The Impact of Lamina Characteristics and Types on Organic Matter Enrichment of Chang 73 Submember in Ordos Basin, NW China

The Chang 7 member in Ordos Basin is an important shale oil exploration layer, with new shale-oil discoveries in recent years. The Chang 73 submember is rich in organic shale, which is the main source rock of shale oil in the Yanchang Formation. In order to clarify the lamina structure, composition, types, and distribution characteristics in Chang 73 submember and its influence on organic matter enrichment, a full coring well in Chang 73 submember located in deep-lacustrine facies is selected to obtain intensive systematic core samples. Core observation, thin section identification, X-ray fluorescence element analysis, X-diffraction analysis, scanning electron microscope, electron probe, rock pyrolysis, and other techniques are performed to systematically analyze the morphology, structure, thickness, mineral compositions, and organic matter content of the shale lamina in the Chang 73 submember. Five types of lamina are identified: silty felsic lamina (SF), tuffaceous lamina (TF), organic-rich clay lamina (ORC), organic-bearing clay lamina (OBC), and homogeneous clay lamina (HC), which are further subdivided into eight subtypes. The lamina types change greatly vertically in the Chang 73 submember, in which the lower part is mainly silty felsic lamina, organic-rich clay, and tuffaceous lamina, the middle part is mainly organic rich and organic clay lamina and organic-bearing clay lamina, and the upper part is mainly homogeneous clay lamina and a small amount of silty felsic organic-bearing clay lamina and organic-bearing clay lamina. Different laminae show various organic matter types, organic matter content (TOC), and organic matter occurrence states which can be divided into four occurrence types. The TOC in organic-rich clay lamina and part of homogeneous clay lamina is high, while that of silty felsic lamina is lower. The relationship between shale lamina and organic matter enrichment is established according to the correlation analysis of laminar characteristics, mineral content, and organic matter content. Among them, the organic-rich lamina is richest of TOC and is a favorable “sweet point” for shale oil exploration.

The classification of laminae is usually based on the organic matter as well as the composition and content of minerals. For example, Shi et al. [8] found that the Silurian Longmaxi Formation in Sichuan Basin developed four types of laminae, containing organic-rich, organic-bearing, clay, and silty; Xi et al. [9] thought that the shale of Chang 7 3 submember of Yanchang Formation in Ordos Basin includes four types of lamina: tuffaceous, organic, silty, and clay rich. As the most important and widely developed sedimentary feature in shale rock, lamina structure not only controls the reservoir physical properties of shale [16][17][18][19][20][21] but also leads to strong heterogeneity of shale reservoir, thus affecting the quality of shale reservoir. In particular, the lamina characteristics and types of continental shale are more complex than those of marine shale. Therefore, the study of laminar types and structures has become an indispensable content in the study of sedimentology in unconventional oil and gas, which has attracted the attention of geologists and explorers recently [22][23][24]. For example, Hua et al. [16] believe that the reservoir properties of coarse laminar shale of Longmaxi Formation in Sichuan Basin are better than thin laminar shale, and thin laminar shale is better than massive mudstone.
The types and characteristics of laminae are closely related to the lithology and lithofacies of shale. Exploration and research show that the lithology types of shale mainly include clay rich, siltstone and carbonate, or their combination [25][26][27]. Compared with lithology, the lithofacies types of shale are more complex [28]. In early studies, the lithofacies types of shale are usually divided according to mineral composition and organic matter content (TOC). The mineral composition usually includes felsic, clay, and carbonate, and TOC can be high or lower. For example, Wang and Carr divided the Marcellus Shale into seven types including organic siliceous shale, organic mixed shale, and gray mudstone [29]. Later, the sedimentary structure was considered in the lithofacies classification, which can generally be divided into laminated, beded, and massive. For example, Song et al. carefully made the lithofacies classification of Shahejie Formation shale in the Raoyang Sag according to the difference of rock type, sedimentary structure, and TOC [30]. Liu et al. divided the Qingshankou shale in the northern Songliao Basin into 7 lithofacies types according to the TOC, fabric, and mineral composition [31].
It is found that the shale of the Chang 7 3 submember in Ordos Basin has complex lithology, containing felsic, clay, sandstone, and siltstone, as well as the tuffaceous and carbonate, which results in diversified lamina structure and types, complex combination modes, and great differences in the distribution of mineral composition and organic matter in lamina [9,22,32]. The type, structure, and mineral composition of different laminae often control the type, enrichment, and occurrence characteristics of organic matter, thus affecting the hydrocarbon generation potential of organic matter and the quality of source rock [33]. In addition, the lamina influences the pore type and pore space distribution of shale, which in turn have an important impact on the content and occurrence of retained hydrocarbons [7,34,35].
Research also found that the organic-rich lamina shale in Chang 7 3 member of Ordos Basin is poor in porosity, but the situation in felsic rich shale is opposite, and the pore relatively developed [36,37]. In addition, the TOC and porosity in tuffaceous and carbonate rich lamina are of great difference, which makes it more difficult to study formation mechanism of lamina, as well as the favorable area evaluation of shale oil exploration. Therefore, the fine research on the type, structure, and influence on organic matter enrichment of shale lamina in Chang 7 3 member is of great significance; however, the previous research in these aspects is relatively weak. Taking a fully cored well in Chang 7 3 member shale in the deep lacustrine faces as the research object, by systematic and intensive sampling, using thin section, X-ray diffraction analysis, scanning electron microscope, electron probe, and other analysis methods, combined with the principle of fine-grained sedimentology analysis, this paper describes the lamina types, structure, and mineral composition. Furthermore, the effects of laminar types on the occurrence forms and enrichment characteristics of organic matter are discussed in order to provide a reference for the enrichment characteristics and evaluation of shale oil in Chang 7 3 submember, Ordos Basin.

Geologic Background
Ordos Basin is a large superimposed basin in Central China, which is composed of six structural units, containing Western thrust belt, Tianhuan depression, Weibei uplift, Yimeng uplift, Yishan slope, and Jinxi fault-fold belt [38] ( Figure 1(c)). During the sedimentary period of Yanchang Formation in the Late Triassic, the basin developed a large inland depression lake, deposited a set of clastic rock including lake and fluvial facies, which can be divided into 10 members from top to bottom (Figures 1(a)). The Chang 7 member in Yanchang Formation developed a greatest lake, and only the area of deep lacustrine faces can reach 6:5 × 10 4 km 2 , with abundant aquatic organisms and plankton, enrichment of organic matter, and black mudstone and shale [39]. The average thickness of Chang 7 member is about 80-100 m, of which Chang 7 3 submember is a section with concentrated distribution of organic-rich shale, with a cumulative thickness of 30-50 m (Figure 1(b)), rich in raspberry pyrite and Collophanite [40][41][42].
Ordos Basin is an important shale oil exploration field in China. The discovery of Qingcheng shale oil field in 2019 with 1 billion ton geological reserves has achieved a historic breakthrough in shale oil exploration progress in Chang 7 member. Moreover, Cy 1 and Cy 2 wells have obtained more than 100-ton oil flow per day in Chang 7 3 submember, with thick organic-rich shale and thin siltstone. In 2020, the shale oil output of Changqing Oilfield reached 143 × 10 4 t, realizing the scale benefit development of shale oil in Ordos Basin [39].
The core samples in this study are from the well that located in Wuqi area in the middle of Ordos Basin. The Chang 7 3 submember is a deep lacustrine faces deposit with a thickness of 46 m. The lithology is mainly shale mixed with siltstone and tuff. It can be divided into three positive cycles from top to bottom, by which Chang 7 3 submember is divided into three sublayers. A total of 152 samples are taken in the whole Chang 7 3 cores, with an average of 3 samples per meter (Figure 2), which makes a good foundation for the fine description of shale lamina types and structural characteristics.        is determined by X-ray diffraction, scanning electron microscopy, and electron microprobe. Organic matter type and TOC value was obtained by CS-I carbon sulfur analyzer. Optical microscope is the German Zeiss polarizing microscope, the eyepiece is 10 times, the objective lens is 5-20 times, single polarized light, and orthogonal transmission light. X-ray diffraction is done by d8advance X-ray dif-

Lamina Structure.
As for the lamina structure, different scholars have put forward different classification schemes according to the lamina thickness and shape [8,44,45]. Ingram called the lamina with thickness less than 3 mm as extremely thin lamina, the lamina with thickness of   [42]. In the process of shale classification of Chang 7 3 member, predecessors mainly considered the lamina thickness and mineral composition and paid less attention to the lamina morphology. In this paper, based on the development form, thickness, and mineral composition of lamina, the lamina is divided into plate-like, wavy, and block types. Thereafter, according to the change of lamina thickness, the lamina with thickness less than 0.5 mm is called extremely thin lamina; the lamina with thickness of 0.5 mm~1 mm is thin lamina; the lamina with thickness of 1 mm~5 mm is medium lamina; the lamina with thickness of 5 mm~10 mm is thick lamina; this thicker than 10 mm is called bed. The shale lamina in Chang 7 3 member of G well is mainly made up of extremely thin-thin plate-like laminae (Figures 3(a)-3(d)), and wavy as well as massive laminae is locally developed (Figures 3(e) and 3(f)). The plate-like laminae occur in continuous horizontal layers (Figures 3(a)-3(d)), in which the bright lamina and the dark one appear alternately. The bright lamina mostly contains quartz and feldspar, and the quartz particles are relatively bigger than other. The content of illite, mica, and other clay minerals as well as organic matter is higher in the dark lamina. The thickness of single lamina is mainly 0.05~1.0 mm (Figure 3(b)). The wavy laminae present near parallel wavy shape, and the bright lamina and dark one appear alternately too. Compared with the plate-like lamina, the clastic particles of the wavy lamina are finer, the single lamina is thinner, and the thickness is mainly distributed in 0.01~0.5 mm. The mineral composition in the bright and dark layer is similar to that in the plate-like lamina (Figure 3(e)). The massive lamina is dark brown to gray, with good homogeneity (Figure 3(f)), which is mainly composed of clay minerals and small amount of very fine silt. The clastic particles such as quartz and feldspar are rounded often, and clay minerals are mainly illite, with a maximum content of 80%, followed by quartz and feldspar, as well as a small amount of pyrite and muscovite, and the content of organic matter changes greatly.

Laminar Mineral Composition.
The shale minerals in Chang7 3 member of Ordos Basin are mainly clay minerals, feldspar, quartz, calcite, and dolomite [43]. The X-ray diffraction test results of 152 samples from G well show that the mineral composition of Chang 7 3 shale is mainly clay and felsic (Table 1), and the clay mineral is mainly illite, containing a small amount of montmorillonite and kaolinite (Figures 4 and 5). The clastic minerals are mainly feldspar  In the clastic minerals of Chang 7 3 shale, the content of quartz is about 15-40%, with an average of 20.1%. The surface of quartz particles is relatively smooth and produced in granular, lenticular, or strip shape ( Figure 5(c)). Plagioclase content is about 5-32%, with an average of about 14.5%. Albite is produced in thin plate, granular and angular shape. Dissolution holes are developed in the particles and filled with organic matter. More special, siliceous spots and veins are relatively developed (Figures 5(d)), which commonly show fluorescence ( Figure 6). In order to understand its genesis, the siliceous area was analyzed in detail by electron microprobe ( Table 2). The data shows that the content of SiO 2 is basically more than 50%, and the content of aluminum, potassium, and sodium minerals is also high, indicat-ing a good associated relationship with feldspar. It is considered that the spotted and vein quartz comes from the dissolution and precipitation of SiO 2 from feldspar. The formula is as follows [46]: Oval authigenic quartz is symbiotic with rectangular irregular feldspar and clay, indicating that there is a genetic relationship between them, and there is no obvious crystal form of quartz (Figure 6(c)). This phenomenon is mainly found in the shale of middle and lower part of Chang 7 3 member.
Pyrite is mainly sulfide of Chang 7 3 member shale, with a diameter of 1.1-25 μm, self-shaped crystal of quadrilateral, hexagonal, or colloidal. The aggregates of pyrite are like strawberry, radial, lenticular, and other forms (Figures 5(e) and 5(f)). Pyrites in different aggregates have complex contact relationships and multistage growth characteristics. Collophanite is common in Chang 7 3 member shale, with a diameter of 10 μm-2.5 mm, in shape of plate, crescent, or ring. The aggregate of collophanite shows banded, lenticular, or irregular ( Figure 5(g)). Collophanite is partially transformed into apatite and calcite during diagenesis.
The content of carbonate in Chang 7 3 member is relatively small, which is mainly composed of calcite, ankerite. Calcite often developed dissolution holes and later filled with (1) Silty Felsic Lamina (SF). The grain in the lamina is mainly feldspar and quartz, with a content of up to 60-70%, but the content of organic matter is low, only 1-5%. This lamina shows light color, developing silt grade positive grain sequence, and particle size decreases upward as well as clay content increases, with the main particle size of 10-50 μm. The minerals are sorted medium to good, and the thickness of a single lamina is about 0.4 mm-10 mm (Figure 7(a)).
(2) Tuffaceous Lamina (TF). The lamina is mainly light gray volcanic tuff material, occurring nearly horizontal, including angular volcanic glass and crystal chips, interbedded with intermittent organic matter bands. Authigenic pyrite is widely developed where tuffaceous matter often contacts banded or dispersed organic matter. The content of organic matter is about 3-5%, and the thickness of a single lamina is about 0.2-1 mm.
(3) Organic-Rich Clay Lamina (ORC). The lamina can be further subdivided into two subtypes. ① Organic-rich plate-like clay lamina: this lamina has a dark color and presents a horizontal mud grade structure, in which a small amount of bright color striated lamina occurs, showing high content of felsic. The thickness of a single lamina is about 0.1-1 mm. A great amount of dispersed organic matter fragments, algal fossils, and collophanite can be seen, and the content of organic matter is about 8-12% (Figures 7(c) and 7(d)). ② Organic-rich wavy clay  (4) Organic-Bearing Clay Lamina (OBC). This lamina has a similar structure and mineral composition to organic-rich clay lamina. It is also further subdivided into two subtypes according to the lamina shapes: ① organic-bearing plate-like clay lamina, which is brownish yellow and a low content of organic matter about 3-6% and ② organic-bearing wavy clay lamina. Clay minerals and organic matter form wavy lamina in lenticular or gentle wavy shape. The thickness of a single lamina is about 0.05-0.5 mm. The organic matter content is about 4-5% (Figures 7(f) and 7(g)).
(5) Homogeneous Clay Bed (HC). This lamina is further subdivided into two subclasses according to the content of organic matter. ① Homogeneous organicrich clay bed: this lamina is black or gray black as to plenty of clay minerals and organic matter, showing a mud clastic structure, and light colored felsic particles dot it. The thickness of the single layer is greater than 10 mm, and the content of clay and organic matter is about 50-80% and 6-10%, respectively (Figure 7(h)). ② Homogeneous organicbearing clay bed. The lamina has lighter color compared with the former, because of lower content of organic matter, only 2-6% (Figure 7(i)).

Longitudinal Distribution of Lamina.
Through the statistical analysis of the core samples, extremely thin and thin plate-like lamina are mainly types in Chang 7 3 submember of well G, and wavy lamina or massive bed develop locally. Moreover, the organic-rich clay lamina most developed, mainly in the middle and lower part of Chang 7 3 member (Figure 8), and the TOC is basically more than 8%. The organic-bearing clay lamina is distributed almost whole Chang 7 3 member, which is complementary to the distribution of organic-rich lamina and homogeneous clay bed, and homogeneous clay bed developed mainly in the up part of Chang 7 3 member. The silty lamina mainly distributes at the top and bottom part where the siltstone deposits, and the tuffaceous lamina occurs mainly at the lower and the middle part. The proportion of these two laminas is relatively low, less than 20%. What conditions may affect this combination? What is the impact on organic matter enrichment? Several combinations of laminar types often occur in the same depth section from Figure 8, which is related to the complex sedimentary environment [8] and the influence of external material events during the deposition of Chang 7 3 member in Ordos Basin. In the middle and lower part of Chang 7 3 member, the shale of semideep to deep lacustrine facies [47] is mainly deposited, which usually develops ORC and OBS lamina combination. However, at the same time, volcanic events [32] and gravity flow [48] occurs often, and the SF and TF laminae are developed. In the upper part, the shale and mudstone mainly deposit under the semideep lacustrine environment. Meantime, affected by gravity flow and terrigenous input, a small amount of SF and OBC lamina combination developed.

Characteristics and Types of Organic Matter in Lamina.
The type of organic matter has a great influence on its hydrocarbon generation capacity and the types of generation products [49,50]. The results of slices analysis show that the shale of Chang 7 3 submember is mainly sapropelic and   posed of hydrogen-rich and hydrogen-poor secondary components, only accounting for 0.1% of whole rock and 1.7% of the relative macerals. Shale in Chang 7 3 submember contains high sapropelic and vitrinite group and has high hydrogen index (between 300-700 mg/g.TOC). It can be clear from the cross plot of hydrogen index (IH) and Tmax that kerogen types are mainly type I and type II 1 , with great hydrocarbon generation potential and oil generation (Figure 9).

Distribution Characteristics of Organic Matter in
Lamina. Through the observation of microscope and scanning electron microscope, the organic matter in Chang 7 3 member shows four occurrence forms: ① dense  13 Geofluids disseminated: the organic matter is densely disseminated and evenly distributed (Figures 10(a) and 10(b)), and the average TOC is about 10%. This type is mainly distributed in plate-like clay lamina and homogeneous clay bed, with low content of felsic, and the thickness of single lamina is usually large; ② sparsely dispersed: organic matter is dispersed in shale (Figures 10(c) and 10(d)), and the TOC is low, mostly less than 8%. This type mainly distributed in silty felsic lamina and clay layer. The content of felsic or clay is high, and the lamina is thin, usually 0.1-0.05 mm; ③ vein and lenticular like; organic matter is densely distributed in vein and lenticular shape (Figure 10(e)), which is often symbiotic with pyrite and collophanite. The TOC is usually high, mostly more than 8%. This type is mainly distributed in organic-rich clay lamina. According to the statistical data, the thinner the lamina, the higher the content of organic matter is. ④ Lamina-like; organic matter is distributed in relatively continuous lamina (Figure 10(f)), but the density of organic matter lamina is low, so the TOC is also low (3-8%), which is mainly distributed in thin parallel plate lamina.  (Figures 8 and 9). The organic matter in organic-rich clay lamina, tuffaceous lamina, and homogeneous clay layer is mainly type I; however, the organic matter types of silty felsic lamina and organicbearing clay lamina are mainly type II 1 . Qiu et al. also put forward that the organic-rich shale of Lucaogou Formation in the Jimusar Sag contained mainly type I-II 1 kerogen, while the silty shale often deposited type II 1 -II 2 kerogen [26]. This is related to the fact that different laminae represent different sedimentary environments and different hydrodynamic conditions. The deposit hydrodynamics of silty felsic lamina is relatively strong, the oxygen content of water body is high, and the organic matter is mainly from land input. The deposit hydrodynamic conditions of organic-rich clay lamina are between silty felsic lamina and homogeneous clay layer. Under relatively weak hydrodynamic conditions, aquatic algae dominated by plankton are easy to deposit, and the organic matter is dominated by lipid compounds (Figures 3(c) and 10(a)). Therefore, this kind of lamina has good organic matter type and high TOC. This is consistent with the understanding of the formation environment of lamina types of Longmaxi formation in Sichuan Basin discussed by Shi et al. [8].

Discussion
However, there are two different kerogen types in the homogeneous clay layer, and the content of organic matter is quite different. Among them, the hydrodynamic conditions of the homogeneous clay layer rich in organic matter are the weakest, and the oxygen content at the bottom of 14 Geofluids the water is lower, which is conducive to the preservation of organic matter. Therefore, the content of organic matter is mostly more than 6%, and the organic matter is densely disseminated. The content of felsic in the homogeneous clay layer containing organic matter is high, indicating that there are certain hydrodynamic conditions and relatively poor preservation conditions. The main organic matter is type II 1 , and the abundance of organic matter is also low. The tuffaceous lamina itself does not contain organic matter, but volcanic ash can bring a lot of nutrients. Algae and collophanite are developed on both sides of the tuffaceous lamina (Figure 7(b)). Therefore, although the content of organic matter in tuffaceous lamina is relatively low, it can promote the growth of organic matter in other lamina. Zhang et al. [33] and Liu et al. [51] also proposed that volcanic eruptions form a large amount of nutrients, which has a "fertilization" effect on aquatic organisms in the lake.

Effect of Lamina Mineral on Organic Matter Enrichment.
Through the statistical analysis of the relationship between mineral composition and organic matter enrichment of different types of laminae, the TOC of shale in Chang7 3 member is generally negatively correlated with quartz and feldspar and positively correlated with pyrite, but no obvious relationship with clay minerals (Figure 11). Previous studies [52] have shown that the higher the content of felsic, the increase of terrigenous substances, good water fluidity, and high oxygen content. It is not easy to preserve after biological death, which is not conducive to the enrichment of organic matter. The deposition of pyrite requires still water and strong reduction environment. Therefore, the increase of pyrite content indicates that the water body has strong reduction, which is conducive to the preservation of organic matter. For different types of laminae, the mineral content of silty felsic laminae changes the most with the TOC. For example, when the TOC increases from 0% to 5%, the content of feldspar and quartz decreases from 40% to 15-20% (Figure 11), while the content of clay increases from 30% to 60%, which indicates that the change of terrestrial input and water energy has the greatest impact on the change of TOC in this kind of lamina. Related to other types of (a) (a) laminae, the TOC of silty felsic laminae is the lowest, so it basically contains no pyrite. The relationship between minerals and organic matter in organic-bearing clay lamina is basically similar to that of silty felsic lamina, except that the content of pyrite increases in the range of 0-10%, which is related to the increase of TOC in this kind of lamina and the enhancement of reducibility of water body. The shale of Qingshankou Formation in the Gulong sag, northern Songliao, also show this law [31], that is, the shale with high TOC (>2-5%) often contains high clay (30-45%) and lower felsic (50-70%) minerals; however, the shale with low TOC (<2) often contains high felsic (65-90%) and lower clay (5-30%) minerals. The relationship between minerals and organic matter enrichment in organic-rich clay lamina has the largest variation range, which is due to the large variation of TOC in this kind of lamina, which is 6%~24%. However, the TOC of this kind lamina has a significant relationship with quartz and pyrite. When TOC is more than 10%, the content of quartz is obviously less than 20%, while the content of pyrite is more than 10%, which basically represents the strong reduction environment of still water in deep lake area.

Geofluids
However, the content of clay minerals tends to decrease from 50% to 40%, which may be caused by the dilution of organic matter enrichment. The change relationship between minerals and organic matter in homogeneous clay layer is complex, in which the content of feldspar decreases with the increase of TOC, while that of pyrite is the opposite. However, the relationship between the content of quartz and clay minerals and the TOC is not obvious, indicating that the enrichment mechanism of organic matter in this kind of lamina is more complex and there are more influencing factors. For tuffaceous lamina, due to its low organic matter content and small number of laminae, the correlation is not very clear, too. The development of multiple laminar assemblages at the same depth also has a certain impact on the enrichment of organic matter. Firstly, the tuffaceous lamina developed by volcanic activity dilutes the TOC of the formation due to its low organic matter content or no organic matter. However, tuffaceous matter contains rich nutrients which promote the growth of algae and leads to the rapid enrichment of organic matter in the shale deposited later. Secondly, the activity of silty gravity flow also dilutes the TOC of the formation, damages the anoxic sedimentary and preservation environment, and reduces the TOC of shale deposited nearly the same time.

Conclusions
In this study, the laminae of the Chang 7 3 member in well G occur in the form of extreme thin to thin parallel plate-like, and parallel wavy and massive are locally developed. The thickness of a single lamina is between 0.05 and 1.0 mm. According to the shape, thickness, mineral composition, and organic matter content of shale lamina, the lamina types of section Chang 7 3 are divided into 5 types and 7 subtypes.
Shale minerals are mainly composed of clay, feldspar, quartz, and Pyrite, with a small amount of collophanite and carbonate. Clay mainly includes illite and illite/smectite mixed layer. Felsic minerals are mainly quartz, and some of them are developed in the form of siliceous spots and siliceous veins. SEM and probe analysis show that they come from the dissolution and precipitation of SiO 2 in feldspar. Some spherical alga fossils are filled with hydrothermal minerals of different stages, indicating that there was hydrothermal activity in diagenetic stage.
The vertical distribution of shale laminae types in Chang 7 3 member varies greatly. The middle and lower part is mainly rich in ORC and OBC, bearing a small amount of TF, and the upper part is mainly HC and SF. The organic matter in ORC and HC is mainly algae and type I, distributed in dense disseminated or lenticular shape, and the TOC is high, usually greater than 8%. The organic matter in SF and OBC is dominated by type II 1 , containing many terrigenous structures, which are sparse dispersed or laminar distribution, and the TOC is usually less than 8%.
Different laminar types deposit different minerals, representing different sedimentary and water environment. The lamina rich in clay, tuffaceous, and pyrite represents large water depth, lack of oxygen at the bottom, less terrigenous input, and good preservation conditions of organic matter, resulting in high TOC and rich shale oil resources. On the contrary, the lamina rich in silt and felsic represents more terrigenous input, turbulent water body, oxidizing environment, and poor preservation conditions of organic matter, leading to low TOC.

Data Availability
Data is not available for confidential reasons.