# Study on the Mechanism of Organic Matter Enrichment in Early Cambrian Marine Shales in the Lower Yangtze Area, South China: An Example Using Well JXY1

Authors: Sihong Cheng; Bin Li; Kun Zhang; Weiwei Liu; Jun Peng; Mingcai Hou; Ming Wen; Qingsong Xia; Xin Wang; Xiaoxue Liu; Li Zhong; Yizhou Huang; Yongyang Liu; Muhe Yuan; Yue Yao
Journal: Geofluids
 (2020)

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## Abstract

The abundance of organic matter in shales, which has a direct effect on the hydrocarbon generation potential of shales, is an important organic geochemical parameter for evaluating shale gas reservoirs. The total organic carbon content (TOC content) in shale is controlled by the abundance of original sedimentary organic matter. Therefore, it is very important to study the mechanism of organic matter enrichment in shale. In this paper, the Lower Cambrian marine shales from the Lower Yangtze region are selected as the research subject, most of which originate from a typical area well called Well JXY1. The degree of pyritization (DOP) is used to characterize the redox environment of the water body, while the P/Al ratio is used to analyze the biological productivity of paleoseawater. The paleosalinity of seawater is calculated via carbon and oxygen isotope analysis. In addition, the early Cambrian hydrothermal activities were studied by using core description; Si, Al, Fe, and Mn elemental analysis; and oxygen isotope calculations. The results show that during the early Cambrian Wangyinpu sedimentary period, the seawater was an anaerobic water body with H2S, and the oxygen concentration was approximately 0 mL/L. In the middle stages of the Wangyinpu sedimentary period, the water body had the strongest reducibility and the highest biological productivity. Moreover, the paleoocean in this period between the Yangtze plate and the Cathaysian plate was greatly affected by hydrothermal activities, with temperatures ranging from 90°C to 120°C. Active hydrothermal activities promoted high biological productivity and an anaerobic environment, both of which were conducive to the preservation and enrichment of organic matter, resulting in extremely high TOC content in the Wangyinpu shales (from 6.5% to approximately 16%).


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## Body

## 1. Introduction

As targets of geological explorations of oil and gas change from conventional reservoirs to unconventional reservoirs, the exploration and development of unconventional oil and gas (including shale gas, shale oil, and tight gas) have achieved great success in North America, and this makes the United States essentially self-sufficient in oil and gas, thus achieving “energy independence” [1–6]. There are also unconventional oil and gas resources with great potential in South China, among which are two sets of marine shales, the Upper Ordovician-Lower Silurian shales and the Lower Cambrian shales, which are the main exploration target series. Since 2010, in reference to shale gas exploration and development experience and to technology, China’s oil companies have successively implemented commercial development in Weiyuan, Changning, Zhaotong, Luzhou, Yongchuan, Jiaoshiba, Dingshan, and other shale blocks [7–10]. The organic matter is not only the hydrocarbon generation material but also the main reservoir space and seepage channel of the shale gas. Therefore, it is necessary to study the enrichment mechanism of sedimentary organic matter [11–14].Various methods have been used to study the mechanism of organic matter enrichment in marine shales from the Yangtze area of South China. Based on the sedimentary facies of the lower member of the Lower Silurian Longmaxi Formation in the Sichuan Basin, the Upper Yangtze Region, and experimental methods (polarizing microscope, X-ray diffraction, and elemental geochemical analysis), Mou et al. considered that the sedimentary facies have an impact on the geological conditions for shale gas accumulation [15]. Zhang et al. selected three Lower Cambrian stratigraphic sections in the Upper Yangtze region, and they tested the organic carbon content and trace elements of the rock samples [16]. In this paper, the variation characteristics of the primary biological productivity and redox conditions in different sedimentary stages of the early Cambrian were analyzed in addition to their effects on organic matter enrichment. Qiu et al. studied the organic carbon content and trace element geochemistry of 30 shale samples from the bottom of the Upper Ordovician Wufeng Formation to the Lower Silurian Longmaxi formation in the Tianba sections of the Wuxi block, Sichuan Basin, and they analyzed the enrichment characteristics and control factors of the organic matter in different intervals [17]. This work argued that sea level fluctuation controls the oxygen deficiency to an extent, which affects the deposition and enrichment of organic matter in the area. He et al. analyzed the relationship between the sedimentary environment and the enrichment of organic matter in the Upper Ordovician Wufeng black shales, the marl of the Guanyinqiao marls, and the Lower Silurian Longmaxi black shales in the Sichuan Basin, Upper Yangtze region, by using geochemical methods to determine organic carbon, sulfur, and trace elements [18].Shale formations contain Fe, S, U, Th, Mg, Ca, Al, Fe, Mn, Ba, and other elements, which provide important evidence for the analysis of the paleosedimentary environment [19–23]. Moreover, carbon and oxygen isotopes can be used to quantitatively calculate the paleotemperature of seawater and to describe the paleoenvironment more accurately. Therefore, this paper combines core description, element analysis, and isotope calculation to study the mechanism of organic matter accumulation in marine shales.


## 2. Geological Settings

### 2.1. Sedimentary and Stratigraphic Characteristics

In the early Cambrian, the sedimentary facies environment of the Lower Yangtze region included ancient land, onshore, shallow shelf, deep shelf, continental slope, and ocean basin sections from northwest to southeast; meanwhile, in this period, the sedimentary environment of the Cathaysian plate included ocean basin, continental slope, deep water, shallow water, onshore, and ancient land sections from northwest to southeast (as shown in Figure1(a)). The junction of the Yangtze plate and the Cathaysian plate was oceanic, with the deepest water found there, gradually becoming shallower on both sides [24, 25].Figure 1
Regional sedimentary characteristics from the early Cambrian in the Lower Yangtze region of South China. (Well JXY1 is located in the Lower Yangtze region, close to the Yangtze plate and the Cathaysian plate.) Modified from references [24, 25].During the early Cambrian, due to the large-scale global transgression, a set of strata was widely deposited on the Yangtze plate and the Cathaysian plate. This set was composed of black organic-rich siliceous shale and is one of the main targets for shale gas exploration in South China. Because of its wide distribution area, it has different names in different regions. It is called the Wangyinpu Formation to the west of the Lower Yangtze region and the Hetang Formation to the east of the Lower Yangtze region [26–30].


### 2.2. Tectonic Characteristics

Our study area is located in the Lower Yangtze region. Based on previous studies, the original continental crust in South China was two ancient plates, the Yangtze plate and the Cathaysian plate, separated by ocean basins in the early Mesoproterozoic, and the Yangtze plate is a cratonic basin [31–38].In the early Cambrian, the Yangtze and Cathaysian plates were under tensile stress. Due to the large-scale global transgression, a set of organic-rich shale was deposited. Subsequently, a large-scale regression occurred, and the water body became shallower, which led to the lithology change from fine-grained shales to coarse-grained clastic rocks, such as siltstone and sandstone. Influenced by the compression and collision of the Cathaysian plate in the Ordovician, the water body over the Yangtze plate continued to become shallower and changed from a clastic sedimentary system to a carbonate sedimentary system. In the late Ordovician-early Silurian, another large-scale transgression occurred due to the melting of glaciers, which resulted in the sedimentary system being changed into a clastic rock sedimentary system again; in addition, a set of organic shale was deposited [39–41]. From the Cambrian to the Silurian, the Yangtze plate and the Cathaysian plate continually subducted and collided. By the end of the Silurian, the Yangtze plate and the Cathaysian plate merged into the unified South China plate [42, 43].


## 2.1. Sedimentary and Stratigraphic Characteristics

In the early Cambrian, the sedimentary facies environment of the Lower Yangtze region included ancient land, onshore, shallow shelf, deep shelf, continental slope, and ocean basin sections from northwest to southeast; meanwhile, in this period, the sedimentary environment of the Cathaysian plate included ocean basin, continental slope, deep water, shallow water, onshore, and ancient land sections from northwest to southeast (as shown in Figure1(a)). The junction of the Yangtze plate and the Cathaysian plate was oceanic, with the deepest water found there, gradually becoming shallower on both sides [24, 25].Figure 1
Regional sedimentary characteristics from the early Cambrian in the Lower Yangtze region of South China. (Well JXY1 is located in the Lower Yangtze region, close to the Yangtze plate and the Cathaysian plate.) Modified from references [24, 25].During the early Cambrian, due to the large-scale global transgression, a set of strata was widely deposited on the Yangtze plate and the Cathaysian plate. This set was composed of black organic-rich siliceous shale and is one of the main targets for shale gas exploration in South China. Because of its wide distribution area, it has different names in different regions. It is called the Wangyinpu Formation to the west of the Lower Yangtze region and the Hetang Formation to the east of the Lower Yangtze region [26–30].


## 2.2. Tectonic Characteristics

Our study area is located in the Lower Yangtze region. Based on previous studies, the original continental crust in South China was two ancient plates, the Yangtze plate and the Cathaysian plate, separated by ocean basins in the early Mesoproterozoic, and the Yangtze plate is a cratonic basin [31–38].In the early Cambrian, the Yangtze and Cathaysian plates were under tensile stress. Due to the large-scale global transgression, a set of organic-rich shale was deposited. Subsequently, a large-scale regression occurred, and the water body became shallower, which led to the lithology change from fine-grained shales to coarse-grained clastic rocks, such as siltstone and sandstone. Influenced by the compression and collision of the Cathaysian plate in the Ordovician, the water body over the Yangtze plate continued to become shallower and changed from a clastic sedimentary system to a carbonate sedimentary system. In the late Ordovician-early Silurian, another large-scale transgression occurred due to the melting of glaciers, which resulted in the sedimentary system being changed into a clastic rock sedimentary system again; in addition, a set of organic shale was deposited [39–41]. From the Cambrian to the Silurian, the Yangtze plate and the Cathaysian plate continually subducted and collided. By the end of the Silurian, the Yangtze plate and the Cathaysian plate merged into the unified South China plate [42, 43].


## 3. Samples, Experiments, and Data Sources

In this paper, the shale samples come from the Lower Cambrian Wangyinpu Formation in Well JXY1, which is a shale gas cored well located in the Xiuwu Basin in the Lower Yangtze area of the Yangtze plate. Since the study area in the early Cambrian was marine sedimentary facies with little variation, this paper chose Well JXY1 as a typical well to study the organic matter enrichment mechanism in the Lower Yangtze area. In this study, the TOC content of 87 core samples was measured using an OG-2000V TOC analyzer. In addition, the Al, Fe, Mn, and Ba elements of 53 core samples from the Lower Cambrian Wangyinpu Formation from Well JXY1 were analyzed by X-ray fluorescence using an Axios mAX spectrometer. Oxygen isotope analyses of core samples from 2634 m to 2649 m of the Lower Cambrian Wangyinpu Formation in Well JXY1 were determined using a Thermo Fisher MAT 253 stable isotope mass spectrometer. This paper also collected the Fe, S, U, Th, Mg, and Ca logging data of Well JXY1, as provided by Schlumberger. The sampling interval of logging data is 0.125 m.


## 4. Results and Discussion

### 4.1. Redox Environment

The degree of pyritization (DOP) is the most commonly used indicator of the redox environment, which is the ratio of iron in pyrite to total reactive iron (iron in pyrite plus iron dissolved in hydrochloric acid) [44]. Because the ratio of iron in pyrite to total iron in the sample (DOPT) is approximately DOP [45, 46], DOPT is used instead of DOP in this study. When estimating the iron content in pyrite, all sulfur elements are assumed to exist in the form of pyrite (FeS2). DOPT is calculated according to the following formula:
(1)DOPT=55.8564.13×SSFeS.55.85 and 64.13 are the atomic masses of the Fe and S elements in pyrite, respectively; SS is the measured sulfur content; and FeS is the total Fe content in the sample.Paleooxygenation facies (POF) is an important parameter to characterize the dissolved oxygen content in water, including the oxic facies (O2content>2mL/L), dysoxic facies (O2 content between 0.2 and 2 mL/L), suboxic facies (O2 content between 0 and 0.2 mL/L), and anoxic facies (O2content=0mL/L) [47]. Pang et al. and Zhang et al. defined DOP characteristics in three sedimentary environments: (1) aerobic environment (including oxic and dysoxic facies), DOPT<0.42; (2) anaerobic environment without H2S (suboxic facies), 0.42<DOPT<0.75; and (3) anaerobic environment without oxygen but with H2S (anoxic facies), DOPT>0.75 [40, 41]. In this paper, DOPT is calculated by using the logging data of Fe and S elements of the Lower Cambrian Wangyinpu Formation of the Cambrian section in Well JXY1. As shown in Figure 2, the DOPT of the whole well of the Wangyinpu Formation was higher than 0.75 and was higher than 1 in the middle part of the Wangyinpu Formation; thus, during the early Cambrian Wangyinpu sedimentary period, the seawater in the research area was an anaerobic environment with H2S, and its reducibility was the strongest in the middle stage of the Wangyinpu sedimentary period.Figure 2
Redox environment index (DOPT) and biological productivity (P/Al) of the Lower Cambrian Wangyinpu Formation in Well JXY1. See Figure 1 for the well location.


### 4.2. Biological Productivity

The premise of organic matter enrichment in shales is that the environment provides sufficient organic matter sources; thus, the seawater needs to have a high level of primary productivity [48]. Here, P is not only one of the most critical nutrient elements in biological metabolism but also a component of many marine biological skeletons, which are deposited in sediments after the death of organisms. Therefore, P is widely used to determine the level of biological productivity [49, 50]. Since P in terrestrial and authigenic minerals may cause inaccuracies in determining biological productivity, P/Al can better reflect the primary productivity of paleooceans than P [51, 52]. As shown in Figure 2, the P/Al in the middle part of the Lower Cambrian Wangyinpu Formation is higher than those of other sections in the JXY1 well, which indicates that the level of biological productivity is highest in the middle stage of the early Cambrian Wangyinpu sedimentary period.


### 4.3. Hydrothermal Activities

#### 4.3.1. Core Description

Shales with horizontal bedding and block bedding were developed in the deep sea where the sedimentary environment was relatively calm [53–56]. If there were hydrothermal activities on the seabed, some special sedimentary structures are easily formed in the relatively soft seabed sediments due to the high velocity and large flow rate, so these structures would provide evidence of hydrothermal activities.(1) Vein Structures. A large number of vein-like ore bodies are often found in the Lower Cambrian Wangyinpu shales, which are distributed in the form of network veins. It shows that this is a structure formed by fractures filled with barite (Figure 3(a)). Because the seabed sediments were affected by hydrothermal fluids before consolidation, strong deformation structures were found in the shales.Figure 3
Sedimentary structures of the Wangyinpu shales in Well JXY1: (a) vein structure, (b) contraction-like structures, and (c, d) contemporaneous deformed structures. See Figure1 for the well location.
(a)(b)(c)(d)(2) Contraction-Like Structures. Some structures similar to desiccation cracks were often found in carbonaceous shales, and the cracks were often filled with barite components (Figure 3(b)), which are typical features of cracks formed by hydrothermal exhalation.(3) Contemporaneous Deformed Structures. Clay minerals, organic matter, and siliceous minerals were deposited in the deep sea, forming soft sediments. Due to the influence of hydrothermal exhalation, a large number of contemporaneous deformed structures, such as convoluted structures, were formed on these sediments (Figures 3(c) and 3(d)) [57, 58].


#### 4.3.2. Elemental Analysis

To accurately determine whether there is hydrothermal activity in the study area, excess siliceous mineral content was used for analysis in this study [59–63]. Excess siliceous mineral content (abbreviated Siex) refers to all siliceous minerals except those from terrestrial clastic deposition and can be calculated by the following formula:
(2)Siex=Sis−SiAlbg×Als.Sis is the Si content in the samples, AlS is the Al content in the samples, and the (Si/Al)bg value is 3.11, which is the average content in shales [64].Figure4 shows the results when using this formula to calculate the excess siliceous mineral content from the Lower Cambrian Wangyinpu Formation section of Well JXY1. Excess siliceous minerals existed in most intervals of the Wangyinpu Formation. In the layers where excess siliceous minerals are present, the excess siliceous mineral content in half of the layers is between 20% and 30%, and the excess siliceous content in some layers is between 30% and 40%, even reaching as high as 40% to 50%. Wedepohl, Adachi et al., and Yamamoto proposed a method of using the Al-Fe-Mn ternary plot to determine whether siliceous minerals are derived from hydrothermal origins or biogenesis [65–67]. In this paper, the elemental analysis values of Al, Fe, and Mn in the layers with excess siliceous minerals from the Lower Cambrian Wangyinpu Formation from Well JXY1 are plotted in the triangular diagram. As shown in Figure 5, the numerical value falls within the range of a hydrothermal origin, which indicates that the excess siliceous minerals are derived from a hydrothermal origin.Figure 4
Excess silicon and TOC content of the Lower Cambrian Wangyinpu Formation in the Yangtze area from Well JXY1. See Figure1 for the well location.Figure 5
Through the Al-Fe-Mn ternary plot analysis, siliceous minerals from the Lower Cambrian Wangyinpu Formation in Well JXY1 contain excess siliceous minerals, which are derived from hydrothermal origins. See Figure1 for the well location.


#### 4.3.3. Hydrothermal Temperature Calculation

Oxygen isotopes in shale can be used to determine the genesis of siliceous minerals [68, 69]. Siliceous minerals from different biogenesis origins have different δ18O values. The specific method is shown in Table 1.Table 1
Sources of siliceous minerals determined byδ18O value.
δ18O (SMOW)Siliceous sourcesMagmatic rocksMetamorphic rocksHydrothermalArenaceous quartzRange8.3‰~11.2‰11.2‰~16.4‰12.2‰~23.6‰10.3‰~12.5‰Theδ18O value of the Lower Cambrian Wangyinpu Formation from Well JXY1 is in accordance with the PDB standard. The experimental results are shown in Table 2. According to the formula
(3)δSMOW=1.03086δPDB+30.86.Table 2
Conversion ofδ18O values under the PDB standard and SMOW standard and calculation results of paleoseawater temperature.
No.δ18O (‰)Paleotemperature of seawater (°C)PDBSMOWBy Equation (4)By Equation (5)1-10.4720.0790.5486.712-13.5916.85118.5699.92Theδ18O value under the PDB standard is converted into the δ18O value of the SMOW standard.Table2 shows that the δ18O values of the SMOW standard in the Lower Cambrian Wangyinpu shales are 16.85‰ and 20.07‰, indicating that the oxygen isotope values of the shale siliceous minerals in the study area are within the range of hydrothermal origins (12.2‰ to 23.6‰), which means that the Lower Cambrian Wangyinpu shales were affected by hydrothermal activities.Oxygen isotopes in the shale can be used to calculate the temperature of the ancient ocean, as shown in the following two empirical formulas:(4)δ18Oshale−δ18Oseawater=3.09×106T2−3.29,(5)=5.0−4.1×δ18Oshale−δ18Oseawater−40.δ18O (shale) is the oxygen isotope in shale, and δ18O (seawater) is the oxygen isotope in a sedimentary medium (seawater). In formula (4), T is the thermodynamic temperature.In the aforementioned formulas, theδ18O in paleoseawater is unknown, but previous studies show that the δ18O in seawater has changed very little, considering the past and present values. Thus, in this study, the δ18O of paleoseawater is assumed to be the same as that of present seawater values, which is 0‰.This formula has been used to calculate the seawater temperature of other areas during the deposition of Lower Silurian, Lower Cambrian, and siliceous rocks. This paper also uses two formulas to calculate the seawater temperature with reference to the previous papers [70–72]. Based on the above assumptions, the results of the paleoseawater temperature calculations are shown in Table 2. According to formula (4), the temperature calculation results of the early Cambrian paleoseawater in the study area (Nos. 1-2) were 90.54°C and 118.56°C, while according to formula (5), the results were 86.71°C and 99.92°C, respectively. According to Hearing et al. (2018), the seawater temperature near the equator in the early Cambrian ranged from 35°C to 45°C, indicating that the paleoseawater between the Yangtze plate and the Cathaysian plate in the early Cambrian was greatly affected by hydrothermal activities.


#### 4.3.4. Effects of Hydrothermal Activities on Sedimentary Organic Matter Enrichment

The existence of hydrothermal silicon in Well JXY1 was related to the active compression between the Yangtze and Cathaysian plates during the early Cambrian [31–33]. The hydrothermal activities formed siliceous minerals in shale, which had an impact on the redox conditions and bioproductivity of water bodies, and thus, this affected the abundance of sedimentary organic matter.The research conducted by Sun et al. and Zhang et al. found that reduced hydrothermal fluids sank to the seafloor to form an oxygen-deficient environment that was conducive to organic matter preservation [73–75]. The redox conditions of the water body were also related to the hydrothermal activity in the study area during the early Cambrian. Figures 2 and 4 show that in some layers with higher hydrothermal silicon content, the DOPT was also high, which shows a positive correlation with the hydrothermal silicon content; in addition, this indicated frequent hydrothermal activities in the early Cambrian. The DOPT of all layers in the Lower Cambrian Wangyinpu Formation was greater than 0.75, with some layers being greater than 1.5, which indicates that during the early Cambrian Wangyinpu sedimentary period, the water body in the research area was an anaerobic environment with H2S.It is generally accepted by many scholars that hydrothermal activities are closely related to paleoproductivity. Halbach et al. studied the hydrothermal activity in the Fiji Basin, and they found that the closer the area is to the hydrothermal activity zone, the greater the number and activity of organisms [76]. In addition, in the hydrothermal activity zone, the abundance of these organisms will be 1 to 3 orders of magnitude higher than that in the normal ocean surface. McKibben et al. (1990) and Korzhinsky et al. (1994) argued that hydrothermal fluids could carry many rare elements on the surface of the crust and that these dissolved trace elements contain several essential nutrients (Si, N, P, Fe, and Zn) for marine life. In addition, trace elements existing in the bodies of these organisms can be in the form of “sea snow,” which sinks to the seafloor after biological death and provides a source of organic enrichment for the source rocks [77, 78].Similarly, biological productivity in the study area also has some correlation with hydrothermal activities during the early Cambrian. As shown in Figures2 and 4, hydrothermal activity in the early Cambrian was frequent. Among the layers with high silicon content, the P/Al values used to characterize biological productivity were relatively higher than those of the other layers with weak hydrothermal activities.The relationships between the DOPT and TOC content and the P/Al and TOC content were statistically analyzed (Figure 6). It was found that both of them were positively correlated, which means that the higher the reducibility of water and the higher the biological productivity, the higher the TOC content of shale. Active hydrothermal activities during the early Cambrian resulted in a high level of biological productivity and an anaerobic environment with H2S, and this caused an increase in the TOC content of up to 6.5%-14% in the lower part of the present-day Wangyinpu Formations (Figure 5).Figure 6
The correlation diagrams of DOPT and TOC content (a) and P/Al and TOC content (b) in the redox environment are all positive.
(a)(b)


### 4.4. Organic Matter Enrichment Mechanism

In the early Cambrian, the Yangtze plate and the Cathaysian plate were separated by the paleoocean. During the Wangyinpu sedimentary period, large-scale transgression occurred [79]. Hydrothermal fluids rich in silicon, uranium, and other mineral elements entered the ocean basin in the deep crust due to the extension between the Cathaysian plate and the Yangtze plate and to the shelf area under the action of upwelling. Its temperature ranged from 90 to 120°C. On the one hand, the hydrothermal solution enters the surface of the sea and carries nutrients to promote the growth and reproduction of plankton and to increase biological productivity. On the other hand, it forms an anaerobic environment without oxygen but with H2S on the bottom of the sea, which is beneficial to the preservation of the original sedimentary organic matter. Both factors are beneficial to the enrichment of sedimentary organic matter (Figure 7).Figure 7
Mechanism of organic matter enrichment in the early Cambrian Wangyinpu Formation in the Lower Yangtze area.


## 4.1. Redox Environment

The degree of pyritization (DOP) is the most commonly used indicator of the redox environment, which is the ratio of iron in pyrite to total reactive iron (iron in pyrite plus iron dissolved in hydrochloric acid) [44]. Because the ratio of iron in pyrite to total iron in the sample (DOPT) is approximately DOP [45, 46], DOPT is used instead of DOP in this study. When estimating the iron content in pyrite, all sulfur elements are assumed to exist in the form of pyrite (FeS2). DOPT is calculated according to the following formula:
(1)DOPT=55.8564.13×SSFeS.55.85 and 64.13 are the atomic masses of the Fe and S elements in pyrite, respectively; SS is the measured sulfur content; and FeS is the total Fe content in the sample.Paleooxygenation facies (POF) is an important parameter to characterize the dissolved oxygen content in water, including the oxic facies (O2content>2mL/L), dysoxic facies (O2 content between 0.2 and 2 mL/L), suboxic facies (O2 content between 0 and 0.2 mL/L), and anoxic facies (O2content=0mL/L) [47]. Pang et al. and Zhang et al. defined DOP characteristics in three sedimentary environments: (1) aerobic environment (including oxic and dysoxic facies), DOPT<0.42; (2) anaerobic environment without H2S (suboxic facies), 0.42<DOPT<0.75; and (3) anaerobic environment without oxygen but with H2S (anoxic facies), DOPT>0.75 [40, 41]. In this paper, DOPT is calculated by using the logging data of Fe and S elements of the Lower Cambrian Wangyinpu Formation of the Cambrian section in Well JXY1. As shown in Figure 2, the DOPT of the whole well of the Wangyinpu Formation was higher than 0.75 and was higher than 1 in the middle part of the Wangyinpu Formation; thus, during the early Cambrian Wangyinpu sedimentary period, the seawater in the research area was an anaerobic environment with H2S, and its reducibility was the strongest in the middle stage of the Wangyinpu sedimentary period.Figure 2
Redox environment index (DOPT) and biological productivity (P/Al) of the Lower Cambrian Wangyinpu Formation in Well JXY1. See Figure 1 for the well location.


## 4.2. Biological Productivity

The premise of organic matter enrichment in shales is that the environment provides sufficient organic matter sources; thus, the seawater needs to have a high level of primary productivity [48]. Here, P is not only one of the most critical nutrient elements in biological metabolism but also a component of many marine biological skeletons, which are deposited in sediments after the death of organisms. Therefore, P is widely used to determine the level of biological productivity [49, 50]. Since P in terrestrial and authigenic minerals may cause inaccuracies in determining biological productivity, P/Al can better reflect the primary productivity of paleooceans than P [51, 52]. As shown in Figure 2, the P/Al in the middle part of the Lower Cambrian Wangyinpu Formation is higher than those of other sections in the JXY1 well, which indicates that the level of biological productivity is highest in the middle stage of the early Cambrian Wangyinpu sedimentary period.


## 4.3. Hydrothermal Activities

### 4.3.1. Core Description

Shales with horizontal bedding and block bedding were developed in the deep sea where the sedimentary environment was relatively calm [53–56]. If there were hydrothermal activities on the seabed, some special sedimentary structures are easily formed in the relatively soft seabed sediments due to the high velocity and large flow rate, so these structures would provide evidence of hydrothermal activities.(1) Vein Structures. A large number of vein-like ore bodies are often found in the Lower Cambrian Wangyinpu shales, which are distributed in the form of network veins. It shows that this is a structure formed by fractures filled with barite (Figure 3(a)). Because the seabed sediments were affected by hydrothermal fluids before consolidation, strong deformation structures were found in the shales.Figure 3
Sedimentary structures of the Wangyinpu shales in Well JXY1: (a) vein structure, (b) contraction-like structures, and (c, d) contemporaneous deformed structures. See Figure1 for the well location.
(a)(b)(c)(d)(2) Contraction-Like Structures. Some structures similar to desiccation cracks were often found in carbonaceous shales, and the cracks were often filled with barite components (Figure 3(b)), which are typical features of cracks formed by hydrothermal exhalation.(3) Contemporaneous Deformed Structures. Clay minerals, organic matter, and siliceous minerals were deposited in the deep sea, forming soft sediments. Due to the influence of hydrothermal exhalation, a large number of contemporaneous deformed structures, such as convoluted structures, were formed on these sediments (Figures 3(c) and 3(d)) [57, 58].


### 4.3.2. Elemental Analysis

To accurately determine whether there is hydrothermal activity in the study area, excess siliceous mineral content was used for analysis in this study [59–63]. Excess siliceous mineral content (abbreviated Siex) refers to all siliceous minerals except those from terrestrial clastic deposition and can be calculated by the following formula:
(2)Siex=Sis−SiAlbg×Als.Sis is the Si content in the samples, AlS is the Al content in the samples, and the (Si/Al)bg value is 3.11, which is the average content in shales [64].Figure4 shows the results when using this formula to calculate the excess siliceous mineral content from the Lower Cambrian Wangyinpu Formation section of Well JXY1. Excess siliceous minerals existed in most intervals of the Wangyinpu Formation. In the layers where excess siliceous minerals are present, the excess siliceous mineral content in half of the layers is between 20% and 30%, and the excess siliceous content in some layers is between 30% and 40%, even reaching as high as 40% to 50%. Wedepohl, Adachi et al., and Yamamoto proposed a method of using the Al-Fe-Mn ternary plot to determine whether siliceous minerals are derived from hydrothermal origins or biogenesis [65–67]. In this paper, the elemental analysis values of Al, Fe, and Mn in the layers with excess siliceous minerals from the Lower Cambrian Wangyinpu Formation from Well JXY1 are plotted in the triangular diagram. As shown in Figure 5, the numerical value falls within the range of a hydrothermal origin, which indicates that the excess siliceous minerals are derived from a hydrothermal origin.Figure 4
Excess silicon and TOC content of the Lower Cambrian Wangyinpu Formation in the Yangtze area from Well JXY1. See Figure1 for the well location.Figure 5
Through the Al-Fe-Mn ternary plot analysis, siliceous minerals from the Lower Cambrian Wangyinpu Formation in Well JXY1 contain excess siliceous minerals, which are derived from hydrothermal origins. See Figure1 for the well location.


### 4.3.3. Hydrothermal Temperature Calculation

Oxygen isotopes in shale can be used to determine the genesis of siliceous minerals [68, 69]. Siliceous minerals from different biogenesis origins have different δ18O values. The specific method is shown in Table 1.Table 1
Sources of siliceous minerals determined byδ18O value.
δ18O (SMOW)Siliceous sourcesMagmatic rocksMetamorphic rocksHydrothermalArenaceous quartzRange8.3‰~11.2‰11.2‰~16.4‰12.2‰~23.6‰10.3‰~12.5‰Theδ18O value of the Lower Cambrian Wangyinpu Formation from Well JXY1 is in accordance with the PDB standard. The experimental results are shown in Table 2. According to the formula
(3)δSMOW=1.03086δPDB+30.86.Table 2
Conversion ofδ18O values under the PDB standard and SMOW standard and calculation results of paleoseawater temperature.
No.δ18O (‰)Paleotemperature of seawater (°C)PDBSMOWBy Equation (4)By Equation (5)1-10.4720.0790.5486.712-13.5916.85118.5699.92Theδ18O value under the PDB standard is converted into the δ18O value of the SMOW standard.Table2 shows that the δ18O values of the SMOW standard in the Lower Cambrian Wangyinpu shales are 16.85‰ and 20.07‰, indicating that the oxygen isotope values of the shale siliceous minerals in the study area are within the range of hydrothermal origins (12.2‰ to 23.6‰), which means that the Lower Cambrian Wangyinpu shales were affected by hydrothermal activities.Oxygen isotopes in the shale can be used to calculate the temperature of the ancient ocean, as shown in the following two empirical formulas:(4)δ18Oshale−δ18Oseawater=3.09×106T2−3.29,(5)=5.0−4.1×δ18Oshale−δ18Oseawater−40.δ18O (shale) is the oxygen isotope in shale, and δ18O (seawater) is the oxygen isotope in a sedimentary medium (seawater). In formula (4), T is the thermodynamic temperature.In the aforementioned formulas, theδ18O in paleoseawater is unknown, but previous studies show that the δ18O in seawater has changed very little, considering the past and present values. Thus, in this study, the δ18O of paleoseawater is assumed to be the same as that of present seawater values, which is 0‰.This formula has been used to calculate the seawater temperature of other areas during the deposition of Lower Silurian, Lower Cambrian, and siliceous rocks. This paper also uses two formulas to calculate the seawater temperature with reference to the previous papers [70–72]. Based on the above assumptions, the results of the paleoseawater temperature calculations are shown in Table 2. According to formula (4), the temperature calculation results of the early Cambrian paleoseawater in the study area (Nos. 1-2) were 90.54°C and 118.56°C, while according to formula (5), the results were 86.71°C and 99.92°C, respectively. According to Hearing et al. (2018), the seawater temperature near the equator in the early Cambrian ranged from 35°C to 45°C, indicating that the paleoseawater between the Yangtze plate and the Cathaysian plate in the early Cambrian was greatly affected by hydrothermal activities.


### 4.3.4. Effects of Hydrothermal Activities on Sedimentary Organic Matter Enrichment

The existence of hydrothermal silicon in Well JXY1 was related to the active compression between the Yangtze and Cathaysian plates during the early Cambrian [31–33]. The hydrothermal activities formed siliceous minerals in shale, which had an impact on the redox conditions and bioproductivity of water bodies, and thus, this affected the abundance of sedimentary organic matter.The research conducted by Sun et al. and Zhang et al. found that reduced hydrothermal fluids sank to the seafloor to form an oxygen-deficient environment that was conducive to organic matter preservation [73–75]. The redox conditions of the water body were also related to the hydrothermal activity in the study area during the early Cambrian. Figures 2 and 4 show that in some layers with higher hydrothermal silicon content, the DOPT was also high, which shows a positive correlation with the hydrothermal silicon content; in addition, this indicated frequent hydrothermal activities in the early Cambrian. The DOPT of all layers in the Lower Cambrian Wangyinpu Formation was greater than 0.75, with some layers being greater than 1.5, which indicates that during the early Cambrian Wangyinpu sedimentary period, the water body in the research area was an anaerobic environment with H2S.It is generally accepted by many scholars that hydrothermal activities are closely related to paleoproductivity. Halbach et al. studied the hydrothermal activity in the Fiji Basin, and they found that the closer the area is to the hydrothermal activity zone, the greater the number and activity of organisms [76]. In addition, in the hydrothermal activity zone, the abundance of these organisms will be 1 to 3 orders of magnitude higher than that in the normal ocean surface. McKibben et al. (1990) and Korzhinsky et al. (1994) argued that hydrothermal fluids could carry many rare elements on the surface of the crust and that these dissolved trace elements contain several essential nutrients (Si, N, P, Fe, and Zn) for marine life. In addition, trace elements existing in the bodies of these organisms can be in the form of “sea snow,” which sinks to the seafloor after biological death and provides a source of organic enrichment for the source rocks [77, 78].Similarly, biological productivity in the study area also has some correlation with hydrothermal activities during the early Cambrian. As shown in Figures2 and 4, hydrothermal activity in the early Cambrian was frequent. Among the layers with high silicon content, the P/Al values used to characterize biological productivity were relatively higher than those of the other layers with weak hydrothermal activities.The relationships between the DOPT and TOC content and the P/Al and TOC content were statistically analyzed (Figure 6). It was found that both of them were positively correlated, which means that the higher the reducibility of water and the higher the biological productivity, the higher the TOC content of shale. Active hydrothermal activities during the early Cambrian resulted in a high level of biological productivity and an anaerobic environment with H2S, and this caused an increase in the TOC content of up to 6.5%-14% in the lower part of the present-day Wangyinpu Formations (Figure 5).Figure 6
The correlation diagrams of DOPT and TOC content (a) and P/Al and TOC content (b) in the redox environment are all positive.
(a)(b)


## 4.3.1. Core Description

Shales with horizontal bedding and block bedding were developed in the deep sea where the sedimentary environment was relatively calm [53–56]. If there were hydrothermal activities on the seabed, some special sedimentary structures are easily formed in the relatively soft seabed sediments due to the high velocity and large flow rate, so these structures would provide evidence of hydrothermal activities.(1) Vein Structures. A large number of vein-like ore bodies are often found in the Lower Cambrian Wangyinpu shales, which are distributed in the form of network veins. It shows that this is a structure formed by fractures filled with barite (Figure 3(a)). Because the seabed sediments were affected by hydrothermal fluids before consolidation, strong deformation structures were found in the shales.Figure 3
Sedimentary structures of the Wangyinpu shales in Well JXY1: (a) vein structure, (b) contraction-like structures, and (c, d) contemporaneous deformed structures. See Figure1 for the well location.
(a)(b)(c)(d)(2) Contraction-Like Structures. Some structures similar to desiccation cracks were often found in carbonaceous shales, and the cracks were often filled with barite components (Figure 3(b)), which are typical features of cracks formed by hydrothermal exhalation.(3) Contemporaneous Deformed Structures. Clay minerals, organic matter, and siliceous minerals were deposited in the deep sea, forming soft sediments. Due to the influence of hydrothermal exhalation, a large number of contemporaneous deformed structures, such as convoluted structures, were formed on these sediments (Figures 3(c) and 3(d)) [57, 58].


## 4.3.2. Elemental Analysis

To accurately determine whether there is hydrothermal activity in the study area, excess siliceous mineral content was used for analysis in this study [59–63]. Excess siliceous mineral content (abbreviated Siex) refers to all siliceous minerals except those from terrestrial clastic deposition and can be calculated by the following formula:
(2)Siex=Sis−SiAlbg×Als.Sis is the Si content in the samples, AlS is the Al content in the samples, and the (Si/Al)bg value is 3.11, which is the average content in shales [64].Figure4 shows the results when using this formula to calculate the excess siliceous mineral content from the Lower Cambrian Wangyinpu Formation section of Well JXY1. Excess siliceous minerals existed in most intervals of the Wangyinpu Formation. In the layers where excess siliceous minerals are present, the excess siliceous mineral content in half of the layers is between 20% and 30%, and the excess siliceous content in some layers is between 30% and 40%, even reaching as high as 40% to 50%. Wedepohl, Adachi et al., and Yamamoto proposed a method of using the Al-Fe-Mn ternary plot to determine whether siliceous minerals are derived from hydrothermal origins or biogenesis [65–67]. In this paper, the elemental analysis values of Al, Fe, and Mn in the layers with excess siliceous minerals from the Lower Cambrian Wangyinpu Formation from Well JXY1 are plotted in the triangular diagram. As shown in Figure 5, the numerical value falls within the range of a hydrothermal origin, which indicates that the excess siliceous minerals are derived from a hydrothermal origin.Figure 4
Excess silicon and TOC content of the Lower Cambrian Wangyinpu Formation in the Yangtze area from Well JXY1. See Figure1 for the well location.Figure 5
Through the Al-Fe-Mn ternary plot analysis, siliceous minerals from the Lower Cambrian Wangyinpu Formation in Well JXY1 contain excess siliceous minerals, which are derived from hydrothermal origins. See Figure1 for the well location.


## 4.3.3. Hydrothermal Temperature Calculation

Oxygen isotopes in shale can be used to determine the genesis of siliceous minerals [68, 69]. Siliceous minerals from different biogenesis origins have different δ18O values. The specific method is shown in Table 1.Table 1
Sources of siliceous minerals determined byδ18O value.
δ18O (SMOW)Siliceous sourcesMagmatic rocksMetamorphic rocksHydrothermalArenaceous quartzRange8.3‰~11.2‰11.2‰~16.4‰12.2‰~23.6‰10.3‰~12.5‰Theδ18O value of the Lower Cambrian Wangyinpu Formation from Well JXY1 is in accordance with the PDB standard. The experimental results are shown in Table 2. According to the formula
(3)δSMOW=1.03086δPDB+30.86.Table 2
Conversion ofδ18O values under the PDB standard and SMOW standard and calculation results of paleoseawater temperature.
No.δ18O (‰)Paleotemperature of seawater (°C)PDBSMOWBy Equation (4)By Equation (5)1-10.4720.0790.5486.712-13.5916.85118.5699.92Theδ18O value under the PDB standard is converted into the δ18O value of the SMOW standard.Table2 shows that the δ18O values of the SMOW standard in the Lower Cambrian Wangyinpu shales are 16.85‰ and 20.07‰, indicating that the oxygen isotope values of the shale siliceous minerals in the study area are within the range of hydrothermal origins (12.2‰ to 23.6‰), which means that the Lower Cambrian Wangyinpu shales were affected by hydrothermal activities.Oxygen isotopes in the shale can be used to calculate the temperature of the ancient ocean, as shown in the following two empirical formulas:(4)δ18Oshale−δ18Oseawater=3.09×106T2−3.29,(5)=5.0−4.1×δ18Oshale−δ18Oseawater−40.δ18O (shale) is the oxygen isotope in shale, and δ18O (seawater) is the oxygen isotope in a sedimentary medium (seawater). In formula (4), T is the thermodynamic temperature.In the aforementioned formulas, theδ18O in paleoseawater is unknown, but previous studies show that the δ18O in seawater has changed very little, considering the past and present values. Thus, in this study, the δ18O of paleoseawater is assumed to be the same as that of present seawater values, which is 0‰.This formula has been used to calculate the seawater temperature of other areas during the deposition of Lower Silurian, Lower Cambrian, and siliceous rocks. This paper also uses two formulas to calculate the seawater temperature with reference to the previous papers [70–72]. Based on the above assumptions, the results of the paleoseawater temperature calculations are shown in Table 2. According to formula (4), the temperature calculation results of the early Cambrian paleoseawater in the study area (Nos. 1-2) were 90.54°C and 118.56°C, while according to formula (5), the results were 86.71°C and 99.92°C, respectively. According to Hearing et al. (2018), the seawater temperature near the equator in the early Cambrian ranged from 35°C to 45°C, indicating that the paleoseawater between the Yangtze plate and the Cathaysian plate in the early Cambrian was greatly affected by hydrothermal activities.


## 4.3.4. Effects of Hydrothermal Activities on Sedimentary Organic Matter Enrichment

The existence of hydrothermal silicon in Well JXY1 was related to the active compression between the Yangtze and Cathaysian plates during the early Cambrian [31–33]. The hydrothermal activities formed siliceous minerals in shale, which had an impact on the redox conditions and bioproductivity of water bodies, and thus, this affected the abundance of sedimentary organic matter.The research conducted by Sun et al. and Zhang et al. found that reduced hydrothermal fluids sank to the seafloor to form an oxygen-deficient environment that was conducive to organic matter preservation [73–75]. The redox conditions of the water body were also related to the hydrothermal activity in the study area during the early Cambrian. Figures 2 and 4 show that in some layers with higher hydrothermal silicon content, the DOPT was also high, which shows a positive correlation with the hydrothermal silicon content; in addition, this indicated frequent hydrothermal activities in the early Cambrian. The DOPT of all layers in the Lower Cambrian Wangyinpu Formation was greater than 0.75, with some layers being greater than 1.5, which indicates that during the early Cambrian Wangyinpu sedimentary period, the water body in the research area was an anaerobic environment with H2S.It is generally accepted by many scholars that hydrothermal activities are closely related to paleoproductivity. Halbach et al. studied the hydrothermal activity in the Fiji Basin, and they found that the closer the area is to the hydrothermal activity zone, the greater the number and activity of organisms [76]. In addition, in the hydrothermal activity zone, the abundance of these organisms will be 1 to 3 orders of magnitude higher than that in the normal ocean surface. McKibben et al. (1990) and Korzhinsky et al. (1994) argued that hydrothermal fluids could carry many rare elements on the surface of the crust and that these dissolved trace elements contain several essential nutrients (Si, N, P, Fe, and Zn) for marine life. In addition, trace elements existing in the bodies of these organisms can be in the form of “sea snow,” which sinks to the seafloor after biological death and provides a source of organic enrichment for the source rocks [77, 78].Similarly, biological productivity in the study area also has some correlation with hydrothermal activities during the early Cambrian. As shown in Figures2 and 4, hydrothermal activity in the early Cambrian was frequent. Among the layers with high silicon content, the P/Al values used to characterize biological productivity were relatively higher than those of the other layers with weak hydrothermal activities.The relationships between the DOPT and TOC content and the P/Al and TOC content were statistically analyzed (Figure 6). It was found that both of them were positively correlated, which means that the higher the reducibility of water and the higher the biological productivity, the higher the TOC content of shale. Active hydrothermal activities during the early Cambrian resulted in a high level of biological productivity and an anaerobic environment with H2S, and this caused an increase in the TOC content of up to 6.5%-14% in the lower part of the present-day Wangyinpu Formations (Figure 5).Figure 6
The correlation diagrams of DOPT and TOC content (a) and P/Al and TOC content (b) in the redox environment are all positive.
(a)(b)


## 4.4. Organic Matter Enrichment Mechanism

In the early Cambrian, the Yangtze plate and the Cathaysian plate were separated by the paleoocean. During the Wangyinpu sedimentary period, large-scale transgression occurred [79]. Hydrothermal fluids rich in silicon, uranium, and other mineral elements entered the ocean basin in the deep crust due to the extension between the Cathaysian plate and the Yangtze plate and to the shelf area under the action of upwelling. Its temperature ranged from 90 to 120°C. On the one hand, the hydrothermal solution enters the surface of the sea and carries nutrients to promote the growth and reproduction of plankton and to increase biological productivity. On the other hand, it forms an anaerobic environment without oxygen but with H2S on the bottom of the sea, which is beneficial to the preservation of the original sedimentary organic matter. Both factors are beneficial to the enrichment of sedimentary organic matter (Figure 7).Figure 7
Mechanism of organic matter enrichment in the early Cambrian Wangyinpu Formation in the Lower Yangtze area.


## 5. Conclusions

In this paper, the Lower Cambrian marine shales from Well JXY1 in the Yangtze area of South China are selected for study as typical shales. Through TOC content testing, elemental analysis of cuttings, and the collected elemental well logging data, the following conclusions can be drawn regarding the organic matter enrichment mechanism:(1)
During the early Cambrian Wangyinpu sedimentary period, the bottom layer of seawater was in an anaerobic environment with the appearance of H2S, and the oxygen concentration was approximately 0 mL/L. The reducibility in the bottom layer of seawater was strongest in the middle stage of this period(2)
The biological productivity was highest in the middle stage of the Wangyinpu sedimentary period but relatively low in other stages(3)
The paleoseawater between the Yangtze plate and the Cathaysian plate in the early Cambrian was greatly affected by hydrothermal activities, and its temperature ranged from 90°C to 120°C. Active hydrothermal activities during the early Cambrian resulted in a high level of biological productivity and an anaerobic environment with H2S, and this caused an increase in the TOC content of up to 6.5%-14% in the lower part of the present-day Wangyinpu Formations



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*Source: 2460302-2020-08-25.xml*