Meso-Neoproterozoic strata and target source rocks in the North China Craton: A review

Precambrian Research 334 (2019) 105458

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Meso-Neoproterozoic strata and target source rocks in the North China Craton: A review ⁎

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Xiaoguang Liua,b, Sanzhong Lib,c, , Jian Zhanga, , Xiyao Lib,c, Shujuan Zhaob,c, Liming Daib,c, Guangzeng Wangb,c a

Guangdong Provincial Key Lab of Geodynamics and Geohazards, School of Earth Sciences and Engineering, Sun Yat-Sen University, Guangzhou 510372, PR China Key Lab of Submarine Geosciences and Prospecting Techniques, MOE, Institute for Advanced Ocean Study, College of Marine Geosciences, Ocean University of China, Qingdao 266100, PR China c Laboratories for Marine Mineral Resources and Marine Geology, National Laboratory for Marine Science and Technology, Qingdao 266237, PR China b

A R T I C LE I N FO

A B S T R A C T

Keywords: Mesoproterozoic Basin evolution North China Craton Source rock

Along with the breakup of the supercontinent Nuna and Rodinia during the Mesoproterozoic and Neoproterozoic, a series of sedimentary basins formed within or at the periphery of the ancient cratons. Under the regime of breakup of the supercontinent, these basins underwent different evolutionary history hence formed different geological elements constituting the petroleum systems. In this contribution, the distribution and the stratigraphic successions of the Meso-Neoproterozoic basins in the North China Craton (NCC) were examined, as well as the retrospective review for the mechanisms of the basin formation. The synthesized geological and geochronological data support a long-term extensional environment for the basins in the northern NCC. The Mesoproterozoic basins in the Yanshan, western Liaoning (Yan-Liao) and the Zhaertai areas formed at the intracratonic position later than that in the Bayan Obo, which possibly deposited in the continental margin. The further efforts still need to be devoted to decipher the huge controversial around the tectonic nature of the basins in the southern NCC, as well as their stratigraphic correlations with the basins in the north and central. The distribution and organic geochemical characteristics of the Mesoproterozoic source rock were also summarized. Three sets of source rock in the central NCC, namely the Chuanlinggou, Hongshuizhuang and Xiamaling Formations developed favorable geological and geochemical conditions for the generation of the hydrocarbon. While in the south, the Cuizhuang Formation was the only interval feasible for potential source rock. The progress in seismic geophysics and borehole drilling suggested the existence of the Mesoproterozoic beneath deep Ordos Basin. This open a new window for the reconstruction of the Mesoproterozoic paleogeography as well as the evaluation of the source potential of the Mesoproterozoic basins in the North China Craton.

1. Introduction Along with the development of the petroleum and gas industry, the Precambrian petroleum systems, which usually buried in deeper depth and underwent complex geological history comparing with Phanerozoic counterpart, arouse huge attention of the petroleum geologists around the world. Commercial oil seepage or potential source rocks mainly composed of the fine-grained siliciclastic rocks were also reported in Meso-Neoproterozoic basins of different cratons including India, Australia, Siberia, South America, Africa, South China and North China (Volk et al., 2003; Liu et al., 2011; Craig et al., 2013; Luo et al., 2016; Basu et al., 2017; Suslova et al., 2017). In the Yangtze areas in China,

the discovery of the Anyue giant gas field consolidated the resource potential within the Sinian-Cambrian sedimentary successions in the Upper Yangtze Craton (Du et al., 2016). Wang and Han (2012) gave a through prospective for the Meso-Neoproterozoic source potential in the NCC, which indicated the possibility for preservation of the resource play in the NCC (Wang and Han, 2012). Whereas despite the widespread Meso-Neoproterozoic sedimentary series and the occurrence of the oil seepage sourced from the Mesoproterozoic successions, there is no confirmed resource output with economic value. Thus, it need more effort to the study of the distribution and evolutionary history of the proto-basins and the geochemical property of the source rock, which is critical for the source potential evaluation.

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Corresponding authors at: Guangdong Provincial Key Lab of Geodynamics and Geohazards, School of Earth Sciences and Engineering, Sun Yat-Sen University, Guangzhou 510372, PR China (J. Zhang). Key Lab of Submarine Geosciences and Prospecting Techniques, MOE, Institute for Advanced Ocean Study, College of Marine Geosciences, Ocean University of China, Qingdao 266100, PR China (S.Z. Li). E-mail addresses: [email protected] (S. Li), [email protected] (J. Zhang). https://doi.org/10.1016/j.precamres.2019.105458 Received 9 April 2019; Received in revised form 3 September 2019; Accepted 6 September 2019 Available online 06 September 2019 0301-9268/ © 2019 Elsevier B.V. All rights reserved.

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Fig. 1. The geological division of the basement and the distribution of the Meso-Neoproterozoic of the NCC. Modified after (Liu et al., 2018a; Liu et al., 2014; Zhao et al., 2002; Zhao and Zhai, 2013).

Xiamaling formations. The research is mainly from two aspects. The first is to investigate the paleo-environment through the study on the microbial organisms or the sedimentary geological record (Lan, 2015; Shen et al., 2018; Yang et al., 2017; Li et al., 2015a; Luo et al., 2015a). The second is to investigate the assemblages of the microorganism and their potential for the source rock (Agić et al., 2017; Luo et al., 2016; Ma et al., 2017; Shi et al., 2017; Tang et al., 2016; Wang et al., 2017; Luo et al., 2015a). Despite the progresses, some critical issues are still unclear. For instance, apart from the areas in the north, central and south, there are still other areas deposited the Meso-Neoproterozoic successions in the NCC. It included the Huangqikou and Wangquankou formations in the western Ordos and Helanshan areas (Peng et al., 2018; Song et al., 2016a, b), the Sanchazi Group in the east of Liaoning Province; Weijiagou Group in the north of the Liaoning Province and the Dunzigou Group in the southwestern NCC (Yang, 2008). Therefore, the distribution of the stratigraphic successions in the whole NCC still need further investigation to give a thorough outlook on the paleogeography during the Mesoproterozoic. Moreover, controversial discussion around the tectonic setting of the basins are still ongoing (Peng et al., 2008; He et al., 2009; Zhao et al., 2009; Zhai et al., 2014; Zhai et al., 2015). The abundant geological records suggested the NCC played an important role in the configuration of the supercontinent Nuna or Columbia. The present understanding on the middle age of the Earth is insufficient to decipher the complicated evolution of the basins in the NCC. This manuscript retrospect progresses on the stratigraphy, geochronology, and paleogeography of the Meso-Neoproterozoic in the NCC, summarized the sedimentary and the organic geochemical characteristics of the successions which have potential for source rocks. From the perspective of the petroleum systems, we aimed to outline the

In the NCC, the un-metamorphic sedimentary cover distributed in the north, central, south and deep beneath the Ordos Basin based on recent geophysical data (Meng et al., 2011; Zhao et al., 2011; Zhai et al., 2014; Zhao et al., 2018). The most recent progresses of the MesoNeoproterozoic basins of the NCC were mainly on three aspects. First, the newly reported isotopic age from different formations revised the Meso-Neoproterozoic stratigraphic framework (Li et al., 2013a). Second, the tentative research on the stratigraphic pattern and paleogeography during the Meso-Neoproterozoic were conducted (Wang et al., 1985; Guan et al., 1993; Meng et al., 2011). Third, the dynamic mechanism of the formation of the basins during the breakup of the supercontinent Columbia was also studied (Zhao et al., 2003; Zhao et al., 2011; Xia et al., 2013; Zhai et al., 2014; Zhai et al., 2015). The progresses in the last decades mainly referred primarily where the basins distributed, geochronological framework as well as how these basin formed initially under a rough tectonic regime surround the NCC. In the research and exploration on the ancient petroleum systems, it is critical to know whether there is sufficient organic matter to form potential source rock, which is the fundamental factor for the petroleum occurrence. It has been well known that the eukaryotic organism has occurred and even possibly evolved into high diversification during the Paleoproterozoic (Lamb et al., 2009; Craig et al., 2013; Javaux and Lepot, 2018). Therefore, during the Meso-Neoproterozoic period, the main types of the microbial organisms for the generation and accumulation of organic matter were prokaryotic and unicellular eukaryotic organisms and they can be preserved under the anaerobic environment (Zhao et al., 2018). In the NCC, sedimentologists and organic geochemists preliminarily investigated the Mesoproterozoic formations developed black shales and mudstone including the Chuanlinggou, Hongshuizhuang and

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beddings (IMBGR, 1991). The sedimentary environment was considered as the fluvial to coastal plain and as the deposition during the initial transgression above the I-type sequence boundary (IMBGR, 1991; Li, 1996b; Qiao et al., 1991). The Zenglongchang Formation, which overlay the Shujigou Formation conformably, was mainly composed of coastal sandstone in the bottom and dolomitic limestone on the top (Li, 1996b; IMBGR, 1991). In the basal coarse-grained quartz sandstone and quartz greywacke successions, large-scale tabular cross bedding was well developed. The middle part of the Zenglongchang Formation was mainly characterized by the carbonaceous silty slate, muddy slate with interlayered quartz sandstone, enriched with wavy and lenticular cross bedding. The uppermost part whereas deposited stromatolite-bearing limestone and muddy limestone with hummocky and trough cross stratifications. Comparing with the Shujigou Formation, water depth became deeper and the carbonate platform deposition dominated during the Zenglongchang period (Qiao et al., 1991). The Agulugou Formation, with a parallel disconformity with the Zenglongchang Formation, was characterized by the lower carbonaceous slate and the upper muddy limestone (IMBGR, 1991; Li, 1996b). The limestone in the upper often developed slump structures. Its sedimentary environment was suggested of the back-platform basin in a passive continental margin (IMBGR, 1991; Li, 1996b; Qiao et al., 1991). The Liuhongwan Formation overlay the Agulugou Formation unconformably and was mainly composed of feldspathic quartz sandstone with intercalated dolomite, which deposited in deltaic environment (Qiao et al., 1991).

general framework of the basin evolution in the NCC during Mesoproterozoic to Neoproterozoic. In addition, through the sedimentary record to discuss the most possible formations that can be the source target. The information synthesized here may give some new insights about the petroleum exploration of the ancient Precambrian petroleum systems in the North China. 2. Lithology and stratigraphy of the Meso-Neoproterozoic in the NCC The Meso-Neoproterozoic in the NCC mainly outcropped in three areas as mentioned above (Fig. 1). The Meso-Neoproterozoic in the north is represented by the Langshan, Zhaertai, Bayan Obo and Huade groups, which were distributed along the Paleoproterozoic Khondalite belt in the Guyang, Bayan Obo, Shangdu and Huade areas (Zhao et al., 2011; Liu and Liu, 2015). The central NCC developed the classical Changcheng, Jixian, Qingbaikou systems and the newly awaiting system composed of the Xiamaling Formation, which was extracted from the original Neoproterozoic Qingbaikou System based on new geochronological data. The Meso-Neoproterozoic in the northeastern and central mainly distributed along with the Yanshan Mount and in the western Liaoning Province (Fig. 1). In the southern NCC, the MesoNeoproterozoic were represented by the volcanic Xiong’er Group and the overlying sedimentary series (Figs. 1, 7). There is a long-term controversy about tectonic setting of the Xiong’er Group as well as the sedimentary successions above (He et al., 2009; Peng et al., 2007; Zhai et al., 2014; Zhao et al., 2009; Zhao et al., 2011).

2.1.2. Lithology and stratigraphy of the Bayan Obo Group The Bayan Obo Group deposited further north comparing with the Zhartai Group (Fig. 2). Spatially, the Bayan Obo Group spread from Bayan Obo to Guyang areas up to 500 km in length. The Wulanbaolige Fault separated the Bayan Obo Group with the Early Paleozoic accretionary complex in the Central Asia Orogeny Belt (CAOB) to the north (Fig. 2). To the south, the Bayan Obo Group unconformably overlain the NCC basement (Fig. 2). Vertically, the Bayan Obo Group can be divided into six formations including the Dulahala, Jianshan, Halahuogete, Bilute, Baiyinbaolage, Hujiertu formations from bottom to top (Fig. 4), which were separated by two major sedimentary hiatus (Jia et al., 2002; Wang and Sun, 1996; Liu et al., 2017b). The Bayan Obo Group is characterized by terrestrial siliciclastic rocks and carbonates undergone low-grade metamorphism, somewhat similar with the Zhartai Group (Fig. 4). The lowermost Dulahala Formation was mainly composed of alternating gravel-bearing coarse feldspathic quartz sandstone and mediate-grained feldspathic quartz sandstone with interlayered lenticular quartz sandstone in the bottom (Li, 1996b; Qiao et al., 1991). Variety types of cross-beddings were found including the low-angle wedge-shaped cross stratifications, lenticular and flaser cross beddings (IMBGR, 1991). The upper part was characterized by alternating light-gray coarse quartz sandstone, carbonaceous fine-grained quartz sandstone and sandy slate. Large-scale aeolian cross bedding and mini-scale tabular cross beddings were well developed in the quartz sandstone layers, which was interpreted as the longshore sandy bar (IMBGR, 1991). The Jianshan Formation was dominated by slate with quartz sandstone in the middle and limestone on top and the lithology can be divided into three parts. The lowermost was characterized by the dark-gray silty slate with interlayered silty meta-sandstone, enriched in horizontal bedding. The lower part mainly consist dark-gray muddy slate, silty muddy slate with interlayered finegrained sandstone with horizontal bedding. Gradually upward was the silty muddy slate alternated with fine-grained meta-sandstone with interlayered mediate-grained quartz sandstone. The lower part of the Jianshan Formation showed variety types of the sedimentary structures including horizontal cross stratifications, flaser and lenticular cross bedding. The middle part of the Jianshan Formation mainly consisted of the dark-gray coarse quartz sandstone with fine-grained sandstone interlayers, enriched in the parallel bedding. The upper part whereas was composed of the muddy limestone with clastic limestone in the

2.1. Northern areas The northern part of the NCC mainly developed the Langshan, Zhaertai, Bayan Obo and Huade groups from west to east, respectively (Liu and Liu, 2015; Zhao et al., 2011; Zhao et al., 2004a). Controversy still exists around the age of the Meso-Neoproterozoic in the Langshan areas (Hu et al., 2014b; Liu et al., 2019). The most recent geochronological study suggested that the Lanshan group belongs to the Mesoproterozoic (Liu et al., 2019), while some researchers acclaimed it deposited during the Neoproterozoic (Peng et al., 2010). Comparing with the central and south areas, research extent in the northern NCC about Mesoproterozoic series are very low for the scarce outcrops and post metamorphism (Liu et al., 2018a; Meng et al., 2011). 2.1.1. Lithology and stratigraphy of the Zhaertai Group The Zhaertai Group mainly distributed in the Zhaertai Mount located at the middle part of the Paleoproterozoic Yinshan orogeny belt (Fig. 2). Its distribution can reach to the Langshan area to the west and Cahayouzhongqi area to the east (Liu et al., 2014). The Zhaertai Group distributed further south than the Bayan Obo and Huade groups, which was constrained by the Shetai-Guyang Fault to the south adjacent with the NCC basement, and to the north unconformably overlying the NCC Archean basement (Liu et al., 2018a; Qiao et al., 1991). The Zhaertai Group is a set of siliciclastic series with interlayered carbonates undergone low-grade metamorphism, which is composed of the quartzite pebbles, conglomeratic arkoses quartz sandstones, dolomitic slates (Li et al., 2007; Liu and Liu, 2015). It can be divided into four formations, namely the Shujigou, Zenglongchang, Agulugou and Liuhongwan formations in ascending order (Fig. 3). As for the geochronological framework and depositional age for the formations, it is still ambiguous and partly controversial (Gong et al., 2016; Li et al., 2007; Liu et al., 2018a; Qiao et al., 1991). Based on the regional geological survey, the lowest Shujigou Formation mainly consists of the conglomerate, pebbly quartz sandstone at the bottom, gradually into the siltstone, mudstone with intercalated quartz sandstone in the upper. The wedge-shaped and trough cross beddings were very common in the Shujigou Formation. The conglomerate discovered in the bottom often developed as lenticular 3

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Fig. 2. The tectonic division of the Mesoproterozoic basins in the northern NCC. Adopted from (Liu et al., 2018a).

distribution of the Huade Group was sporadic destructed by the later igneous intrusions (Fig. 2). The Bayan Obo and Huade group are continuous in lateral distribution, while previous geological survey adopted different scheme of geological division in different areas. For instance, in the Kangbao area, the Huade Group were divided into upper and lower sub-section and further into seven formations. While in the Shangdu area, the Mesoproterozoic was regarded as the Bayan Obo Group. Li et al. (2005) redefined the geological correlations and revised the Huade Group into the Maohuqing, Gejiaying and Sanxiatian groups in ascending order and this scheme was adopted by subsequent researchers (Hu et al., 2009; Li et al., 2005; Liu et al., 2014; Liu et al., 2018a). The Maohuqing Formation, which correlated with the Dulahala and Jianshan formations according to Li et al. (2005), mainly consists of pebbly feldspathic quartz sandstone at the bottom and two-mica quartz schist in the upper (Fig. 5). The Gejiaying Formation, which possibly correlated with the Halahuogete Formation (Li, 1996b; Li et al., 2005), was composed of marble with interlayered meta-sandstone. It can be further divided into three lithological units. The lower part was mainly characterized by the two-mica quartz schist with alternated marble, while the middle part mainly composed of the gray marble with intercalated diopsidite. The upper unit was dominated by the gray diopsidite with marble and quartzite interlayers. The uppermost Sanxiatian Formation is mainly composed of the alternating staurolitebearing two-mica quartz schist and phyllitic slate, developing swashing cross stratifications and ripple marks, consistent with the deposition in the coastal littoral zone (Fig. 5). Apart from the bottom boundary, contact between these three formations was considered as conformity (Li et al., 2005).

uppermost. The Halahuogete Formation, which overlay the Jianshan Formation unconformably, was mainly composed of limestone formed on the carbonate platform. Zhang et al (1993) proposed a scheme that divided the Halahuogete into three lithological sections. The lower part was characterized by basal pebbly feldspathic quartz sandstone and the upward quartz sandstone with intercalated slate. The middle part mainly consisted of the chert-bearing muddy limestone with intercalated coarse quartz sandstone. The upper part of the Halahuogete Formation was dominated by carbonates composed of massive silty and muddy limestone with minor quartz sandstone and slates (Zhang et al., 1993). With a conformable contact overlying the Halahuogete Formation, the Bilute Formation was mainly composed of fine-grained siliciclastic rocks. The lower part deposited dark-gray siltstone and fine-grained quartz sandstone intercalated with silty slate, developing parallel bedding and ripple marks. The lithology of the upper part transformed into the dark-gray fine-grained sandstone, siltstone in the tidal flat and the muddy slate with intercalated muddy limestone deposited in the carbonate platform. The top surface of the Bilute Formation was a subaerial unconformable surface and thus formed the weathering crust on the top of the Bilute Formation (IMBGR, 1991; Zhang et al., 1993). The Baiyinbaolage Formation was subdivided into two lithological units, with the lower unit dominated by the coarse quartz sandstone rich in cross stratification and ripple marks whereas upper part characterized by the silty slate intercalated by siltstone with flaser and lenticular bedding (IMBGR, 1991; Zhang et al., 1993). Overlying the Baiyinbaolage Formation with a parallel disconformity, the Hujiertu Formation was composed of micritic limestone interpreted as the carbonate littoral deposition (Li, 1996b).

2.2. Northeastern and central areas 2.1.3. Lithology and stratigraphy of the Huade Group The Huade Group mainly distributed in the Huade, Shangdu, Kangbao and Taipusiqi areas (Liu et al., 2018a). Laterally, the

In the northeastern and central NCC, the classical Changcheng, Jixian and Qingbaikou systems composed the Meso-Neoproterozoic 4

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Fig. 3. Generalized stratigraphic column and unit descriptions for the Zhaertai Group. Modified after (Qiao et al., 1991; Li et al., 2007; Gong et al., 2016).

sedimentary series, with the quartzitic conglomerate and sandstone with interlayered volcanic rocks in the bottom while dolomite in the upper. The deposition is successive which is reflected by the conformity between these formations (Tian, 2008). The Jixian System, which cover Changcheng System unconformably, is dominated by carbonates except for the Hongshuizhuang Formation. The Gaoyuzhuang Formation, which is in the lowest, is characterized by dolomite and dolomitic limestone with basal pebbly coarse sandstone and feldspathic quartz. The Yangzhuang Formation, overlain the Gaoyuzhuang Formation conformably, is mainly composed of thin-layered micritic dolomite. The Wumishan Formation mainly deposited chert-bearing massive dolomite in coastal or shallow marine (Luo et al., 2015b; Tian, 2008). The Hongshuizhuang Formation, successive deposition after the Wumishan period, is dominated by the silty shales and considered formed in shelf and tidal flat (Luo et al., 2016). The Tieling Formation, which overlay the Hongshuizhuang Formation conformably, can be divided into two subunits based on lithological characteristics. The lower subunit is mainly composed of thick-layered dolomite with intraclasts, the upper purple and greenish shales and the manganese-containing muddy dolomite on top. The upper subunit consist of the thin-layered dolomite and have a hiatus with the lower part (Luo et al., 2010; Su et al., 2010; Huo et al., 2012; Luo et al., 2012). The Xiamaling Formation was mainly

successions thick up to tens of thousands of meters regionally. Spatially, the Meso-Neoproterozoic mainly distributed in the south of Yanshan Mount and west of the Liaoning Province, in NE-SW trending, which was usually termed as the Yan-Liao Rift in previous literatures (Fig. 1; Wang et al., 1985). Vertically, the lowest Changcheng System was divided into the Changzhougou, Chuanlinggou, Tuanshanzi, Dahongyu formations and the Jixian System was further divided into the Gaoyuzhuang, Yangzhuang, Wumishan, Hongshuizhuang, Tieling formations, both in ascending order (Fig. 6). The geochronological framework, sedimentary characteristics and basin evolution have been investigated tentatively (Li et al., 2013a; Meng et al., 2011). The Changcheng System is characterized by siliciclastic series with intercalated carbonate and minor volcanic rocks in the upper (Fig. 6). The Changzhougou Formation, overlain the Archean Suizhong Granite or the high-grade metamorphic basement, is mainly composed of coarse quartz sandstone with normal grading in the bottom. According to lithological characteristics, the Changzhougou Fromation can be divided into two parts, with lower pebbly coarse sandstone and upper coastal glauconite-bearing mature quartz sandstone (Tian, 2008; Chen et al., 2014). The Chuanlinggou Formation is dominated by fine-grain siltstone and shales, with minor carbonates. The Tuanshanzi Formation mainly consists of the iron-bearing dolomite deposited in the tidal flat (Tian, 2008). The Dahongyu Formation is a set of volcanic and 5

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Fig. 4. Generalized stratigraphic column and unit descriptions for the Bayan Obo Group. Adopted from (Liu et al., 2017b).

top. The lowermost Dagushi Formation is characterized by basal conglomerate, coarse sandstone and the upper silty shale, which is typical for the fluvial environment and is considered as the initial deposition after the rifting (Ma, 2008). The Xushan Formation is composed of pyroxene-bearing andesite and andesite, which conformably cover the Dagushi Formation. Due to the limited distribution of the Dagushi Formation, it often overlies the Archean basement directly. The Jidanping Formation is distinct from with other formations with intermediate-acid dellenite and rhyolite, thick up to ca. 100 m. The andesite, pyroxene-bearing andesite and basaltic andesite were dominant in the Majiahe Formation, with interlayered volcanic clasts. The Ruyang or Gaoshanhe group overlie the Majiahe Formation unconformably (Fig. 7).

composed of gray to dark shales and siltstone and overlain by the Neoproterozoic quartz sandstone of the Longshan Formation unconformably (Fig. 6). 2.3. Southern areas The Meso-Neoproterozoic in the southern NCC was represented by the volcanic Xiong’er Group and overlying sedimentary series, which mainly distributed in three sub-regions, namely the XiaoqinlingLuanchuan, Mianchi-Queshan and Songshan-Jishan areas, from south to north (Fig. 7). Although research on the Xiong’er Group has lasted for more than forty years, there is still huge controversy on its duration, petrogenesis and tectonic setting (Zhao et al., 2015). The Xiong’er Group mainly distributed in the southwestern Henan, eastern Shaanxi and southern Shanxi, truncated by faults or inferred faults in a nearly triangle shape (Fig. 7, Sun et al., 1981). As a whole, the Xiong’er Group is predominantly composed of intermediate-basic volcanic with thousands meters thick and can be divided into four formations including the Dagushi, Xushan, Jidanping and Majiahe formations from bottom to

2.3.1. The Xiaoqinling-Luanchuan areas In Xiaoqinling-Luanchuan areas, the Meso-Neoproterozoic are represented by the Gaoshanhe, Guandaokou and Luanchuan groups, in which the former two belong to the Mesoproterozoic while the latter to Neoproterozoic according to the general geological survey (Ma, 2008; SXBGR, 2008; Xi and Pei, 2008). There are still different geological 6

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Fig. 5. Generalized stratigraphic column and unit descriptions for the Huade Group. Modified after (Liu et al., 2014; Liu et al., 2018a).

composed of the purple hematite-bearing and chert-bearing dolomite, which is rich in stromatolites. The Xunjiansi Formation is mainly composed of the light-gray fine-grained stromatolite-bearing dolomite, with minor greenish silty mudstone in the bottom, conformably overlain the Longjiayuan Formation. The Duguan Formation, which is characterized by pebbly silty slate in the bottom, gradually upward into the fine-grained chert-banded dolomite, covered by the Fengjiawan light-gray thick-layered micritic dolomite conformably.

division for the Gaoshanhe Group. For example, some researchers consider the Gaoshanhe as the lowest formation of the Guandaokou Group (Hu et al., 2013; Wang, 2015a). While some others suggested it as the Gaoshanhe Group or a single stratigraphic unit (Ma, 2008; Xi and Pei, 2008). The Gaoshanhe Group is mainly composed of siliciclastic rocks while the Guandaokou Group is dominated by carbonates (Fig. 8). The Gaoshanhe Group is further divided into Biegaizi, Erdaohe and Chenjiajian formations from bottom to top (Ma, 2008; Xi and Pei, 2008). The Biegaizi Formation is mainly composed of the gray thick-layered quartz sandstone with minor siltstone, bottom of which usually deposited thinlayered conglomerate and pebbly sandstone, unconformably overlain the Xiong’er Group. This formation developed abundant cross bedding structures and ripple marks, which revealed the sedimentary environment from coastal to tidal flat (Ma, 2008). The Erdaohe Formation can be further divided into two lithological parts, with lower part mainly composed of the light gray quartz sandstone, feldspathic quartz sandstone while the upper mainly light gray fine-grained dolomite bearing stromatolite. The Chenjiajian Formation is characterized by gray quartz sandstone with minor silty mudstone in the middle, which is overlain unconformably by the Longjiayuan Formation of the Guandaokou Group (Fig. 8). The deposition between the three formations is successive. The Guandaokou Group consists of four formations including Longjiayuan, Xunjiansi, Duguan and Fengjiawan formations, in ascending order (Fig. 8). The lowest Longjiayuan Formation is mainly

2.3.2. The Song-Qi areas The Wufoshan Group and the underlying Bingmagou Formation constituted the Meso-Neoproterozoic successions in the Song Mount and Qi Mount areas (Fig. 8), with the former divided into the Ma’anshan, Putaoyu, Luotuopan, Hejiazhai formations in ascending order. The Bingmagou Formation is considered as the initial deposition and its distribution is limited locally in the Jiyuan and Songshan areas (Xi and Pei, 2008). The Bingmagou Formation is considered as the alluvial to fluvial deposition and characterized by basal conglomerate, sandstone and silty shales with normal grading (Zheng et al., 2016). It covered the Archean basement unconformably and in return covered by the Wufoshan Group with a parallel disconformity. Overlying the Bingmagou Formation with a parallel disconformity, the Ma’anshan Formation was mainly composed of the light-gray quartz sandstone with minor silty shales and lenticular conglomerate. The composition of the lenticular varied from quartzite to magnetite quartzite. 7

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Fig. 6. Generalized stratigraphic column and unit descriptions for the Meso-Neoproterozoic successions in the Yan-Liao areas. Modified after (Wang et al., 1985). 8

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Fig. 7. Distribution of the Meso-Neoproterozoic successions in the southern NCC. Modified after (Wang, 2015a).

sandstone with minor shales and dolostone. The sandstone layers was glauconite-bearing and developed well ripple marks and cross stratification. The Luoyu Group, which divided into the Cuizhuang, Sanjiaotang and Luoyukou formations, received more carbonate contribution comparing with the underlying Ruyang Group. The Cuizhuang Group, which overlying the Beidajian Formation conformably, was composed of the shales with minor quartz sandstone and muddy limestone. Glauconite was well occurred in the intercalated sandstones. The depositional environment was interpreted as the shallow marine with relative static hydraulic condition (Xi and Pei, 2008). The Sanjiaotang Formation showed monotonous lithological features with quartz sandstones, with the occurrence of the wedge-shaped cross stratification and ripple marks, indicative of coastal depositional environment. The Luoyukou Formation, overlying conformably with the Sanjiaotang Formation, was characterized by the lower greenish and carbonaceous shales and upper carbonates intercalated by sandstone. The carbonate rocks in the upper was rich in stramatolite and the upper of the Luoyukou Formation was overlain by the Cambrian successions with a parallel disconformity (Xi and Pei, 2008)

The Putaoyu Formation showed monotonous lithological characterization with dominated shales intercalated by minor sandstone and carbonaceous shales, underlying by the Ma’anshan Formation with a conformity. The Luotuopan Formation, conformable with the underlying Putaoyu Formation, was characterized by monotonous quartz sandstone, with the development of horizontal stratification, wedgeshaped stratification and ripple marks. The Hejiazhai Formation, successive deposition overlying the Luotuopan Formation, was mainly composed of purple, greenish shales, limestone and dolostone, among which the carbonates containing stramatolite (Fig. 8). 2.3.3. The Mianchi-Queshan areas The Meso-Neoproterozoic in the Mianchi-Queshan areas is represented by the Ruyang and Luoyu groups (Figs. 7, 8). The Ruyang Group is mainly composed of siliciclastic series and further divided into the Yunmengshan, Baicaoping and Beidajian formations from bottom to top (Fig. 8). In the Jiyuan and Songshan areas, the lowest Yunmengshan Formation unconformably overlay the Bingmagou Formation. While in the other areas, it unconformably overlay the Xiong’er Group directly (Meng et al., 2018). The lithology of the Yunmengshan Formation was mainly characterized by the basal conglomerate and the upward lightgray quartz sandstone with intercalated shales. The composition of the basal conglomerate was mainly quartzite and andesite. The quartz sandstone in the upper part developed wedge-shaped cross stratification and ripple marks. Combining the lithological and sedimentary characterizations, the Yunmengshan Formation was interpreted as the deposition evolved from fluvial, deltaic to the coastal environment (Xi and Pei, 2008). The Baicaping Formation, which overlying the Yunmengshan Formation continuously, was mainly composed of the purple, greenish silty shales with intercalated quartz sandstones, rich in the horizontal and wavy beddings which was deposited in the littoral zone. Overlying the Baicaoping Formation with a conformity, the Beidajian Formation consisted of dominated quartz sandstone, feldspathic quartz

2.4. The Ordos basin and Helanshan areas Due to the huge thickness of the Paleozoic and Mesozoic cover, the Precambrian strata beneath the Ordos Basin was seldom studied. Recently, geophysical profile and drilling core revealed the Mesoproterozoic widely distributed beneath the Ordos basin (Chen et al., 2016; Song et al., 2016a, b; Guan et al., 2017). Seismic profiles across the Ordos Basin revealed the southwest possessed thick Mesoproterozoic successions and gradually thinner to the northeast direction (Figs. 9; 10). The strike of the major faults, which are active during the initial rifting, mainly trend in NE-SW direction (Fig. 10). This NE-SW direction actually parallel to the strike trending of the boundary faults 9

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Fig. 8. Generalized stratigraphic column and unit descriptions for the Meso-Neoproterozoic in the Xiaoqinling-Luanchuan areas. Modified after (Hu et al., 2013). YDA represents the youngest zircon age.

with the cease of the Lvliang Movements, which represented the amalgamation of the Columbia supercontinent at ca. 1850 Ma. The International Commission on Stratigraphy set the boundary between the Proterozoic and the Mesoproterozoic at ca. 1600 Ma. While recent geochronological evidences suggested the revision of the lower boundary of the Changcheng System in the Yan-Liao areas with an older age and correlated the lower boundary of the Jixian System at ca. 1600 Ma (Li et al., 2011; Peng et al., 2011; Li et al., 2013a). In that case, the boundary of the Mesoproterozoic in the international scheme actually correlated with the lower boundary of the Jixian System in China, which means the Changcheng System belongs to the Paleoproterozoic. Meanwhile, huge controversy on the petrogenesis of the Xiong’er volcanics as well as the depositional age of the sedimentary series above. The southern NCC developed the volcanism possibly related to the initial breakup of the craton (Zhao et al., 2004c). This led to the conclusion that the deposition of the southern basins was possibly earlier than that of the north (Su, 2016; Wang, 2015a). From aspects above, it suggested the asynchrony of the breakup as well as the deposition occurred not only between the basins interior of the NCC but also between the NCC and other cratons. Second, some stratigraphic successions belong to the Mesoproterozoic before were excluded based on new geochronological data available. For example, part of the deposition in the eastern NCC which originally considered as Mesoproterozoic were redefined as the Neoproterozoic now (Hu et al., 2012a; SDBGR, 1996). Third, the new evidence from the subsurface borehole and the geophysics revealed the existence of the Mesoproterozoic beneath the Ordos Basin (Zhao et al., 2018). It enable our insights on the areas which ever be dismissed and will change the outlook of the distribution of the basins in the whole NCC dramatically. Fourth, the tectonic property of basins at the interior and the margin of the NCC as well as the depositional age of the different basins were not well

in the Yanshan-Liaoxi areas during the early Mesoproterozoic, although the Mesoproterozoic beneath the Ordos Basin wedge out to the NE direction. The distribution of the Mesoproterozoic revealed by the seismic profiles is consistent with that from the borehole core drilling (Guan et al., 2017; Zhao et al., 2018). For instance, the Ningtan-1 and Zhentan-1 wells in the southwest, drilling into the Jixian System with thickness up to 600 m and 300 m, respectively, while the wells in the northeast have distinct smaller thickness which the Paleozoic or Mesozoic overlain on the Archean directly (Zhao et al., 2018). Despite the consolidation of its existence, depositional age, geological division and stratigraphic succession of the Mesoproterozoic beneath the Ordos Basin are far from clear. No publication about the sedimentary characteristics of the Mesoproterozoic beneath the Ordos basin was reported, neither confirmed isotopic age. Whether these successions have the similar divisional scheme with those in the Yanshan-Liaoxi areas or in the southern NCC, it is unclear until to date. 3. The paleogeography and basin evolution of the NCC In 1980s, a remarkable milestone on the reconstruction of the paleogeography of the Meso-Neoproterozoic NCC were along with the publication of atlas of the paleogeography of China (Wang et al., 1985). In this contribution, it reconstructed the paleogeography within different periods as well as the tectonic setting of the basins, in spite of the scarce geochronological, geophysical and borehole information (Wang et al., 1985). Although recent studies have witnessed huge progresses, understanding on the Mesoproterozoic paleogeography of the NCC were hindered for many reasons. First, long disagreement about initial of the Meso-Neoproterozoic deposition of the NCC. Originally, many Chinese geologists consider the initial sedimentary cover simultaneous 10

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Fig. 9. The remnant thickness and the faults distribution of the Mesoproterozoic beneath the Ordos Basin. Modified after (Guan et al., 2017).

respectively. New geochronological data enable a new geochronological framework in the northern NCC. For instance, the age of the rapakivi granites overlay by the Changcheng System unconformably was dated at ca. 1.65 Ga (Gao et al., 2008c; Li et al., 2011; Yang et al., 2005). Whereas some others though the dating of the mafic sills at ca 1731 Ma preferred a slighter older age for the lower boundary of the Changcheng System (Peng et al., 2011). Together with the detrital zircon or monazite U-Pb age of the overlying sedimentary series (He et al., 2011; Wan et al., 2003; Zhang et al., 2015c), what seems more convinced is that the Mesoproterozoic basins in the Yanshan-Liaoxi areas occurred earlier than that in the southern NCC (Peng et al., 2011;

constrained. This further limited our understanding on the basin evolution under global tectonic regime during Meso-Neoproterozoic. 3.1. Northern and central basins 3.1.1. Chronostratigraphic framework In the Yanshan-Liaoxi areas, last two decades witnessed significant progresses in the chronostratigraphy (Lu et al., 2010; Niu et al., 2013; Peng et al., 2011; Gao et al., 2008c; Geng and Lu, 2014). The geochronological advances in the northern NCC and the Yanshan-Liaoxi areas in the northeastern NCC were compiled into the Tables 1 and 2, 11

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Fig. 10. Seismic profiles crossed the Ordos Basin. The position of the seismic lines was labeled in the Fig. 11.

Table 1 Summarization of the geochronological data in the northern NCC. Units

Lithology

Agea

Dating methods

References

Zhaertai Group

basalt quartz sandstone (Shujigou Fm.) quartz sandstone (Shujigou Fm.) meta-sandstone (Agulugou Fm.) quartz schist (Liuhongwan Fm.) carbonatite black schist slate (H9) sandstone (Dulahala Fm.) graywacke (Jianshan Fm.) calcic sandstone (Halahuogete Fm.) quartz sandstone (H4) limestone sandstone (Dulahala Fm.) slate (Halahuogete Fm.) siltstone (Bilute Fm.) calcic sandstone (Hujiertu Fm.) gabbro (intruding Dulahafa Fm.) gabbro (intruding Bilute Fm.) quartz sandstone (Baiyinbaolage Fm.) carbonatite phyllitic slate (Sanxiatian Fm.) quartz schist (Maohuqing Fm.) quartzite (Gejiaying Fm.) quartzite (Sanxiatian Fm.) quartz sandstone (Maohuqing Fm.) quartzite (Sanxiatian Fm.) granite granite granite

1734 ± 7 Ma 2423 Ma 1732 Ma 1767 Ma 1746 Ma 1337 ± 51 Ma 1450 ± 51 Ma 1502 ± 12 Ma 1769 Ma 1847 Ma 1680 Ma 1761 ± 44 Ma 1694 ± 45 Ma 1827 ± 33 Ma 1350 Ma 1524 Ma 1013 Ma 1670 ± 14 Ma 1342 ± 9 Ma 1183 Ma 1417 ± 19 Ma 1336 ± 15 Ma 1855 Ma 1847 Ma 1444 Ma 1758 ± 7 Ma 1457 ± 28 Ma 1324 ± 14 Ma 1330 ± 12 Ma 1331 ± 11 Ma

LA-ICP-MS ID-TIMS LA-ICP-MS LA-ICP-MS LA-ICP-MS SHRIMP Re-Os isochron Hf model age LA-ICP-MS LA-ICP-MS LA-ICP-MS LA-ICP-MS Pb-Pb isochron SHRIMP LA-ICP-MS LA-ICP-MS LA-ICP-MS LA-ICP-MS LA-ICP-MS LA-ICP-MS ID-TIMS LA-ICP-MS LA-ICP-MS LA-ICP-MS LA-ICP-MS LA-ICP-MS LA-ICP-MS LA-ICP-MS LA-ICP-MS LA-ICP-MS

Li et al. (2007) Li et al. (2007) Gong et al. (2016) Gong et al. (2016) Gong et al. (2016) Liu et al. (2018b) Liu et al. (2016) Lai et al. (2015) Zhong et al. (2015) Zhong et al. (2015) Zhong et al. (2015) Yang et al. (2012) Yang et al. (2012) Ma et al. (2014) Liu et al. (2017b) Liu et al. (2017b) Liu et al. (2017b) Zhou et al. (2016) Zhou et al. (2016) Wang (2015b) Fan et al. (2014) Liu et al. (2018a) Liu et al. (2014) Liu et al. (2014) Liu et al. (2014) )Hu et al. (2009) )Hu et al. (2009) Zhang et al. (2012b) Zhang et al. (2012b) Zhang et al. (2012b)

Bayan Obo Group

Huade Group

a

The age of the sandstone chosen as the youngest of the single-grain zircon age. 12

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Table 2 Summarization of the geochronological data in the northeastern and central NCC. Units

Lithology

Agea

Dating methods

References

Changcheng System

mafic sills mafic sills mafic sills anorthosite anorthosite anorthosite rapakivi granite rapakivi granite rapakivi granite volcanic tuff (Chuanlinggou Fm.) mafic sills (Chuanlinggou Fm.) dioritic dyke (Chuanlinggou Fm.) potassium volcanic (Tuanshanzi Fm.) volcanic (Dahongyu Fm.) volcanic (Dahongyu Fm.) alkline basalt (Dahongyu Fm.) volcanic tuff (Gaoyuzhuang Fm.) volcanic tuff (Gaoyuzhuang Fm.) volcanic tuff (Wumishan Fm.) mafic sills (Wumishan Fm.) diabase sills (Wumishan Fm.) diabase sills (Wumishan Fm.) bentonite (Tieling Fm.) bentonite (Tieling Fm.) diabase sills (Tieling Fm.) bentonite (Xiamaling Fm.) bentonite (Xiamaling Fm.) bentonite (Xiamaling Fm.) bentonite (Xiamaling Fm.) bentonite (Xiamaling Fm.) diabase (Xiamaling Fm.) diabase (Xiamaling Fm.)

1778 ± 3 1769.1 ± 2.5 1781–1765 Ma 1693 ± 7 Ma 1715 ± 6 Ma 1726 ± 9 Ma 1679 ± 10 Ma 1685 ± 15 Ma 1673 ± 10 Ma 1621 ± 12 Ma 1620 ± 9 Ma 1634 ± 9 Ma 1637 ± 15 Ma 1625.3 ± 6.2 Ma 1625.9 ± 8.9 Ma 1624 ± 9 Ma 1559 ± 12 Ma 1577 ± 12 Ma 1483 ± 13 Ma 1345 ± 12 Ma 1324 ± 5 Ma 1323 ± 11 Ma 1437 ± 21 Ma 1439 ± 14 Ma 1316 ± 37 Ma 1379 ± 12 Ma 1372 ± 18 Ma 1368 ± 12 Ma 1370 ± 11 Ma 1366 ± 9 Ma 1320 ± 6 Ma 1325 ± 5 Ma

SHRIMP TIMS Ar-Ar TIMS TIMS SHRIMP LA-ICP-MS SHRIMP LA-ICP-MS SHRIMP SHRIMP LA-ICP-MS LA-ICP-MS LA-ICP-MS SHRIMP SHRIMP SHRIMP LA-ICP-MS SHRIMP LA-ICP-MS SIMS SHRIMP SHRIMP SHRIMP SIMS SHRIMP SHRIMP SHRIMP SHRIMP SHRIMP ID-TIMS SIMS

Peng et al. (2005) Li et al. (2001) Liao et al. (2003) Zhao et al. (2004b) Zhao et al. (2004b) Zhang et al. (2007) Yang et al. (2005) Gao et al. (2008c) Li et al. (2011) Sun et al. (2013) Zhang et al. (2015a) Zhang et al. (2013) Zhang et al. (2013) Lu and Li (1991) Gao et al. (2008b) Zhang et al. (2015a) Li et al. (2010) Tian et al. (2015) Li et al. (2014) Zhang et al. (2009) Zhang et al. (2012b) Zhang et al. (2012b) Su et al. (2010) Li et al. (2014) Zhang et al. (2012b) Su et al. (2008) Su et al. (2010) Gao et al. (2007) Gao et al. (2008a) Gao et al. (2008b) Li et al. (2009) Zhang et al. (2012b)

Jixian System

Newly-built System

a

The age of the sandstone chosen as the youngest of the single-grain zircon age

of the upper boundary no older than ca. 1330 Ma (Li et al., 2009; Zhang et al., 2017; Zhang et al., 2018b). Combined these new geochronological reports, the Xiamaling Formation was suggested to be deposited during 1400–1300 Ma, and the hiatus between it and overlying Longshan Formation may last about 300 Ma (Qiao and Wang, 2014). Above all, main progresses of the chronostratigraphy in the Yanshan-Liaoxi areas concentrate on three aspects. First, the duration of the Changcheng System was constraint approximately 1650 Ma (1731 Ma)–1600 Ma, correlated with the Statherian. Second, the boundary between the Changchang and Jixian systems was at the base of the Gaoyuzhuang Formation at ca. 1600 Ma and the Jixian System correlate with the Calymmian. Third, the Xiamaling Formation was excluded from the Neoproterozoic Qingbaikou System and its duration was from 1400 Ma to 1300 Ma. There is about 300 Ma hiatus with overlying Neoproterozoic Qingbaikou System. Comparing with the Yanshan-Liaoxi areas, the northern basins lack volcanic rocks for precise dating of the deposition, especially the Zhaertai and Huade groups. With the development of the zircon chronology, more researchers use the detrital zircon as the proxy for minimum depositional age. However, in some cases, this on the contrary increase the ambiguity. For instance, Qiao et al (1991) built the geological correlation between the Zhaertai and Bayan Obo groups based on the sequence stratigraphic theory (Qiao et al., 1991). While some researchers acclaimed a different scheme according to zircon ages in the Zhaertai Group (Gong et al., 2016). Actually, inadequacy in sediment dating always limited the research on the integrated tectonosedimentary evolution of the rift basins (Gawthorpe and Leeder, 2000). Recently, a synthesized geochronological framework were built based on compilation of the detrital zircon dataset in the northern margin of the NCC, which gave a general geochronological correlation in the Zhaertai, Bayan Obo, Huade and Yanliao areas (Fig. 11; Liu et al., 2018a).

Zhao et al., 2015). Tuff from the Chuanlinggou Formation yield age of 1621 ± 12 Ma (Sun et al., 2013). While the dioritic porphyrite and mafic dykes intruding the Chuanlinggou Formation yield ages of 1634 ± 9 Ma and 1620 ± 9 Ma, respectively (Zhang et al., 2013; Zhang et al., 2015a). Some researchers yield the zircon age of 1683 ± 67 Ma for the potassium-rich volcanics in the Tuanshanzi Formation (Li et al., 1995). While recent study yielded a younger age at ca. 1637 ± 15 Ma (Zhang et al., 2013). The alkaline volcanics in the Dahongyu Formation yield ages of ca. 1625 Ma (Gao et al., 2008b; Lu and Li, 1991; Zhang et al., 2015a). The tuff from the Gaoyuzhuang Formation yield age of ca. 1560 Ma (Li et al., 2010; Tian et al., 2015). Considering the uniformity between the Gaoyuzhuang and Dahongyu Formations, now the consensus is that the Gaoyuzhuang Formations should belong to the Jixian Group and its lower boundary is possibly with age of ca. 1600 Ma, coincide with boundary between the Mesoproterozoic and Paleoproterozoic. In that case, the Changcheng Group in the Yanshan belongs to the late Paleoproterozoic Statherian. The geochronological data in the Jixian System mainly concentrated in the Wumishan and Tieling formations. The tuffs recently discovered in the Wumishan Formation was dated at ca. 1485 Ma (Li et al., 2014). However, the mafic dykes intruding the Wumishan Formation yield age of 1345 ± 12 Ma (Zhang et al., 2009). The Tieling Formation also developed tuffs with age of ca. 1440 Ma (Su et al., 2010; Li et al., 2014). In that case, the present geochronological division regarded the boundary between Tieling and Xiamaling formations as the age of ca. 1400 Ma, coincide with the top of Calymmian. The discovery and dating of the tuffs in the Xiamaling Formation changed the geochronological framework significantly. The age of tuffs trapped in the Xiamaling Foramtion suggested the deposition of the Xiamaling Formation should be at late Mesoproterozoic rather than Neoproterozoic previously regarded (Gao et al., 2008a; Gao et al., 2008b; Gao et al., 2007; Su et al., 2008; Zhang et al., 2015b). Moreover, the mafic sills intruding into the Xiamaling Formation confined the age 13

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Fig. 11. Geochronological correlation between different Mesoproterozoic basins. Adopted from (Liu et al., 2018a).

characterized by pebbly coarse sandstone unconformably covering the Archean granites (Fig. 12). Moreover, with the high compositional and textural maturity together with wide-spreading bidirectional crossbedding, it seems to be contradictory with the traditional fluvial interpretation (Zhong et al., 2011). This feature local in the YanshanLiaoxi areas are distinct from the lower thick-layered conglomerate in the basins of southern NCC. Possibly, the Changzhougou Formation formed with the fast transgression with no adequate time and accommodation for the development of the fluvial sediments. Through the lateral variation of the stratigraphic thickness together with the recognition of the sedimentary structure induced by paleoearthquakes, previous researchers illustrated the striking of the faults at the early stage of rifting was mainly NE-trending (He et al., 2000; Song et al., 2000). This indicated the development of the basins in YanshanLiaoxi areas was with an axis of NE-trending and progressively into the north and south. The transportation of the sediments indicated the paleocurrent was mainly along the NE direction and NW direction, which is parallel and perpendicular with the axis of the Mesoproterozoic basins in the Yanshan-Liaoxi areas, respectively (He et al., 1994; Chen et al., 2014). Through the study about the composition of the sandstone at the bottom of the Changzhougou Formation combined with the paleocurrent data, Chen et al (2014) further suggested the source are intracratonic and the Yan-Liao basin are intracratonic basin. This hypothesis is consistent with the study from the perspective of the detrital zircon, in which the whole Meso-Neoproterozoic successions showed no

3.1.2. Provenance and tectono-sedimentary evolution of the basins The Mesoproterozoic in the Yanshan-Liaoxi areas were considered to be deposited in a continental rift, which was termed as the Yanliao Aulocogen in previous literatures and was widely accepted by researchers subsequently (Lu and Dai, 1989; Wen, 1989; He et al., 1994; Meng et al., 2011; Qiao and Wang, 2014; Zhai et al., 2014, 2015). The conclusion was mainly based on the thick Mesoproterozoic successions and the lack of the Mesoproterozoic oceanic crust records, which is consistent with the rift tectonic setting. The distribution of the Mesoproterozoic in the northern and central NCC indicated the rift extended to the south of Taihang Mount (Figs. 13, 14). To the north, the Zhaertai, Bayan Obo and Huade groups were considered as the deposition at the periphery of the NCC, which evolved from initial rift to the continental margin and eventually departure with another craton (Wang et al., 1985; Zhao et al., 2011). However, how the stratigraphic pattern and facies variation interior of the basins responded to the development of the rift are still vague. The Changzhougou Formation is the lowest of the Changcheng System and the initial deposition, while it is controversy on its sedimentary facies. Some researchers suggested the bottom part was in alluvial-fluvial environment, representing the basal sediments during the breakup of the NCC in the Yanshan-Liaoxi areas (He et al., 1994, 2000; Chen et al., 2014). On the contrary, some others consider the basal conglomerate formed in coastal areas (Wen, 1989; Song, 2007; Zhong et al., 2011). Actually, the conglomerate in the basal parts of the Changzhougou Formation was of centimeters thick and more

Fig. 12. Representative photos for the Changzhougou Formation in the Yan-Liao areas. 14

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Fig. 13. Diagrams illustrating the tectono-sedimentary model in the northern and central areas. Adopted from (Meng et al., 2011).

Miyun, 1680 Ma in Laiwu and eastern Hebei, the 1620 Ma in Taishan and the ca. 1330 Ma mafic dykes intruding into Xiamaling Formation (Li et al., 2015; Peng, 2010; Peng et al., 2007; Wang et al., 2016a, 2016b, Zhang et al., 2009, 2017). The ca. 1.78 Ga diabase swarms were considered as of the same source with Xiong’er Group and caused by mantle plume centered in Xiong’er rift (Peng, 2010). Some others reported diabase with different ages and discussed their nature (Li et al., 2015; C. M. Wang et al., 2016; C. Wang et al., 2016). The ca. 1.35 Ga diabase intruding into the Xiamaling or Wumishan formations were suggested to constitute a large igneous province in the central NCC and characterized the breakup of the supercontinent Columbia (Zhang et al., 2009, 2017). Recent studies suggested the earliest basins maybe formed in the southern NCC, while the Mesoproterozoic in the Yanshan-Liaoxi areas later than ca. 1650 Ma only represented the local deposition in the Yanshan-Liaoxi areas (Qiao and Wang, 2014). The U-Pb geochronological analysis on the igneous zircons of the Xiong’er Group and detrital zircon of the sedimentary series above indicated deposition in the south later than ca 1.75 Ga but prior to ca 1.6 Ga (Hu et al., 2014a; Meng et al., 2018; Zhao et al., 2004c; Wang, 2015a). These results indicated possible the basins in the south developed earlier than those in the north. As mentioned above, the distribution of the basins in the central can extend to the Taihang Mount areas. Many researchers regarded the basins as the restricted gulf as the extension of the Yanshan-Liaoxi rift into the interior of the NCC (Wang et al., 1985; Qiao and Wang, 2014). However, recent paleogeography reconstruction suggested that possibly the basins in the central and south connected in southern Taihang, Qinshui and Changzhi areas (Wang et al., 2018; Zhao et al., 2018). If so, the study on the Mesoproterozoic in this area are of vital importance to discuss the relationship of the basin in the north and south and the reconstruction of the paleogeography.

zircon input from sources out of the NCC (Wan et al., 2011). Meng et al (2011) set a good example on how to use the stratigraphic pattern and sedimentary characteristics to discuss the tectonosedimentary evolution of the Mesoproterozoic rift basins in the NCC. Their work investigated the distribution of the unconformity between the Archean basements with the overlying different formations of the Changcheng System, and revealed that transgressive unconformity between the Tuanshanzi Formation and the Archean basement represented the breakup of the NCC (Meng et al., 2011). It suggested the Yanshan-Liaoxi underwent the fault-controlled rifting in the early period and subsequent thermal decay subsidence, while the ZhartaiBayan Obo-Huade groups deposited further north and eventually evolved into a passive continental margin (Fig. 13; Meng et al., 2011). It also indicated possibly the final breakup of the NCC with another continent occurred to the north at ca. 1.6 Ga, which indicated by the breakup unconformity between the Gaoyuzhuan Formation and the basement (Meng et al., 2011). This sequential evolution was consistent with the model in which a juxtaposition of the NCC and another craton, in spite of the different cratons in these models (Zhang et al., 2012; Zhao et al., 2011; Zhang et al., 2017). This conceptual tectono-sedimentary model suggested the Mesoproterozoic in the Zhaertai and Yanshan-Liaoxi areas were deposited in the intracontinental rift while that in the Bayan Obo and Huade areas in a passive continental margin. This conclusion can be also backed up by the detrital zircon age patter of these areas, which showed that the Yanshan-Liaoxi and Zhaertai have no younger age peaks than 1600 Ma (Fig. 14; Gong et al., 2016). The magmatic activities occurred along with development of the basin in the northern and central NCC. The mafic dyke swarms with different ages were widespread in the northern and central NCC. There petrogenesis as well as the paleomagnetism were studied to shed some lights on the basin evolution. For instances, multiple mafic events during the late Paleoproterozoic to Mesoproterozoic were reported in northern NCC, including the 1780 Ma in Taihang, the 1730 Ma in 15

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the Mesoproterozoic basins in the southern NCC was compiled into the Table. 3. Most of the age reports in the Xiong’er Group is divergent on its duration. Some works on the Xiaoqinling and western Henan suggested the duration of the Xiong’er Group ranges from 1950 Ma to 1750 Ma (Huyan and Lu, 2016; Zhao et al., 2001). While some others reported younger age of 1450 Ma in the upper part and suggested a much longer duration of the Xiong’er volcanic activity (He et al., 2009; Zhao et al., 2009). As for the sedimentary series above the Xiong’er Group, recent geochronological progress mainly concentrated in the MianchiQueshan areas, where the Ruyang and Luoyu groups developed. Many researchers considered part of the Ruyang Group deposited earlier than the Changcheng System, with the evidence that youngest detrital zircon age is older than the lower boundary of the Changcheng System (Hu et al., 2014a; Li et al., 2013b; Wang, 2015a). Moreover, controversy was aroused on the depositional age of the Luoyu Group, which is above on the Ruyang Group in the geochronological column. With the dating on the tuff trapped in the Luoyu Group at ca. 1611 Ma, some researchers suggested the depositional age of the Luoyu Group was earlier than the Changcheng System in the Yanshan-Liaoxi areas (Su et al., 2012; Li et al., 2017). However, some researchers consider the Luoyu Group should correlated with the Jixian Group based on the dating on the diagenetic xenotime in the Sanjiaotang Formation (Lan et al., 2014). In the Song-Ji mounts areas, recent study indicated the youngest age of the detrital zircons in the Ma’anshan Formation, which is in the lowest of the Wufoshan Group, is older than ca. 1650 (Hu et al., 2012b; Meng et al., 2018). The Gaoshanhe and Guandaokou Groups in the XiaoqinlingLuanchuan areas (Fig. 8), the scarce geochronological data was absent because of low research extent. The only isotopic geochronological report on the Gaoshanhe Group is from the detrital zircon age of the one quartz sandstone sample (Wang, 2015a). The combination of these published data also indicate the initial deposition of the basins in the south are probably prior to that in the central. Whereas what should be noted is the limitation of the detrital zircon in the constraints on the depositional age, and whether the age from one formation can represent the whole group is still doubtable. 3.2.2. Provenance and tectono-sedimentary evolution of the basins There is long-term controversy on the tectonic setting of the southern margin of the NCC. The two schools mainly diverge from intracontinental rift to continental marginal arc (Sun et al., 1981; Qiao et al., 1985; He et al., 2009; Zhao et al., 2009; Zhai et al., 2015). The school arguing for a continental rift acclaimed that the petrology of Xiong’er volcanics showed bimodal characteristics, which is typical for the continental rift (Zhai et al., 2014). In addition, the Xiong’er Group in the Zhongtiaoshan, Xiaoshan, and Waifangshan areas was considered as the triple junction rift system and of the same magma source with the widespread ca. 17.8 Ga mafic dykes, suggesting a mantle plume model (Peng et al., 2008; Zhai et al., 2014). Another school insisted on a continental marginal arc model for the petrological and geochemical character, the erupted time showing affinity with the continental arc (He et al., 2009; Zhao et al., 2009). The tectonic setting of the Xiong’er Group closely related with the property sedimentary basins overlain. The intracontinental rift model will define the sedimentary series overlain the Xiong’er Group within rift basin, while the continental margin model indicated the basins are arc-related basins. Recent research suggested the earliest breakup of the NCC possibly occurred in the south, where the Xiong’er volcanic series manifested the early igneous event during the breakup of the Columbia at ca. 1800 Ma (Qiao and Wang, 2014; Zhai et al., 2015). It also indicated the deposition in the central Yanshan-Liaoxi areas was later than that in the south (Qiao and Wang, 2014; Zhao et al., 2015). From the perspective of the sedimentology, study referred to the stratigraphic correlation between the different geological units and the

Fig. 14. Detrital zircon compilation and comparison of the MesoNeoproterozoic between different areas in northern NCC. The data of Yanliao area from (Wan et al., 2011); the data of the Bayan Obo Group from (Hu, 2016; Liu et al., 2017; Zhong et al., 2015; Wang, 2015a); the data of the Huade Group from (Hu et al., 2009; Liu et al., 2014; Liu et al., 2018a).

3.2. Southern basins 3.2.1. Chronostratigraphic framework In the last decades, most of the studies in the southern NCC focused on the Xiong’er Group, about its duration, petrogenesis and tectonic setting. By contrast, for the lack of interlayered volcanic for precise dating, depositional age for the formations overlying the Xiong’er Group are far beyond to a consensus let alone a uniform geochronological framework across the basins. The geochronological advances of

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Table 3 Summarization of the geochronological data in the southern NCC. Units

Lithology

Age*

Dating methods

References

Xiong'er Group

basaltic andesite rhyolite pyroxene diorite dacite rhyolitic porphyry andesite Luoling granite Zhangjiaping granite diorite Shizhaigou diorite sandstone (Yunmengshan Fm.) sandstone (Baicaoping Fm.) sandstone (Yunmengshan Fm.) sandstone xenotime (Sanjiaotang Fm.) tuff (Luoyukou Fm.) tuff (Luoyukou Fm.) silty phyllite (Baishugou Fm.) sandstone quartz sandstone sandstone (Ma'anshan Fm.) sandstone (Ma'anshan Fm.) sandstone (Ma'anshan Fm.) sandstone (Bingmagou Fm.)

1750 Ma 1959 ± 44 Ma 1761 Ma 1450 ± 31 Ma 1763 ± 15 Ma 1810 ± 41 Ma 1786 ± 7 Ma 1530 Ma 1746 ± 22 Ma 1780 ± 11 Ma 1744 ± 22 Ma 1817 ± 22 Ma 1760 ± 24 Ma 1368 Ma 1611 ± 8 Ma 1638 ± 9 Ma 1164 Ma 1785 ± 15 Ma 1757 ± 23 Ma 1788 ± 14 Ma 1655 ± 22 Ma 1698 ± 47 Ma 1792 Ma

SHRIMP LA-ICP-MS TIMS LA-ICP-MS LA-ICP-MS LA-ICP-MS SIMS LA-ICP-MS LA-ICP-MS SIMS LA-ICP-MS LA-ICP-MS LA-ICP-MS SIMS LA-ICP-MS LA-ICP-MS LA-ICP-MS LA-ICP-MS LA-ICP-MS SIMS LA-ICP-MS LA-ICP-MS LA-ICP-MS

Zhao et al. (2004c) Zhao et al. (2001) Zhao et al. (2001) He et al. (2009) Wang et al. (2010) Huyan and Lu (2016) Cui et al. (2013) Deng et al. (2016) Wang et al. (2016c) Cui et al. (2011) Hu et al. (2014a) Li et al. (2013b) Wang (2015a) Lan et al. (2014) Su et al. (2012) Li et al. (2017) Liu et al. (2019) Zhu et al. (2011) Wang (2015a) Zhang et al. (2016) Hu et al. (2012b) Meng et al. (2018) Meng et al. (2018)

Ruyang Group

Luoyu Group

Guandaokou Group

Wufoshan Group

* The age of the sandstone chosen as the youngest of the single-grain zircon age

limited on the local scale. Some researchers speculated the Bingmagou Formation under the Ruyang Group recorded the paleo-environment shift from the alluvial fan to the coastal marine and the highland was at the northeast (Fig. 15; Yue et al., 2018). It also suggested that the Gaoshanhe Group in the southernmost Luanchuan area possibly can correlated with the upper part of the Bingmagou Formation (Yue et al., 2018). This evolutionary model validated the transgression from south to the north and indicated the Yunmengshan period had been in a continental marginal environment (Hu et al., 2014a). It also indirectly endorsed the continental rift model in the south margin of NCC.

basin evolution in the three sub-regions is seldom. Most of the studies concentrated on the provenance of the sediments through the method of the detrital zircon geochronology. The detrital zircons from the sandstone in the Yunmengshan Formation showed various sediment influx including the age similar with the volcanism in the Xiong’er Group (Hu et al., 2014a), which is consistent with the composition of basal conglomerate in the Yunmengshan Formation (Meng et al., 2018). This indicated directly that probably the Xiong’er volcanic rocks provided source input for the Yunmengshan Formation. While in the Song and Qi mount areas, the zircon geochronological data showed that the Wufoshan Group with exclusively older Archean detrital zircon influx (Hu et al., 2012b; Zhang et al., 2016). This is well consistent with the inference for the different tectonic positions of the Wufoshan Group and the Ruyang Group, which the former possessed a higher topography during deposition and far away from the volcanic erupted center of the Xiong’er Group (Zhou, 1999). The study on the paleogeography reconstruction were mainly

4. The hydrocarbon potential of the Meso-Neoproterozoic in the NCC 4.1. Paleo environment and source accumulation The paleo-environment, geological conditions for the fossil fuels

Fig. 15. Sedimentary model of the Bingmagou Formation on the southern margin of the North China Craton. Modified after (Yue et al., 2018). 17

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4.2. The Chuanlinggou formation

generation, accumulation and preservation of the Mesoproterozoic in the central NCC were also studied and gained much progress. As early as 90s in twentieth century, some researchers made the classification of the algal mega fossils from the Proterozoic successions of China (Du et al., 1995). The recent work suggested the Mesoproterozoic in the central NCC were rich in microfossils including the cyanobacteria, eukaryote, acritarches and even the macroalgae, which can form the potential hydrocarbon source rocks (Shi et al., 2008; Peng et al., 2009; Shi et al., 2017; Zhao et al., 2018). The flourish of the eukaryotic life during the Mesoproterozoic era were possibly related with the rising of the oxygen of the Mesoproterozoic ocean (Zhang et al., 2018a). Meanwhile, a series of sedimentary structures induced by the microbials, mainly in Chuanlinggou and Wumishan formations, indicated the activity of the microorganisms during Mesoproterozoic (Lan, 2015; Yang et al., 2017). Some researchers proposed different mechanism for the “microbial-induced” structures and consider them as the result of paleo-earthquake, which indicated the extensional settings during the Chuanlinggou period (Shi et al., 2016; Yang et al., 2017). As for the physicochemical condition of the water body, some researchers speculated the anoxic condition during deposition of the Chuanlinggou Formation (Shi et al., 2008; Tang et al., 2009), which is consistent with the low oxygen content during the Proterozoic (Tang et al., 2016; Javaux and Lepot, 2018). Whether these microbial mats have the potential for hydrocarbon generation, some researchers also have done some researches. Vertically, three set of the black shales including the Chuanlinggou Formation in the Changcheng System, the Hongshuizhuang Formation in the Jixian System and the Xiamaling Formation in the northeastern NCC (Table 4). These three formations become the objective for the investigation of the resource potential from organic geochemical perspective. For instance, some researchers consider the authigenic pyrites and sand veins as the indication for the generation of the methane during the deposition of the Chuanlingou Formation (Shi et al., 2008; Tang et al., 2009). Investigation on the Hongshuizhuang Formation revealed the organic matter, which had a lower thermal maturity in the early to middle oil window, mainly originated from prokaryotes (Luo et al., 2016). It also shows distinct differences between lower and upper part in Total Organic Carbon (TOC), with lower part higher than 1.0% (Ma et al., 2017). The oil seepage and bitumen spots were discovered in the Xiamaling Formation and considered as the most ancient oil accumulation in the NCC (Liu et al., 2011). The TOC of the organic matter in Xiamaling Formation can be as high as 16% and positively correlated with the Si content, which possibly caused by the fertilization of the thermal fluid activity (Chen and Sun, 2004). Moreover, the dominant primary producers for the accumulation of the organic matter may be the cyanobacteria (Luo et al., 2015c).

The Chuanlinggou Formation was mainly composed of silty shales with intercalated sandstone and carbonates, overlain above on the Changzhougou quartz sandstone conformably. In the west of the Yanshan mount range, the Chuanlinggou Formation is mainly siltstone with banded sandstone deposited in the littoral zone of coastal marine. While in the east of Miyun, the lithology are mainly composed of the shales with intercalated limestone in the coastal and shallow marine (Li, 1996a). The largest thickness of the Chuanlinggou Formation is in the Jixian section, which can be thick up to the 889 m, and became thinner toward south and north gradually (Cui et al., 1979). Organic geochemical characteristics revealed that the Total Organic Carbon (TOC) of the Chuanlinggou mudstone in the Jixian area ranges from 0.05% to 2.23%, with average value of 0.75%, increasing from bottom to top (Niu et al., 2015). While in the Kuancheng area, the TOC became richer up to 2.0% in average (Zhao et al., 2018). The average Ro of the Chuanlinggou Formation in the Kuanchang and Jixian areas are 2.2% and 2.03% respectively, suggesting a dry-gas stage in a high-level maturity (Table 4). 4.3. The Hongshuizhuang Formation The Hongshuizhuang Formation was mainly composed of the dark gray shales with intercalated quartz sandstone in the bottom and dolomites in the upper, enriched in microorganism and pyrite aggregation (Cui et al., 1979; Yang, 2008). The subtle horizontal bedding together with the lithological characteristics indicated the Hongshuizhuang Formation in subtidal zone under static hydraulic condition (Cui et al., 1979; Luo et al., 2016). The distribution of this formation suggested that the depo-center was possibly located in the east of the Pingquan as well as the Jixian areas, with the largest remnant thickness up to 183 m in the western Liaoning Province (Cui et al., 1979; Yang, 2008). Comparing to the Chuanlinggou Formation, the Hongshuizhuang Formation have richer TOC content while lower maturity of the organic matter (Table 4). The TOC content of the shales in the lower part ranges from 1.3% to 4.17 with average of 2.47%, which is distinctly higher than that of the upper argillaceous dolomites with the range varying from 0.15% to 1% (Ma et al., 2017). However, the maturity of organic matter in the Honngshuizhuang Formation was in a low grade with the Ro ranging from 0.68% to 0.77%, average at 0.73% (Ma et al., 2017). Some other researchers got the similar results indicated a low thermal maturity in wet oil window (Luo et al., 2014; Niu et al., 2015; Zhao et al., 2018). 4.4. The Xiamaling Formation As for the tectonic property of the Xiamaling Formation, some

Table 4 Summarization of the thickness and organic geochemical parameters of the potential source rocks in the NCC. Region

Strata

Thickness/m

TOC/%

Ro/%

Data location

Data source

Central (Yanliao)

Chuanlinggou Formation

> 240 / > 90 130 ~130 / / > 260 / < 5(not penetrated) > 40 10–30 ~100 100–300

0.6–15.0 (2.0) 0.05–2.23 (0.75) 1.0–6.0 (4.1) 0.15–4.17 (1.91) 0.9–8.0 (3.9) 0.72–3.44 (1.71) / 3.0–21.0 (5.2) 0.08 3.0–5.0 (3.6)

1.2–2.5 (2.2) 1.54–3.01 (2.03) 0.8–2.10 (1.63) 0.68–0.77 (0.73) 0.82–0.88 1.44–1.52 (1.48) 0.81–2.52 0.6–1.4 (1.1) (1.44) 1.8–2.2 (2.0)

Kuancheng in Hebei Jixian in Tianjin Kuancheng in Hebei Kuancheng in Hebei Kuancheng in Hebei Jixian in Tianjin Lingyuan in Liaoning Xiahuayuan in Hebei Jixian in Tianjin Well Tao 59

0.20–1.50 (0.52) 0.2–1.21 (0.51) 0.15–0.88 (0.35) 0.8–17.0 (3.8)

2.5–3.0 (2.6) / / 2.0–3.0 (2.2)

Yongji in Shanxi Yongji in Shanxi Luonan Guyang in Inner Mongolia

Zhao et al. (2018) Niu et al. (2015) Zhao et al. (2018) Ma et al. (2017) Luo et al. (2014, 2016) Niu et al. (2015) Liu et al. (2011) Zhao et al. (2018) Niu et al. (2015) Changqing Oil-field Company; Zhao et al. (2018) Zhao et al. (2018) Wang et al. (2018) Wang et al. (2018) Changqing Oil-field Company; Zhao et al. (2018)

Hongshuizhuang Formation

Xiamaling Formation

Ordos

Changcheng Group

South

Cuizhuang Formation

North

Chenjiajian Formation Shujigou Formation

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Mesoproterozoic source rock and reservoirs beneath the Qinshui Basin. Apart from the source and reservoirs, the available of the seals which act as the cap to prevent the scatter of accumulation of the hydrocarbon is important as well. The scarce research on this suggest that the most favorable seals for the inferred Mesoproterozoic hydrocarbon is the Cambrian fine-grained mudstones (Wang et al., 2018).

researchers suggested a retro-arc basin, mainly based on the geochemical affinity with the arc of the tuff beds in this Formation (Su et al., 2006; Qiao and Wang, 2014). This is inconsistent with the model which manifest long-term extension in the central and north NCC. Despite the controversy above, the Xiamaling Formation still became the objective for the potential source rock. Most recent research even suggested the possible oldest oil accumulation was discovered in the Xiamaling Formation in the North China (Liu et al., 2011). The Xiamaling Formation was mainly composed of the grey, greenish, darkgrey shales and siltstone, with the depo-center in the east of Huailai and southwest of Chengde areas from the distribution (Cui et al., 1979). The largest thickness of the Xiamaling Formation was in the Zhuolu and Huailai areas, which can be thick up to 500 m (Li, 1996a). From the perspective of the organic geochemistry, the scarce data report indicated the TOC content of Xiamaling Formation in different areas varies distinctly. For instances, in the Xiahuayuan in the Zhangjiakou area, the TOC content ranges from 3.0% to 21.0%, with average value of 5.2% (Zhao et al., 2018). While in the Jixian area, the TOC content is only about 0.08% in average (Niu et al., 2015). As for the maturity, the Ro of the samples of the Xiamaling Formation is mostly larger than 1% and fall into the wet-gas zone (Niu et al., 2015). In the other areas, including the southern and northern NCC, deep in the Ordos basin, the study about the source rock evaluation are very rare. In the south, the Cuizhuang Formation of the Luoyu Group in the Yongji areas showed variation of the TOC ranges from 0.2% to 1.5% with average of 0.52%, whereas the maturity characterized by the Ro revealed it at a high level (Wang et al., 2018; Zhao et al., 2018). In the deep of the Ordos basin, even less data from the boreholes drilled into Mesoproterozoic successions showed it still have the source potential from the richness of the organic matter and the maturity (Zhao et al., 2018).

Acknowledgement We are grateful to Editor Professor Zhao and three anonymous reviewers for their thoughtful comments. This research was financially funded by the National Key Research and Development Program of China (No. 2016YFC0601002), National Science and Technology Major Project (No. 2016ZX05004001-003), Fundamental Research Funds for the Central Universities (No. 32110-31650011), National Natural Science Foundation of China (No. 41772214, 41602042 and 41702206). This study was also supported by Aoshan Talents Program from Qingdao National Laboratory for Marine Science and Technology to Prof. Sanzhong Li (No. 2015ASTP-0S10) and the Taishan Scholar Program to Prof. Sanzhong Li. References Agić, H., Moczydłowska, M., Yin, L.M., 2017. Diversity of organic-walled microfossils from the Early Mesoproterozoic Ruyang Group, North China Craton-a Window into the Early Eukaryote Evolution. Precambrian Res. 297, 101–130. Basu, H., Dandele, P.S., Kumar, K.R., Achar, K.K., Umamaheswar, K., 2017. Geochemistry of Black Shales from the Mesoproterozoic Srisailam Formation, Cuddapah Basin, India: implications for Provenance, Palaeoweathering, Tectonics, and Timing of Columbia Breakup. Chem. Erde 77 (4), 596–613. Chen, J.F., Sun, S.L., 2004. Preliminary study of geochemical characteristics and formation of organic matter rich Stratigraphy of Xiamaling Formation of Later Proterozoic in North China. Nat. Gas Geosci. 02, 110–114 (in Chinese with English abstract). Chen, X., Zhang, C.H., Liu, J.J., Te, G.S., 2014. Fluvial facies in the Changzhougou Formation in the Jixian area of China and geological Significance. J. Stratigr. 02, 236–244. Chen, Y.Z., Fu, J.H., Yang, G.Y., Xiao, A.C., Sun, L.Y., Xu, B., Bao, H.P., Mao, L.G., 2016. Researches on basin property of ordos block during mesoproterozoic Changcheng Period. Acta Petrol. Sin. 03, 856–864 in Chinese with English abstract. Craig, J., Biffi, U., Galimberti, R.F., Ghori, K.A.R., Gorter, J.D., Hakhoo, N., Le Heron, D.P., Thurow, J., Vecoli, M., 2013. The palaeobiology and geochemistry of Precambrian Hydrocarbon Source Rocks. Mar. Petrol. Geol. 40, 1–47. Cui, M.L., Zhang, B.L., Zhang, L.C., 2011. U-Pb dating of baddeleyite and zircon from the Shizhaigou diorite in the southern margin of North China Craton: constrains on the timing and tectonic setting of the Paleoproterozoic Xiong'er group. Gondwana Res. 20 (1SI), 184–193. Cui, M.L., Zhang, L.C., Zhang, B.Y., Zhu, M.T., 2013. Geochemistry of 1.78Ga A-type granites along the southern margin of the North China Craton: implications for Xiong'er magmatism during the break-up of the supercontinent Columbia. Int. Geol. Rev. 55 (04), 496–509. Cui, S.Q., Yang, Z.S., Qiu, G.L., Ge, X.H., 1979. The Lithofacies Paleogeographic Evolution of the Late Proterozoic in the Yanshan Areas. J. Jilin Univ. (Earth Sci. Ed.) 04, 29–52 (in Chinese). Deng, X.Q., Zhao, T.P., Peng, T.P., 2016. Age and geochemistry of the early Mesoproterozoic A-type granites in the southern margin of the North China Craton: constraints on their petrogenesis and tectonic implications. Precambr. Res. 283, 68–88. Du, J.H., Wang, Z.C., Zou, C.N., Xu, C.C., Shen, P., Zhang, B.M., Jiang, H., Huang, S.P., 2016. Discovery of Intra-Cratonic Rift in the Upper Yangtze and its Control Effect on the Formation of Anyue Giant Gas Field. Acta Petrol. Sin. 01, 1–16. Du, R.L., Wang, Q.Z., Tian, L.F., 1995. Catalogue of Algal Megafossils from the Proterozoic of China. Precambr. Res. 73 (1), 291–298. Fan, H.R., Hu, F.F., Yang, K.F., Franco, P., Liu, X., Wang, K.Y., 2014. Integrated U-Pb and Sm–Nd geochronology for a REE-rich carbonatite dyke at the giant Bayan Obo REE deposit, Northern China. Ore Geol. Rev. 63, 510–519. Frolov, S.V., Akhmanov, G.G., Bakay, E.A., Lubnina, N.V., Korobova, N.I., Karnyushina, E.E., Kozlova, E.V., 2015. Meso-Neoproterozoic Petroleum Systems of the Eastern Siberian Sedimentary Basins. Precambr. Res. 259 (SI), 95–113. Gao, W., Zhang, C.H., Gao, L.Z., Shi, X.Y., Liu, Y.M., Song, B., 2008c. Zircon SHRIMP U-Pb Age of Rapakivi Granite in Miyun, Beijing, China and its Tectono-Stratigraphic Implications. Geol. Bull. China 06, 793–798. Gao, L.Z., Zhang, C.H., Shi, X.Y., Song, B., Wang, Z.Q., Liu, Y.M., 2008a. Mesoproterozoic Age for Xiamaling Formation in North China Plate Indicated by Zircon SHRIMP Dating. Chin. Sci. Bull. 21, 2617–2623 (in Chinese with English abstract). Gao, L.Z., Zhang, C.H., Shi, X.Y., Zhou, H.R., Wang, Z.Q., 2007. Zircon SHRIMP U-Pb Dating of the Tuff Bed in the Xiamaling Formation of Qingbaikou System in North China. Geol. Bull. China 03, 249–255 (in Chinese with English abstract). Gao, L.Z., Zhang, C.H., Yin, C.Y., Shi, X., Wang, Z.Q., Liu, Y.M., Liu, P.J., Tang, F., Song, B., 2008b. SHRIMP Zircon Ages: basis for Refining the Chronostratigraphic

5. Prospect for Precambrian resource potential The spatial and temporal distribution of hydrocarbon preservation was controlled by tectonic, paleogeography and biogeochemical history of Proterozoic supercontinents during their accretion, amalgamation and the breakup (Craig et al., 2013; Frolov et al., 2015). The present industrial resource output in China was merely exploited in the South China, whilst mainly in the Ediacaran System of the Neoproterozoic (Du et al., 2016). As for the evaluation of hydrocarbon potential of the Mesoproterozoic in the NCC progressed slowly. The problems included the distribution of the Mesoproterozoic source rock, the organic property for the hydrocarbon generation, the availability of reservoir as well as the post preservation of the reservoirs. The difficulties for the Precambrian resource investigation mainly reside in that the multi-stage tectonic movements ruined the original integrity of geological preservations. This leads to the uncertainty on the paleogeography reconstruction as well as the prediction on ancient reservoir. For instance, in the Qinshui Basin, joint of the Yan-liao rift and southern Mesoproterozoic basins, was inferred to preserve the Mesoproterozoic record in the deep despite no borehole drilling consolidating this conclusion (Wang et al., 2018; Zhao et al., 2018). Solely from the organic geochemical perspective, three set of source rock series, namely Chuanlinggou, Hongshuizhuang and Xiamaling formations showed hydrocarbon potential while their distribution especially under the subsurface was not well understood. Based on the present data available, these three formations all possessed relative considerable vertical thickness and chemical parameters, especially in the central Yan-liao areas (Cui et al., 1979; Zhao et al., 2018). Specifically, the Hongshuizhuang Formation in the Calymmian (Jixian System), the lower part in particular, showed relative continuous thickness and enrichment of the organic matter (Ma et al., 2017). Additionally, the Cuizhuang Formation in the southern basin also possessed valid source rock in spite of the relative lean TOC (Wang et al., 2018). To some extent, it further efforts is worthy devoted to confirm the development of the 19

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