Figure
1.
Regional geological map of the Siziwangqi area, Inner Mongolia (modified after Zhao et al., 1999 and our field observations). Fm. Formation.
| Citation: | Yueshuang Du, Zhiguang Zhou, Guosheng Wang, Chen Wu, Wenchao Xu. Druse Calcite Crystals Formed by Mesoproterozoic Paleo-Earthquake Activity in the Northern Margin of the North China Craton. Journal of Earth Science, 2024, 35(2): 514-524. doi: 10.1007/s12583-021-1416-0
|
The Meso-neoproterozoic Bayan Obo rift is located along the northern margin of the North China Craton, and was associated with the break-up of the Columbia supercontinent. During rift evolution, syn-sedimentary deformation occurred due to tectonic activity and earthquakes. Seismic events are recorded in the Jianshan Formation of the Bayan Obo Group, Inner Mongolia, as soft sediment deformation structures in the central Bayan Obo rift. Druse calcite crystals and collapse breccias in the Jianshan Formation may provide information on the rift evolution. The druse calcite crystals are idiomorphic-columnar in shape and associated with graphite, pyrite, and quartz. δ13C values of the graphite are -20‰, indicative of biogenic deoxygenation and formation in water. The druse calcite crystals are inorganic in origin and formed in water at a temperature of 55 ℃, based on calcite δ13C and δ18O data. The calcite grew in paleo-caves containing fault breccias, with heat derived from faulting. As such, the druse calcite crystals are important evidence for seismic events. The collapse breccias (i.e., fault breccias) and other indicators of slip show that displacement occurred from NE to SW, which is different from the paleocurrent direction in the Jianshan Formation. The thickness of the collapse breccia is ~200 m, which represents the height of the fault scarp. The strike of the fault scarp was NE-SW, based on the distribution of the collapse breccia. The Bayan Obo and Yanliao rifts experienced rapid NW-SE extension, and developed similar deformation structures at ca. 1.6 Ga related to break-up of the Columbia supercontinent.
The North China Craton (NCC) was involved in the Mesoproterozoic break-up of the Columbia supercontinent (e.g., Wang et al., 2019; Kusky et al., 2018, 2016; Wu et al., 2018, 2016a; Liu and Liu, 2015; Peng, 2010; Zhao, 2009; Hou et al., 2006; Xia et al., 2006; Zhao et al., 2005, 2002), and rift systems developed in the NCC include the Bayan Obo, Yanliao, and Xiong'er rifts (e.g., Zhai, 2004) (Figure 1). These rifts experienced seismic events and record typical seismogenic soft sediment deformation structures (SSDSs; e.g., Jiao et al., 2011; Qiao and Gao, 2007; Lü et al., 2006; Qiao et al., 2002, 1994). The SSDSs that are induced by seismic events are termed "seismites" (e.g., Rodríguez-Pascua et al., 2000; Rossetti, 1999; Lowe, 1975; Sims, 1975; Seilacher, 1969), which can provide quantitative information regarding the sedimentary and tectonic environment in which they formed (e.g., Rodríguez-Pascua et al., 2000; Mohindra and Bagati, 1996). Qiao and Gao (2007) suggested that the Yanliao rift developed due to rapid extension along the northern margin of the NCC, based on seismic records and syn-sedimentary faults. Recently, seismites were found in the Bayan Obo rift (e.g., Zhang et al., 2013; Lü et al., 2006), but its rift spatio-temporal evolution process remains unclear.
In this paper, we document for the first time typical SSDSs and druse calcite crystals in the Jianshan Formation of the Bayan Obo rift in the Siziwangqi area of Inner Mongolia, China. The druse calcite crystals formed in fault breccia in association with graphite, which has important implications for the evolution of the Bayan Obo rift. Seismic events and rift evolution should be recorded by the Bayan Obo Group given its Meso-neoproterozoic Age (ca. 1.6 Ga; e.g., Zhou et al., 2018, 2016; Fan et al., 2014, 2002). The main objectives of this study are to: (1) describe the occurrence of the calcite samples, determine the stable carbon and oxygen isotopic composition of graphite (carbon isotope) and calcite (carbon and oxygen isotope) minerals, and further explain the origin of the druse calcite crystals; (2) identify the different types of SSDSs to constrain the syn-sedimentary deformation; (3) combine the observed evidences to decipher the evolution of the Bayan Obo rift at ca. 1.6 Ga.
A Meso-neoproterozoic rift system developed in the NCC during ca. 1.8 Ga (e.g., Zhou et al., 2020, 2018; Zhai, 2011; Zhai and Liu, 2003). Three major rifts, including the Xiong'er, Yanliao and Bayan Obo, formed from south to north. The sedimentary strata in the Bayan Obo rift (i.e., the Bayan Obo Group) were controlled by E-W-trending normal faults that formed in the Early Mesoproterozoic (Wu et al., 2018; Zhou et al., 2018). The early stages of rift evolution resulted mainly in deposition of terrigenous clastic rocks (e.g., Shen et al., 2009; Lu et al., 2002). Subsequently, the NCC underwent rifting causing a marine transgression, which formed a carbonate platform in a shallow ocean. Tectonism became more intense and the sedimentary environment was dominated by semi-closed bay facies, and hydrothermal sedimentary sulfides were deposited in the eastern platform region (e.g., Inner Mongolia BGMR, 1991). The Bayan Obo Group includes the Dulahala Formation (Chd) and Jianshan Formation (Chj; Paleoproterozoic Changchengan Period); Halahuogete Formation (Jxh) and Bilute Formation (Jxb; Mesoproterozoic Jixian Period); and Baiyinbaolage Formation (Qnb; Neoproterozoic Qingbaikou Period). The Dulahala Formation comprises mainly metamorphosed quartz sandstones. The Jianshan Formation consists of littoral sediments that are light gray limestones and metamorphosed quartz sandstones, which contain SSDSs and thin calcite veins. The Halahuogete Formation comprises gray-white, thick-bedded limestones. The lower Bilute Formation consists of gray silty-muddy slates and thin metamorphosed sandstone beds. The Baiyinbaolage Formation comprises light gray metamorphosed quartz sandstones, and localized gray quartzites and silty slates. The main rock types in the Permian Dahongshan Formation are gray-green welded andesitic tuffs, gray-white welded rhyolitic tuffs, and breccias. The Upper Jurassic Daqingshan Formation (J3d) consists of gray polymict conglomerates (e.g., Zhou et al., 2016; Inner Mongolia BGMR, 1996). Frequent magmatism occurred in the Bayan Obo rift, and Hercynian silicic igneous rocks form part of the Meso-neoproterozoic Bayan Obo Group (e.g., Zhou et al., 2016; Liu et al., 2010; Zhang et al., 2009).
The study area covers the Tolgoi Mountain in northeastern Siziwangqi, located in the eastern Yinshan Block and central-southern Bayan Obo rift (Figure 1). The strata in this region include the Bayan Obo Group, Permian Dahongshan Formation, and Upper Jurassic Daqingshan Formation. The Hercynian was the most active stage of magmatism. The syn-sedimentary deformation developed in the Jianshan Formation. The regional structure was dominated by an E-W-trending anticlinorium in the Bayan Obo rift, which was disrupted by later stage NE-SW-trending thrust faults and NW-SE-trending normal faults (e.g., Li et al., 2018; Wu et al., 2018, 2016b; Zhou et al., 2018).
The calcite formed in brecciated limestone. The brecciated fragments retain their original sedimentary structures (Figure 2b), thus the breccia was formed by seismic events. The calcite occurs in gray-white, radial crystal clusters (Figures 2a–2b) and is euhedral, with the main crystal plane parallel to [4041], indicating that the calcite forms columnar crystals (Figure 2d).
Each calcite crystal is the same color (i.e., grayish yellow under the plane polarized light) and the mineral cleavage extends through the entire crystal (Figures 2c–2d). Pyrite (Figure 2e), quartz (Figure 2f), and graphite (Figures 2g–2h) are associated with the calcite. Quartz is sub-rounded and detrital in origin, pyrite is euhedral, and graphite is ellipsoidal in shape. Pyrite and graphite formed at the same time as the calcite, because the former is enclosed by the calcite crystals. The graphite comprises micron-sized granular carbon that is visible under the microscope (Figure 2h). The pyrite indicates a reducing environment, it is likely that the graphite formed from organic matter (e.g., Lin et al., 2014).
Stable carbon isotopes can be used to identify whether carbon has a biotic or abiotic origin; biogenic carbon has low δ13C values (e.g., Lin, 2016). We undertook stable carbon isotope analysis of the graphite. Samples were first crushed to powder, washed with 5% hydrochloric acid and water, and then graphite grains were handpicked under a binocular microscope at the China University of Geosciences, Beijing, China. The insoluble graphite was sent to the Analytical Testing Center of the Beijing Research Institute of Nuclear Geology, China, for stable carbon isotopic analysis. The graphite δ13C value is -20‰ (Table 1), indicating a biogenic origin (e.g., Cai et al., 2009). As such, the druse calcite crystals formed in an underwater environment, because there was biological activity during calcite formation (e.g., Li et al., 2003; Peng P et al., 1998).
| Sample | Mineral | δ13CV-PDB (‰) | δ18OV-PDB (‰) | δ18OV-SMOW (‰) | |||
| DJP01-HB1 | Calcite | -0.3 | -6.4 | 24.3 | |||
| DJP01-HB5 | Calcite | -0.1 | -5.6 | 25.2 | |||
| DJP01-HB7-1 | Calcite | -0.4 | -7.1 | 23.6 | |||
| DJP01-HB7-2 | Calcite | -0.1 | -5.3 | 25.4 | |||
| DJP01-HB8 | Calcite | -1.3 | -11.9 | 18.6 | |||
| DYS | Graphite | -20 | 0 | 0 |
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We analyzed the druse calcite crystals for stable carbon and oxygen isotopes. Firstly, the rock samples were sent to the Langfang Regional Geological Survey Institute, Langfang, China, for calcite separation. The stable carbon and oxygen isotopic analyses were undertaken at the Analytical Testing Center of the Beijing Research Institute of Nuclear Geology. Isotope ratios were determined with a MAT-253 mass spectrometer. The resultant isotopic values are normalized to NBS-19 in conventional delta notation (δ18Oc and δ13Cc) and are reported relative to VPDB with uncertainties better than 0.08‰ and 0.06‰, respectively. Five samples were decomposed with the phosphoric acid method, by placing the sample into 100% phosphoric acid in a vacuum at a constant temperature at 25 ℃ for > 4 h. The pure CO2 that was released was analyzed for δ13C and δ18O values (e.g., Phosphoric Acid Method to Determination of Carbon and Oxygen Isotopic Composition in Carbonate Minerals or Rocks), the accuracy is ±0.2‰. The stable isotope data for calcite are listed in Table 1.
Carbon derived from organic sources is reduced carbon and has low δ13C values, whereas carbon derived from inorganic sources is oxidized carbon and has high δ13C values (e.g., Cai et al., 2009). δ13C values of inorganic carbon range from -4.0‰ to +4.0‰, which reflects supersaturated precipitation of CaCO3 in an alkaline ocean (e.g., Wang et al., 2007). The δ13C values of the studied calcite minerals range from -0.1‰ to -1.3‰ (average = -0.61‰), indicating an inorganic carbon source. δ18O values of calcite minerals are related to the temperature of the ocean (or fluid) during calcite formation, and δ18O values decrease with increasing temperature when the salinity is constant. Therefore, Shackleton et al. (1975) proposed an equation for calculating paleo-temperatures based on previous studies:
|
t=16.9–4.38(δC–δW)+0.1(δC–δW), |
where t is the paleo-temperature, δC is the calcite δ18O value (relative to the PDB standard), δW is the ocean δ18O value (relative to the SMOW standard). A δW value of 0 was used in the present study. Based on this equation and our calcite δ18O data, the paleo-temperature was 83–43 ℃ (average = 55 ℃), which is in the temperature range for the formation of columnar calcite crystals (75–25 ℃; e.g., Li, 1994). So the occurrence and formation of calcite indicate that the druse calcite crystal grew in a single event and was unmodified by later tectonic and metamorphic effects. The calcite crystallized in a closed alkaline groundwater sedimentary environment (e.g., Wang et al., 1998). Pure columnar calcite crystals form in paleo-caves formed by fault brecciation when the groundwater is over-saturated with CaCO3.
In this study, syn-sedimentary deformation in the Jianshan Formation was divided into two types: collapse and SSDS. The SSDSs can be triggered by a variety of mechanisms (i.e., earthquakes) and controlled by a range of deformation mechanisms (i.e., liquefaction, thixotropic, hydroplastic, gravity-driven, and brittle deformation). Liquefaction can be induced by earthquakes (Ms ≥ 5), which can form liquefied sand, micrite veins, breccias, sand volcanoes, mixed-layer structures, and escaped water structures (e.g., Tian and Zhang, 2016; He, 2010; van Loon, 2009; Montenat et al., 2007; Rodríguez-Pascua et al., 2000; Rossetti and Goes, 2000; Takahama et al., 2000; Owen, 1995; Guiraud and Plaziat, 1993; Plaziat and Poisson, 1992; Plaziat et al., 1990; Liu and Xie, 1984; Reineck and Singh, 1980; Sims, 1975). Thixotropic deformation occurs in water-saturated, soft sediments with a grain size of < 0.005 mm due to seismic shear stress (Ms ≥ 7), when the sediment strength is decreased and the viscosity and strength are partially restored (e.g., Tian and Zhang, 2016; Li et al., 2010; Feng et al., 2004; Moretti et al., 1999; Rossetti, 1999; Obermeier, 1996; Owen, 1996; Zhang, 1989; Allen, 1982; Lowe and Lopiccolo, 1974). Hydroplastic deformation also occurs in water-saturated soft sediments; the seismic shear stress causes the pore fluid pressure to increase and the supporting strength between the sediment grains to weaken, thereby allowing continuous deformation to occur. An instantaneous frequent stress transfer and low-angle slope is necessary for hydroplastic deformation. Structure types include slumping, intense folding, plate-spine brecciation, convoluted bedding, and boudinage-like structures (e.g., He and Qiao, 2015; Qiao and Li, 2009, 2008; Rodríguez-Pascua et al., 2000; Calvo et al., 1998; Owen, 1996; Song, 1988; Lowe, 1975; Williams, 1960). When the sediment water-saturation is low and the degree of consolidation is high, cracks or even local breccias form (e.g., Guiraud and Plaziat, 1993). Load, flame-like, pseudo-nodule, and ball-pillow structures can form due to earthquakes (e.g., Shanmugam and Wang, 2015; Shao et al., 2014; McLaughlin and Brett, 2004; Owen, 2003; Obermeier, 1996; Allen, 1982; Visher and Cunningham, 1981; Anketell et al., 1970; Kuenen, 1958). Brittle deformation results in fault and joint formation in (semi-)consolidated rocks in upper sedimentary layers, including stepped normal faults, fissures, Neptunian dikes, in-situ pillows, and shatter breccias (e.g., Qiao et al., 2012; Moretti and Sabato, 2007; Zhou et al., 2006; van Loon, 2002; Obermeier, 1996; Roep and Everts, 1992; Montenat et al., 1991; Reineck and Singh, 1980).
A sketch of the collapse feature in this study is shown in Figure 3, which include locations at 41°44′16′′N–111°21′51′′E and an altitude of 1 484.4 m (Figure 1). The collapse feature is developed at the top of the sedimentary sequence, including the collapse breccias and sliding layers (Figure 3), and has a width of ~800 m, length of ~6 km, thickness of ~5 m, and strikes NE-SW.
During sliding, the sediments liquefied and formed composite folds, which had little effect on the underlying consolidated sediment layers. Collapse structures are typically divided into four regions, including the root tension area (where the druse calcite crystals formed), isoclinal fold shear zone, front edge thrust-controlled fold, and thickened and shortened area (with thrust faulting and folding; e.g., Alsop and Marco, 2012).
The northern part of the collapse feature is dominated by breccia and druse calcite crystals. The southern part is dominated by hydroplastic folds and stepped normal faults (Figure 3). Hydroplastic folds developed irregularly in gently sloping areas due to instantaneous forces caused by seismic events. Paleocurrent analysis is an important part of sedimentary basin research. The Jianshan Formation contains small cross-bedding. The silty-fine-grained sandstones were affected by paleo-flows, accumulated on a slope, and contain small cross-beds, which can be used to determine the paleocurrent direction. The occurrence of the cross-bedding in the Jianshan Formation directs to East (Figures 4a–4b). We collected paleocurrent data for 32 sets of cross-bedding (Table S1). Firstly, the original data of cross-bedding were tilt-corrected, returned to horizontal position. Secondly, Stereonet 8 Rosette software (Allmendinger et al., 2012) was used to produce a rose diagram (Figure 4c). This showed that the paleocurrent direction in the Jianshan Formation was 45°, which is different from the sliding direction of the collapse feature.
Different types of SSDSs were analyzed in two outcrops (PM04 and PM08). PM04 is located in the lower part of the aforementioned collapse and contains stepped normal faults. PM08 is located 5 km NE of PM04, and contains convoluted bedding and shatter breccias in fine-medium-grained sandstone and limestone. The SSDSs were analyzed and are described below (Figure 5).
Outcrop PM04 was affected by brittle deformation and liquefaction (Figures 5a–5d), and developed stepped normal faults (Figure 5a), fissures (Figure 5b), hydroplastic folds (Figure 5c), and liquefaction breccias (Figure 5d). The stepped normal faults record the sliding direction of the SSDSs (Figure 5a). The fissures are nearly vertical, tensile fractures in consolidated rocks, indicating the seismic magnitude was > 6 (Figure 5b) (e.g., Scott and Price, 1988), and overlying limestone-mudstone filled the fissures. Hydroplastic folds occur as irregular supine that developed during the sliding deformation of thin argillaceous layers (Figure 5c).
Outcrop PM08 is divided into layers 1–9 (SSDSs) and layers 10–14 (collapse feature); the thickness of the collapse feature is ~200 m. The collapse breccia is the product of a small displacement, has a lithology that is the same as the surrounding rocks, and contains clasts that are 10–50 cm in size. Due to a seismic event, the collapse breccia was affected by brittle deformation, forming a shatter breccia with a clast size of 5–10 cm and fissures infilled with overlying sediments (Figures 5h–5k). Similar shatter breccias were also found in the Wumishan Formation, which is in the lower part of the Zhuanghuwa River Section in the Yanliao rift (e.g., Qiao and Gao, 2007). In this case, the breccia clasts are dolomite. The collapse breccia fell into weaker and fine-grained sediments to form a variety of load structures (Figures 5f–5k'). The lower part of the PM08 outcrop was affected by liquefaction deformation (Figures 5f'–5e'–5i) and hydroplastic deformation (Figures 5e–5g). The convoluted bedding resulted from the seismically triggered liquefaction of fine-grained-silty sediments (e.g., Reineck and Singh, 1980; Williams, 1960). The shear stress exerted by the fluid due to gravity formed continuous wide synclines and tight anticlines (e.g., Xiao, 2009). The top of the convoluted bedding is truncated by the overlying sediment layer (Figures 5e–5i), indicating that deformation occurred before sedimentation of the overlying layer. The convoluted bedding was caused by hydroplastic deformation (e.g., Rossetti, 1999). Liquefaction and hydroplastic deformation are the two most common deformation mechanisms during earthquakes. For example, the Wumishan Formation in the Yanliao rift contains convoluted bedding.
Liquefaction deformation can be observed near outcrop PM08, including veins and diapirs. During seismic shaking, pore waters escape to lower pressure zones, forming liquefaction veins (e.g., Qiao and Li, 2009; van Loon, 2009; Obermeier, 1996; Nichols et al., 1994; Qiao et al., 1994; Plaziat and Poission, 1992; Figure 6a). The liquefied sandstone carried dolomite trap with long axis of ~8 cm to move and formed liquefied breccia (Figure 6b). The liquefied sediments (sandstone and limestone) flowed beneath the surface along tubular channels and were erupted at the surface, forming sand volcanoes (e.g., Qiao and Li, 2009; Figure 6c). The diapirs deformed the overlying sediments (e.g., Owen, 1996; Figure 6d); some of the diapirs did not penetrate the overlying sediments (Figure 6e), whereas others penetrated the overlying sediments forming sandstone layers on the surface (Figure 6f). The Yanliao rift contains similar liquefied vein (diapir) structures in the Changcheng System rocks in the Zhuanghuwa River Section.
The druse calcite crystals are associated with graphite, quartz, and pyrite, and the calcite crystals have a columnar form. The calcites formed from a fluid at temperatures of ~55 ℃, similar to a hot spring environment. It is possible that the calcite formed in alkali-rich, hot spring waters in a paleo-cave containing collapse breccias. The calcite, pyrite, and anaerobic micro-organisms co-existed in an underwater reducing environment, which formed columnar calcite crystals and graphite (from the micro-organisms).
Extensional faults formed during the development of the Bayan Obo rift were infiltrated by seawater. The seawater was then heated and hot spring waters ascended and were discharged back into the basin along the faults. This provided the heat source and fluid for calcite precipitation.
During the Meso-neoproterozoic, the NCC underwent extension and the major faults produced earthquakes (Ms > 5) (e.g., Scott and Price, 1988). Seismic shaking led to sediment fluidization due to the associated increase in pore fluid pressure, non-permeable layers, and well-sorted sediments (e.g., Lowe, 1975).
In the Bayan Obo rift, the SSDSs are seismogenic given that: (1) the study area was located in an active earthquake zone (Ms > 5) (e.g., Scott and Price, 1988); (2) the deformation layers are laterally continuous and occur repeatedly in the stratigraphy; (3) the deformation layers are thin; (4) the properties of the SSDSs are similar to those documented in previous studies; (5) the sediment grain size is in the range of that necessary for liquefaction; (6) the SSDSs meet the criteria for seismites (e.g., Rossetti, 1999; Sims, 1975). The Jianshan Formation limestone was deposited in hydrostatic environment. In outcrop PM08, the SSDSs developed on a gentle slope, and deformation was limited to a specific horizon, implying a single and instantaneous triggering event. In addition, the convoluted bedding can be inferred to record syn-sedimentary deformation associated with seismic shaking (e.g., Cojan and Thiry, 1992). As such, the syn-sedimentary deformation was earthquake-triggered.
The sliding direction of the collapse feature differs from the paleocurrent direction in the Jianshan Formation, and outcrop PM08 is located NE of outcrop PM04, which implies that syn-sedimentary deformation developed in a NE-SW-trending depression (Figure 7). During earthquakes, collapse breccias (i.e., fault breccias) formed along the fault scarp. The height of the fault scrap was ~200 m, based on the thickness of the collapse breccia in outcrop PM08, and subsequently the fault provided the heated fluids for druse calcite crystal formation. As such, the druse calcite crystals are important evidence of seismic events.
The documented SSDSs were produced by seismic shaking related to the extensional tectonic setting of the Bayan Obo rift. The Jianshan Formation experienced NW-SE-oriented tensile stress, which produced NW-SE-trending normal faults and collapse breccias in fault depressions. The Yanliao rift had a similar tectonic setting and stress field to the Bayan Obo rift (e.g., Qiao and Gao, 2007), as both formed in response to break-up of the Columbia supercontinent at ca. 1.6 Ga.
The break-up event of the Columbia supercontinent is evident from metamafic dike swarms (i.e., Zhang et al., 2017). A mantle plume resulted in intraplate rifting, and the tholeiitic dike swarms were intruded from 1.78–1.73 Ga (e.g., Peng, 2015, 2010; Peng et al., 2006; Zhao et al., 2001). Previous studies suggested that the Bayan Obo rift formed at a passive continental margin (e.g., Zhang et al., 2012; Zhang and Liu, 2010). The seismic evidence and collapse breccias documented in the present study indicate the rapid development of the Bayan Obo rift and break-up of the Columbia supercontinent at ca. 1.6 Ga (e.g., Zhou et al., 2018, 2016), when the lithosphere began to thin and formed a passive continental margin along the northern NCC. The druse calcite crystals preserved the key deformation structures in the Bayan Obo rift at ca. 1.6 Ga.
(1) The druse calcite crystals formed in paleo-caves containing fault breccias, and the mineralogy and stable isotopic systematics of the calcite indicate its formation in a hot spring environment. The fault activities provided the space (i.e., fault breccia) and heat (i.e., fluid) for calcite formation.
(2) The SSDSs in the study area were earthquake-triggered in a NW-SE extensional stress field. The NE-SW-trending faults formed depressions and paleo-caves, which subsequently formed collapse breccias in which the druse calcite crystals formed.
(3) Seismites and syn-sedimentary faulting indicate that the Bayan Obo and Yanliao rifts had the same stress field and developed similar deformation structures. Therefore, the Columbia supercontinent experienced rapid NW-SE extension at ca. 1.6 Ga.
ACKNOWLEDGMENTS: This research was financially supported by the National Natural Science Foundation of China (Nos. 41772227, 41872232). This work was supported by the Inner Mongolia Mapping Programs (Nos. 1212010811001, 1212011120700, DD20160045, 1212010510506) awarded to Zhiguang Zhou and administered by the Institute of Geological Survey, China University of Geosciences (Beijing). We thank Chief Editor, Associate Editor, and three anonymous reviewers for their constructive comments that have led to a significant improvement of the original draft of this paper. The final publication is available at Springer via https://doi.org/10.1007/s12583-021-1416-0.|
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| 1. | Jian-Fang Guo, Qiang Ma, Jian-Ping Zheng, et al. Spatial and Temporal Evolution of Lithospheric Mantle beneath the Eastern North China Craton: Constraints from Mineral Chemistry of Peridotite Xenoliths from the Miocene Qingyuan Basalts and a Regional Synthesis. Journal of Earth Science, 2025, 36(2): 474. doi:10.1007/s12583-022-1691-4 |
Figures(7) / Tables(1)
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Yueshuang Du, Zhiguang Zhou, Guosheng Wang, Chen Wu, Wenchao Xu. Druse Calcite Crystals Formed by Mesoproterozoic Paleo-Earthquake Activity in the Northern Margin of the North China Craton. Journal of Earth Science, 2024, 35(2): 514-524. doi: 10.1007/s12583-021-1416-0
| Sample | Mineral | δ13CV-PDB (‰) | δ18OV-PDB (‰) | δ18OV-SMOW (‰) | |||
| DJP01-HB1 | Calcite | -0.3 | -6.4 | 24.3 | |||
| DJP01-HB5 | Calcite | -0.1 | -5.6 | 25.2 | |||
| DJP01-HB7-1 | Calcite | -0.4 | -7.1 | 23.6 | |||
| DJP01-HB7-2 | Calcite | -0.1 | -5.3 | 25.4 | |||
| DJP01-HB8 | Calcite | -1.3 | -11.9 | 18.6 | |||
| DYS | Graphite | -20 | 0 | 0 |
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