Massif; PB, Pyeongnam Basin; SS, Sangwon System; IB, Imjingang Belt; GM, Gyeonggi Massif; TB, Tabaeksan Basin; OB, Ogcheon Metamorphic Belt; YM, Yeongnam Massif; GB, Gyeongsang Basin.

In this study, the deposition age of sedimentary rocks in the JLJB was figured out by combining the detrital zircon ages in the metasedimentary rocks and intrusion and extrusion ages of igneous rocks in the JLJB in the previous studies. The review on the petrogenesis and ages of the igneous rocks and the metamorphic evolution in the JLJB were also carried out for a comprehensively interpretation on the igneous and metamorphic evolution of the JLJB. By combining these review results on the sedimentary, igneous and metamorphic rocks, we tried to ascertain which tectonic model is correct for the tectonic evolution of the JLJB.

2. Sedimentary events in the JLJB

The whole JLJB experienced a series of sedimentary events during the Paleoproterozoic. From northeast to southwest, eight groups were identified, namely, the Macheonryeong, Laoling, Ji’an, North Liaohe, South Liaohe, Fenzishan, Jingshan, and Wuhe Groups (Fig. 1: Zhao et al., 2005, 2012; Lu et al., 2006; Liu et al., 2018a). Previous studies divided these groups into two parts based on the rock type and metamorphic degree. The northern part consists of the Laoling, North Liaohe, and Fenzishan Groups, and the southern part is composed of the Ji’an, South Liaohe, and Jingshan Groups (Fig. 1).

2.1 The Macheonryeong Group

The Macheonryeong Group is located between the Nangrim and Kwanmo Massifs in the north-eastern Korean Peninsula and has a northwest-southeast direction (Liao et al., 2016) (Fig. 1). The Macheonryeong Group consists of the Songjin Formation (marble, schist, and amphibolite), the Puktaechon Formation (carbonate), and the Namdaechon Formation (terrigenous clastic rocks), from bottom to top (Paek et al., 1996). Based on the remarkable differences in rock type and metamorphism between the Songjin Formation and the Puktaechon and Namdaechon Formations, Liao et al. (2016) suggested that the Songjin Formation should be part of the Neoarchean supracrustal rocks rather than the Macheonayeong Group. The SIMS U-Pb age data show that the Puktaechon Formation was deposited after 2178 Ma and metamorphosed 1846 Ma, and the Namdaechon Formation was deposited after 2018 Ma and metamorphosed 1961 Ma (Liao et al., 2016) (Table 1).

Table 1.

Representative geochronological data of sedimentary rocks in the JLJB.

3. Magmatic events

3.1 Igneous activities during 2.2-2.1 Ga

3.1.1 Igneous activities in the Liaoji area

Igneous rocks with an age range of 2.2-2.1 Ga were widely distributed in the Liaoji area (Fig. 2; Table). In this part, we will introduce serval well studied plutons in the Liaoji area. Two felsic plutons (the Mafeng and Muniuhe plutons) are present in the northwest part of the Liaoji area. The Mafeng hornblende monzogranites, within an area of 35 km × 3 km, are located northwest of the North Liaohe Group in the Liaodong area (Wang et al., 2017c). Two studies were performed in this area, and they reported that the Mafeng pluton formed during 2.17-2.18 Ga (Li and Zhao, 2007; Wang et al., 2017c). Wang et al. (2017c) classified the Mafeng monzogranites into A-type granites, and Wang et al. (2020d) further divided them into A₂-type granites. The Muniuhe granitic plutons are located in the northwestern Liaoji area and mainly consist of granodiorite and syenogranite with no distinct boundary between them (Wang et al., 2020d). The Muniuhe plutons formed ~2.18 Ga and were metamorphosed ~1.88 Ga (Wang et al., 2020d). Based on geochemical data, Yang et al. (2015) and Wang et al. (2020d) confirmed that the Muniuhe granite could be classified as I-type granite.

Fig. 2.

Schematic diagram showing the locations of the 2.2-2.1 Ga felsic intrusions in the Liaoji area (modified after Wang et al., 2020d).

Four felsic plutons are located in the central part of the Liaoji area: the Hupiyu-Hadabei, Simenzi-Gujiabao, Qianzhuogou, and Dafangshan plutons. The Hupiyu-Hadabei pluton intruded during 2.15-2.16 Ga (Fig. 2; Table 2) (Lu et al., 2004a; Li and Zhao, 2007; Yang et al., 2015). Lu et al. (2004a) classified the Hupiyu-Hadabei plutons as A-type granite intrusions, whereas Yang et al. (2015) classified the Hupiyu-Hadabei pluton as I-type granite intrusions. The Simenzi-Gujiabao pluton intruded during 2.15-2.2 Ga (Yang et al., 2015; Song et al., 2016). Both Yang et al. (2015) and Song et al. (2016) considered the Simenzi-Gujiabao pluton an I-type granite; however, Wang et al. (2020d) suggested that they consist of both I- and A₂-type granites based on geochemical variations. The Qianzhuogou pluton is located in the northeastern part of the Liaoji area and intruded ~2.16 Ga (Lu et al., 2004b). The Dafangshan pluton is located south of the Muniuhe pluton and formed 2.14 Ga (Li and Zhao, 2007). Both the Qianzhuogou and Dafangshan plutons have been classified as A₂-type granite (Yang et al., 2015; Wang et al., 2017a, 2020d; Liu et al., 2018b).

Table 2.

Representative geochronological data of igneous rocks in the JLJB.

Two felsic plutons are located in the southeastern part of the Liaoji area, including the Jiguanshan and Laoheishan-Yongdian plutons (Fig. 2; Table 2). Li and Zhao (2007) reported that they formed at ~2.18 Ga and can be classified as A₂-type granite (Li et al., 2017a, 2017b; Teng et al., 2017).

Mafic intrusions have mostly been discovered in the middle to northern Liaoji area in the JLJB, and they intruded the Liaohe Groups during 2.08-2.15 Ga and were metamorphosed during 1.92-1.84 Ga (Meng et al., 2014; Yuan et al., 2015; Xu et al., 2018a; Wang et al., 2020b). Xu et al. (2018a) concluded that these mafic rocks formed in a subduction-related back-arc extensional environment.

3.1.2 Igneous activities in the Jiaobei area

The 2.2-2.1 Ga granitic igneous rocks intruded in two stages (~2.19-2.17 Ga and ~2.10 Ga) (Liu et al., 2011, 2014; Lan et al., 2015; Wang et al., 2020c). Mafic rocks with an age range of 2.2-2.1 Ga mainly occurred as enclaves or deformed dikes in TTG gneisses or granitic gneisses (Liu et al., 2013b). Lan et al. (2015) reported alkali feldspar granite (2193 Ma) and albite granite (2171 Ma) from the Changyi iron deposit, and they can be classified as A-type granite (Table 2). Wang et al. (2020c) reported 2.1 Ga mafic and granitic rocks in the southern part of the Jiaobei area, and these rocks are considered to have formed in a subduction-related back-arc extensional environment.

3.2 Igneous activities during 1.87-1.84 Ga

Magmatism in the age range of 1.87-1.84 Ga also occurred regionally, forming porphyritic granite and alkaline syenite, and 1.87-1.84 Ga igneous rocks are mostly distributed along the southern part of the JLJB (Fig. 3; Table 2) (Hao et al., 2004; Li and Zhao, 2007; Liu et al., 2017a; Wang et al., 2020b). The zircons in the felsic rocks give intrusion ages of 1.87-1.84 Ga without a metamorphic signature (Li and Zhao, 2007; Liu et al., 2017a; Wang et al., 2020b). Liu et al. (2017a) proposed that these rocks formed in an anorogenic environment based on their A-type character; however, Wang et al. (2020d) suggested that they were further classified into A₂-type granite and formed in a post-collisional tectonic setting by melting of the crust, which was highly enriched during subduction before the continent-continent collision.

Fig. 3.

Schematic diagram of the JLJB showing the locations of the 1.87-1.84 Ga igneous rocks including porphyritic granite and syenite. Data are from multiple sources (Lu et al., 2004a; Yang et al., 2007; Liu et al., 2017a; Wang et al., 2020b).

4. Metamorphic events

The metamorphic aspect of the JLJB has been studied for more than 20 years (Lu et al., 1996; He and Ye, 1998; Li et al., 2001b; Wang et al., 2010, 2020b; Tam et al., 2012a, 2012b, 2012c; Liu et al., 2013a, 2017c, 2019; Cai et al., 2017, 2019; Zou et al., 2017, 2019, 2020). Early studies have suggested that the northern and southern parts experienced different P-T paths (Lu et al., 1996; He and Ye, 1998; Zhao and Cawood, 2012). He and Ye (1998) reported clockwise P-T paths for the North Liaohe and Laoling Groups based on staurolite inclusions in garnet. Zhao et al. (2012) also confirmed a clockwise P-T path for the Fenzishan Group. These studies indicate a clockwise P-T path metamorphism of the northern JLJB. A counter-clockwise P-T path metamorphism of the southern part of the JLJB was suggested based on P-T estimation using a conventional geothermobarometer (Lu et al., 1996; He and Ye, 1998). However, recent studies did not support different P-T paths in the northern and southern parts of the JLJB (Wang et al., 2010, 2020b; Tam et al., 2012a, 2012b, 2012c; Liu et al., 2013a, 2017c, 2019; Cai et al., 2017, 2019; Zou et al., 2017, 2019, 2020).

4.2 Metamorphism in the Liaodong area

In the Liaodong area, Liu et al. (2017b) and Liu et al. (2019) reported clockwise P-T paths in the northern part of the South Liaohe Group (Fig. 4b). Liu et al. (2017b) reported a garnet-bearing amphibolite that intruded the Li’eryu Formation, South Liaohe Group, and then underwent three stages of metamorphism: the M1 (7.2-6.8 kbar and 600-570℃), M2 (9.8-10.1 kbar and 710-690℃), and M3 (6.1-5.2 kbar and 700-670℃) stages. The sample experienced peak metamorphism at the M2 stage and then experienced an increase in the geothermal gradient, resulting in a transition from intermediate- (M2) to low- (M3) P/T type metamorphism. Liu et al. (2017b) obtained ages of 1.96-1.94 Ga and 1.92-1.83 Ga for the peak M2 and post-peak M3 metamorphic stages, respectively, from the amphibolite sample. Liu et al. (2019) reported the M1 (7.1-6.6 kbar and 650-620℃), M2 (11-9.6 kbar and 840-790℃), M3 (6.5-6.2 kbar and 785-725℃), and M4 (5.5-4.3 kbar and 625-595℃) metamorphic stages from pelitic granulite collected from the Dashiqiao Formation in the South Liaohe Group. The sample experienced peak metamorphism at the M2 stage and post-peak metamorphism at the M3 stage. According to the P-T conditions of M2 and M3, the sample experienced an increasing geothermal gradient indicated by the transition from intermediate- (M2) to low- (M3) P/T type metamorphism. Liu et al. (2019) obtained ages of ca. 1.95 Ga and 1.85-1.84 Ga for the peak M2 (intermediate-P/T type) and post-peak M3 (low-P/T type) metamorphic stages in the granulite, respectively. Wang et al. (2021) studied two granulite facies metamorphic rocks on the southern margin of the South Liaohe Group and reported that these rocks experienced peak metamorphic conditions of 890-860℃ and 6.9- 9.2 kbar and then underwent retrograde metamorphism at 570-670℃ and 3.3-4 kbar (Fig. 4b). The SHRIMP zircons in the two granulite facies metamorphic rocks give a peak metamorphic age of ~1.87 Ga.

Fig. 4.

Metamorphic P-T path diagram of the JLJB. The arrows represent the P-T paths of Paleoproterozoic metamorphic rocks in the Jiaobei area (a) and the Liaodong and Jinan areas (b) in the JLJB from the previous studies. 1. Zhou et al. (2004); 2. Wang et al. (2010); 3. Tam et al. (2012a); 4. Tam et al. (2012b); 5. Tam et al. (2012c); 6. Liu et al. (2013a); 7. Zou et al. (2017); 8. Liu et al. (2017c); 9. Zou et al. (2019); 10. Zou et al. (2020); 11. Liu et al. (2017b); 12. Liu et al. (2019); 13 and 14. Wang et al. (2020b); 15. Cai et al. (2019); 16. Cai et al. (2017); 17 and 18. Wang et al. (2021). Metamorphic facies diagram after Oh and Liou (1998). BS, blueschist facies; EG, eclogite facies; EA, epidote-amphibolite facies; GS, greenschist facies; AM, amphibolite facies; HGR, high-pressure granulite facies; LGR, low-pressure granulite facies; And, andalusite; Ky, kyanite; Sil, sillimanite.

5. Discussion

5.3 Tectonic implications of the JLJB

The JLJB is one of the Paleoproterozoic collision belts in the NCC and is essential for understanding the evolution of the NCC and the Korean Peninsula. Several different tectonic models have been proposed in the JLJB, but the tectonic evolution is still under debate (Zhang and Yang, 1988; Bai, 1993; Faure et al., 2004; Li et al., 2011, 2017a; Zhao et al., 2012; Li and Chen, 2014; Peng et al., 2014; Yuan et al., 2015; Xu and Liu, 2019).

Zhang and Yang (1988) first suggested a rifting-collision model, which was improved by other studies (Liu et al., 1997; Li et al., 2001a, 2003, 2004, 2005, 2006, 2011). In this model, the Archean Longgang and Nangrim Blocks were considered one block, which was then separated by early Paleoproterozoic rifting. Rifting thus provided an environment for successive sedimentation and associated igneous activities. The model was proposed due to the discovery of counterclockwise P-T path metamorphism in the southern Groups (Jinshan, South Liaohe, and Ji’an Groups) in the JLJB and the widespread 2.20-2.13 Ga A-type granitoids (Lu et al., 1996; He and Ye, 1998; Li et al., 2001b). However, there are some geologic features that contradict this rifting-collision model. The clockwise P-T path in the northern Groups of the JLJB (Fenzishan, North Liaohe, and Laoling Groups) is difficult to explain by the rifting-collision model. Recently, instead of the counterclockwise P-T path, a clockwise P-T path has been confirmed in the southern part of the JLJB (Cai et al., 2017, 2019; Liu et al., 2017b, 2019; Wang et al., 2020b). Mafic igneous rocks in the JLJB have been suggested to have formed in a back-arc basin environment with enriched mid-oceanic ridge basalt (E-MORB) characteristics instead of ocean island basalt (OIB) characteristics (Cawood et al., 2012; Xu et al., 2018a, 2018b). Furthermore, Wang et al. (2020d) studied 2.2-2.13 Ga felsic igneous rocks and proposed that these igneous rocks are mainly A₂-type granites with some I-type granites, confirming a back-arc basin environment instead of a continental rift tectonic setting. Moreover, it is also difficult to explain the high-pressure (>13 kbar) pelitic granulite found in the Jiaobei area by this model (Tam et al., 2012b, 2012c; Liu et al., 2013a, 2017c; Zou et al., 2017, 2019, 2020).

Bai (1993) first introduced a continental collision and subduction model, and then the model was modified to a continent-arc-continent collision model by Faure et al. (2004). Similar models have been proposed within recent decades (He and Ye, 1998; Lu et al., 2006; Yuan et al., 2015; Chen et al., 2016; Tian et al., 2017). Zhao et al. (2012) suggested that a rift basin first developed into an ocean basin, and then the continuous extension resulted in subduction of the oceanic lithosphere, which was followed by the final continent-continent collision, forming high-pressure granulites in the Jingshan Group, JLJB. However, within the JLJB, evidence of subduction, such as suture zones or ophiolites, has not been discovered. Recently, Wang et al. (2020b) proposed a back-arc rifting tectonic setting in the Liaoji Belt during 2.18-2.11 Ga based on the coexistence of 2.18-2.14 Ga A₂- and I-type granitoids and the 2.13-2.11 Ga mafic igneous rocks formed in a back-arc basin environment. Postcollisional metamorphic and igneous activities during 1.87-1.84 Ga after the continent-continent collision along the southern margin of the JLJB also support the subduction-collision model together with the clockwise P-T path and high-pressure granulite-facies metamorphism in the JLJB (Wang et al., 2020b, 2021).

Combining the above discussion and previous studies, we suggest a subduction-collision-postcollision model. As explained in discussion 5.1 and 5.2 in the JLJB, 2.2-2.1 Ga felsic and mafic igneous activities were active under back-arc basin environments, and the deposition of the sedimentary rocks occurred ~2.20-1.86 Ga. Therefore, we propose that there was an arc-related subduction zone with a back-arc basin during 2.2- 2.1 Ga along the Liaoji Belt. Wang et al. (2020d) suggested that back-arc extension started >2.18 Ga and continuously expanded until 2.11 Ga when mafic rocks intruded the area (Fig. 5a and b). Continent-continent collision is suggested by the identification of intermediate-P/T type metamorphism during 1.97-1.90 Ga (Fig. 5c). After the collision between the two blocks, postcollisional metamorphic and igneous activities occurred during 1.87-1.84 Ga (Fig. 5d). The postcollisional metamorphism is a low-P/T type metamorphism and mainly occurred along the southern part of the JLJB with postcollisional granites. Wang et al. (2021) explained that postcollisional igneous and metamorphic activities were caused by high heat supplied from the upwelling asthenospheric mantle. The upwelling of asthenospheric mantle occurred due to slab break-off between the continental and oceanic slabs at depths where the buoyancy of the subducted continental slab became stronger than the pulling force exerted by the previously subducted oceanic slab. Near isothermal decompression of the P-T path could be additional evidence for postcollisional extension, as it reflects rapid uplift after collision. These data indicate that the southern part of the JLJB experienced a postcollisional extension (Fig. 5d).

Fig. 5.

Simplified model of the tectonic evolution of the JLJB from 2.2 Ga to ~1.84 Ga.

The subduction location and direction in the JLJB are difficult to evaluate because no suture zone or ophiolite was reported in the JLJB. Previous studies have reported widely distributed postcollisional porphyritic granites not only along the southern part of the JLJB but also in the Nangrim Massif and northern Gyeonggi Massif in the Korean Peninsula (Lee et al., 2014; Yengkhom et al., 2014). Besides, compared to the Nangrim and northern Gyeonggi Massifs, almost no 1.90-1.80 Ga postcollisional igneous and metamorphic events have been reported from the Longgang Block, indicating no slab beak-off event under the Longgang Block. These data indicate southward subduction, in which the Longgang Block subducted under the Nangrim Massif before the collision between them.

The amalgamation process along the JLJB can be figured out based on the change of metamorphic pattern and age along the JLJB as did for the Himalayan collision belt and Qinling-Dabie-Hongseong collision belt (Oh, 2010; Oh and Lee, 2018). As introduced above, the Liaodong area experienced intermediate-P/T type metamorphism during 1.95-1.96 Ga, whereas the Jiaobei area experienced intermediate-P/T metamorphism during 1.93-1.94 Ga. Based on the time difference, we proposed that the collision first occurred in the northeastern part of the JLJB and propagated towards the southwest (Fig. 6).

Fig. 6.

Cartoon diagram showing the Paleoproterozoic amalgamation of the eastern North China Craton. (a) Before 1.95 Ga, the Longgang Block subducted under the Nangrim Massif and forming an arc and back-arc basin. (b) Subduction continued, and the collision between the Longgang Block and Nangrim Massif occurred first in the northern part. (c) The collision between the Longgang Block and Nangrim Massif propagated southwards, (d) Finally the collision along the JLJB was completed.

During the collision, the continental slab subducts until the buoyancy of the continental slab became stronger than the pulling force exerted by the oceanic slab that subducted before the collision; then, slab break-off between the continental slab and oceanic slab occurs at that depth (Ernst, 2006; Oh and Lee, 2018; Wortel and Spakman, 2000). The slab break-off depth increased with an increased in the pulling force exerted by the oceanic slab, which subducted before the collision. The pulling force increases as the amount of subducted oceanic slab increases, and the amount of subducted oceanic slab can be increased as the width of the ocean between two continents increases (Oh, 2010, 2016; Oh and Lee, 2018). The peak pressures of intermediate-P/T type metamorphism in the Liaodong area were at least 3 kbar lower than those in the Jiaobei area (Liu et al., 2013a, 2017b, 2017c, 2019; Zou et al., 2017, 2019, 2020). These data indicate that the ocean between the two continental blocks was wider in the Jiaobei area than in the Liaodong area which caused slab break-off at shallower depths (~10 kbar = ~30-33 km) in the Liaodong area and deeper depths (>13 kbar = >39-43 km) in the Jiaobei area. In the Jiaobei area, the continental slab subducted to a deeper depth (>13 kbar, >39-43 km) as (1) the subduction period was 10-30 million longer and (2) there was a larger pulling force caused by the more subducted oceanic slab due to the wider ocean compared to that in the Liaoji area.

The low-P/T type metamorphism in the southern margin of the Liaoji area was the result of the high heat supplied by upwelling of the asthenospheric mantle through the opening formed by slab break-off during the postcollisional stage. The ages of low-P/T type metamorphism generally became younger from 1.89-1.87 Ga in the Jinan area through 1.87-1.85 Ga in the Liaodong area to 1.87-1.83 Ga in the Jiaobei area (Liu et al., 2017b, 2017c, 2019; Cai et al., 2019; Zou et al., 2019, 2020). These data indicate that slab break-off occurred in the Liaoji area (1.89-1.85 Ga) and then propagated to the Jiaobei area (1.87-1.83 Ga) with an increasing slab break-off depth.

Therefore, we suggest the following collision process along the JLJB. The width of the ocean between the Longgang Block and Nangrim Massif was narrower in the Liaoji area than in the Jiaobei area before the collision. Subduction occurred southeastwards along the back-arc basin during 2.2-2.11 Ga. The collision and subduction of the continental slab first occurred in the Liaoji area at ~1.95 Ga and propagated towards the Jiaobei area until ~1.93 Ga. The metamorphism related to the postcollisional event occurred ~10-30 Ma earlier in the Liaoji area with a shallower slab break-off depth (30-33 km) and propagated to the Jiaobei area, where the slab break-off occurred at deeper depths (39-43 km).

6. Conclusions

According to reviewed data and related discussion, we conclude the followings:

Igneous rocks with an age range of 2.2-2.1 Ga intruded in an arc tectonic setting with a back-arc basin in the JLJB.

Igneous intrusions with an age range of 1.87-1.84 Ga have been widely discovered along the southern part of the JLJB, and they have been suggested to have occurred under a postcollisional tectonic environment.

Clockwise P-T paths with isothermal decompression during uplift were identified in both the northern and southern JLJB. The ~1.95-1.90 Ga peak and ~1.89-1.84 Ga post-peak metamorphisms have been identified. The ~1.95-1.90 Ga metamorphism shows intermediate-P/T type metamorphic characteristics indicating a continent-continent collision tectonic environment. The ~1.89-1.84 Ga metamorphism shows low-P/T type metamorphic characteristics and occurred together with 1.87-1.84 Ga postcollisional igneous activities under a postcollisional extension environment.

Along the JLJB, the Longgang Block in the NCC subducted under the Nangrim Massif on the Korean Peninsula during 2.2-2.1 Ga. Then, the JLJB started to close and finally collided during ~1.95-1.90 Ga. After collision, the belt experienced postcollisional extension during ~1.89-1.84 Ga.

The collision between the Longgang Block and the Nangrim Massif began in the Jinan area and then propagated towards the Jiaobei area.

Acknowledgments

We sincerely thank the coeditor-in-chief (Jin-Yong Lee) and the reviewers for their valuable comments and suggestions. This work is supported by National Research Foundation of Korea (NRF) grants funded by the Korean government (NRF-2017R1A2B2011224 and NRF-2017K1A1A2013180).

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