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Article

Origin of the Multiple-Sourced Cherts in Maokou Carbonates in Sichuan Basin, South China

by
Haofu Zheng
1,*,
Junfeng Wu
1,
Hailei Tang
2,
Bo Liu
2,3,*,
Xiangyang Yang
1,
Kaibo Shi
3,
Kaiping Luo
4,
Qi Qiu
4 and
Yixin Dong
5
1
College of River and Ocean Engineering, Chongqing Jiaotong University, Chongqing 400074, China
2
School of Earth Sciences, Yunnan University, Kunming 650091, China
3
School of Earth and Space Sciences, Peking University, Beijing 100871, China
4
Wuxi Research Institute of Petroleum Geology, SINOPEC, Wuxi 214126, China
5
State Key Laboratory of Oil and Gas Reservoir Geology and Exploitation, Chengdu University of Technology, Chengdu 610059, China
*
Authors to whom correspondence should be addressed.
Minerals 2021, 11(11), 1269; https://doi.org/10.3390/min11111269
Submission received: 1 October 2021 / Revised: 10 November 2021 / Accepted: 11 November 2021 / Published: 15 November 2021
(This article belongs to the Special Issue The Mineralogy of the Siliceous Concretions)
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Abstract

:
Cherts have been thought to originate from biosilicification, terrestrial inputs and hydrothermal activity. The study of cherts is helpful in understanding the paleo-ocean environment and tectonic–sedimentary processes. Large amounts of cherts occur widely in the Maokou Formation in the Sichuan Basin, which may be largely connected to the Permian Chert Event (PCE). However, the source of silica and the formation process of cherts remain debated. Here, we analyze the petrographic and geochemical features of the cherts from the Guadalupian Maokou Formation (~268–259 Ma) in six sections in the Sichuan Basin. Two main types of cherts, nodular and bedded, are recognized in the Maokou Formation. The formation of nodular cherts was mainly affected by hydrothermal fluids, whereas the bedded cherts are mainly of biogenetic origin. The Emeishan large igneous province (ELIP) caused the activation of deep faults, accompanied by intense hydrothermal activities. Correspondingly, the cherts of significant hydrothermal origin developed near the active deep faults. The intensified hydrothermal activities may provide extra silica supplies and flourish the silica-secreting organisms by the associated volcanogenic upwellings that facilitated the enrichment of cherts. The study of Maokou cherts can help to record the volcanic- and silicon-related biological activities in the eastern Paleo-Tethys Ocean and can provide significant implications for chert enrichment in analogous settings.

1. Introduction

Cherts have attracted wide attention because they were formed under specific geochemical conditions, which are of great significance in the reconstruction of the paleo-ocean environment, paleotectonic activity and paleogeography [1,2,3,4,5]. During the Permian period, cherts were extensively deposited along the northeastern Panthalassic Ocean, called the Permian Chert Event (PCE) [6,7,8,9,10], which is attributed to the upwellings associated with ice melting at high latitudes [6,7]. PCE has been reported in many regions around the world, such as New Zealand, Oman, Greece, Italy, Thailand, North America and China [6,7,8,9], and is believed to have been caused by the special paleo-ocean environment.
The widespread Guadalupian cherts in the Yangtze Block in southern China are considered to be a response to PCE [4,5,11,12,13,14]. However, the origin of cherts has been associated with biological processes, terrestrial inputs and hydrothermal activity [15,16,17,18,19,20,21]. Furthermore, current studies overwhelmingly believed that the major formation of the Guadalupian cherts in the Upper Yangtze area was related to biosilicification and hydrothermal activity caused by regional tectonic and volcanic activity [4,22,23,24]. The Emeishan large igneous province (ELIP) occurred simultaneously with the enrichment of the Guadalupian cherts [25,26], suggesting a genetic link [22,24]. Alternatively, the Guadalupian cherts were formed under the influence of the silicon-rich hydrothermal fluids and volcanogenic upwellings, and they mainly accumulated in the stretched troughs related to the ELIP [5]. However, the Guadalupian cherts are characterized by multiple occurrences and heterogeneous spatial distribution, and the previous studies mainly concentrated on the cherts in the northwestern Upper Yangtze region, limiting the full explanation of the enrichment of the Guadalupian cherts.
To understand the formation mechanism thoroughly, we collected Guadalupian chert and host limestone samples from several outcrops in the Sichuan Basin. Systematic petrological and geochemical (element compositions and stable silicon isotopes) analyses were carried out to explore the siliceous sources and triggering factors for the formation of various types of cherts, and we propose a reasonable conceptual model for the origin of Guadalupian cherts in the Sichuan Basin.

2. Geological Setting

The Sichuan Basin is located on the Upper Yangtze Block in South China and has experienced multiple periods of tectonic movement (Figure 1) [27]. In the Guadalupian, the sedimentary facies of the Sichuan Basin were mainly a shallow-water carbonate platform, with extensive shoals in the central and western regions of the basin [28]. The ELIP event on the Upper Yangtze platform (Figure 1B) occurred during the Guadalupian, and the main eruption time was ~260–257 Ma [29]. The associated basalts are mainly distributed in the southwestern regions, and a small number of basalts have also been discovered near the basement faults in the central Sichuan Basin [30]. The subduction of the Jinshajiang–Mojiang Ocean Basin from south to north triggered the ELIP events and caused the extensional tectonic environment of the Upper Yangtze platform [31,32]. Therefore, the structure—sedimentary differentiation, namely a deep-water trough development on the shallow-water carbonate platform, appeared in the northern part of the basin (Figure 1C). Dark-colored argillaceous limestones were deposited in the trough, containing many nodular or bedded cherts [5,22]. In addition, massive dolomites were found in the Middle Permian successions, mostly interpreted as hydrothermal dolomites formed by the hydrothermal fluids from the activated deep faults [5,22,33].
The Middle Permian succession includes the Liangshan Formation (P2l), Qixia Formation (P2q) and Maokou Formation (P2m) in the Sichuan Basin. The Maokou Formation can be subdivided into four members from bottom to top: Mao1, Mao2, Mao3 and Mao4 (Figure 2). The Mao1 member is mainly composed of micrite and argillaceous limestone, indicating a relatively deep-water sedimentary environment, which may be related to the large transgression that occurred on the Yangtze platform in the early Maokou period. In contrast, bioclastic limestone and dolomite developed in the Mao2 member, indicating the formation of shallow shoals under high-frequency sea-level changes. The deposition of the Mao3 and Mao4 members reflects the sedimentary differentiation pattern of trough-platform facies. In the central and southern regions of the Sichuan basin, the Mao3 and Mao4 members mainly consist of dolomite and bioclastic limestone. In contrast, in the extensions of the trough, the Mao3 and Mao4 members are mainly composed of argillaceous limestone and shale, accompanied by a large number of bedded and nodular cherts [28,33]. Besides, numerous bedded and nodular cherts developed in the Mao3 and Mao4 members in the deep-water facies in the periphery of the platform (Figure 2).

3. Materials and Methods

A total of 15 chert samples and six host limestone samples of the Maokou Fm. were collected from the Changjianggou section (CJG; 32°19′25″ N, 105°27′9″ E), Maeryan section (MEY; 32°16′23″ N, 105°25′3″ E), Xibeixiang section (XBX; 32°31′35″ N, 105°44′42″ E), Sanduizhen section (SDZ; 32°28′54″ N, 105°38′23″ E), Shuanghe section (SH; 31°57′04″ N, 108°39′28″ E), Zhengyuan section (ZY; 32°22′44″ N, 106°18′39″ E), Xiaoyan section (XY; 29°28′11″ N, 107°55′26″ E) and Erya section (EY; 30°32′42″ N, 106°49′17″) (Figure 1C). Detailed petrographic studies on 40 thin sections were carried out at the School of Earth and Space Sciences, Peking University. The thin sections were stained with Alizarin Red S to identify silica from calcite. Afterward, the chert and limestone samples were conducted with an FEI- QUANTA650FEG scanning electron microscope (SEM) with a working current of 10 kV and a distance of 11.4 mm at the Peking University’s Key Laboratory of Orogenic Belts and Crustal Evolution (OBCE). After selecting and washing the samples, they were crushed to powders by an agate mortar and pestle to below 200 mesh for geochemical analyses.
The major and trace elements were analyzed at the OBCE at Peking University. The samples were microfragmented by a dental drill to eliminate the interference of veins or other minerals and were screened by a 200-mesh sieve. For the analysis of major elements, 2 g sample powders and lithium tetraborate were mixed into a fused glass with a ratio of 1:8. Then the fused glass was measured by a Thermo Arl Advant’XP X-ray fluorescence spectrometry (XRF). The accuracy and precision of the data were better than 2.5%.
The analysis of trace and rare earth elements required 0.5 mL concentrated HNO3 to dissolve and then dry the 50 mg sample powders. The dried sample was dissolved in 5 mL of HNO3 with a concentration of 1.42 g/mL and was heated for 3 h (at 130 °C). Then, the heated solution was diluted to 60 mL by adding ultra-pure H2O for trace element testing. The contents of trace and rare earth elements were determined by using an inductively coupled plasma mass spectrometer (ICP-MS, Agilent 7500, USA). For the standardization of REE data, we used the data of Post-Archean Average Shale (PAAS). The anomalies of Eu and Ce were calculated by the following formulas: Ce/Ce* = CeSN/(0.5LaSN + 0.5PrSN) and Eu/Eu* = EuSN/(0.67SmSN + 0.33TbSN) [39].
The Si isotope analyses were carried out at the Institute of Mineral Resources, Chinese Academy of Geological Sciences. Chert samples were dissolved with HCl at 500 °C to remove other components of the sample, such as carbonate or organic components. Afterward, SiF4 was formed in a metallic vacuum line by reacting with BrF5. Then, we purified the obtained SiF4 gas by using a Cu tube with Zn particles at 60 °C. Finally, the ratios of the Si isotope were tested by a MAT-253 gas source isotopic mass spectrometer. According to the NBS-28 reference material, the silicon isotopic compositions were recorded as δ30Si (Rsam = the value of the sample, Rstd = the value of the reference material):
δ X S i = ( R s a m R s t d − 1 )   ( i n   p e r m i l )
GBW04421 and GBW04422 were used as two standard materials to be tested together with the samples and the secondary standard samples (AGV-2, andesite) in the experiment, which both had better long-term reproducibility than ±0.1‰(2σ) [40,41,42].

4. Results

4.1. Petrography of Cherts

The Maokou cherts hosted within limestones display uneven thickness (Figure 3A–I). The most common types of cherts are nodular and bedded cherts (Figure 3). Bedded cherts are mainly developed in the Erya (EY), Luomuhe (LMH), Lengshuixi (LSX), Shuanghe (SH), Xibeixiang (XBX) and Zhengyuan (ZY) sections (Figure 3A,B,D), which are interbedded with micrite limestone (Figure 3A,B) or argillaceous limestone layers (Figure 3D). The bedded cherts are composed of microcrystalline quartz and abundant siliceous organism fragments, including spicules, radiolarians and ostracods (Figure 4E and Figure 5B). The structures of skeletal grains (e.g., spicules, radiolarians) were legible and preserved perfectly (Figure 5C,D).
Nodular cherts are mainly found in Maerya (MEY) and Xiaoyan (XY) sections. Most nodular cherts show dark gray or brownish-yellow colors due to exposed weathering or oxidization (Figure 3E–I). Some calcareous gastropod and brachiopod fragments were preserved in the nodular cherts and were partially silicified (Figure 3C,E). The calcareous dolomites appeared to be close to the nodular cherts that were wrapped by host micrite limestone in the Maokou Fm. (Figure 3F). At the MEY section, fusulinids and other bioclasts were partially silicified near the boundary between the chert and host limestone (Figure 4D). In addition, many small rhombic dolomite grains were found in the host limestone near the nodular cherts at Maokou Fm. (Figure 4A). SEM observation shows that calcareous organisms (foraminifera, etc.) were replaced by fine-grained quartz aggregates in the host limestone (Figure 5A). The microcrystalline quartz was recrystallized to medium size (Figure 5E). Clean precipitated quartz appears in the dolomite of Maokou Fm. in the Xinjigu (XJG) section (Figure 5F).

4.2. Geochemistry

4.2.1. Major and Trace Elements

The SiO2 contents of the bedded cherts in the Maokou Fm. span from 77.96% to 93.30% (average 87.12%) (Table 1). The Fe2O3 concentrations of the bedded cherts range from 0.04% to 0.48% (average 0.19%), and Al2O3 content ranges from 0.05% to 0.32% (average 0.27%). The contents of TiO2 are relatively low, varying from 0.002% to 0.023% (average 0.009%). The SiO2 concentrations of the nodular cherts range from 74.89% to 97.30% (average 88.41%), which are similar to those of bedded cherts. The range of Fe2O3 and Al2O3 content of the nodular cherts are from 0.02% to 1.54% (average 0.0.74%) and 0.06% to 1.19% (average 0.35%), respectively. The TiO2 contents of the nodular cherts are slightly higher than those of the bedded cherts, varying from 0.010% to 0.055% (average 0.025%).
The Mn concentrations of the bedded and nodular cherts in the Maokou Fm. range from 3.9 to 85.4 ppm (average 36.3 ppm) and from 19.7 to 1201 ppm (average 588.4 ppm). The Co contents of the bedded cherts range from 0.2 to 396.6 ppm (average 119.0 ppm), which are much higher than those of the nodular cherts with a range of 0.092 to 2.165 ppm (average 0.884 ppm) (Table 2). The range of the Cd contents of the bedded and nodular cherts are 0.038 to 5.908 ppm (average 1.374 ppm) and 0.027 to 0.119 ppm (average 0.074 ppm). The Mo contents of the bedded cherts (0.004 to 0.024 ppm; average 0.011 ppm) are lower than those of the nodular cherts (1.80 to 0.024 ppm; average 5.110 ppm).

4.2.2. Rare Earth Elements

The total rare earth elements (REEs) concentration of nodular cherts ranges from 0.38 to 8.33 ppm (average 2.70 ppm), and the total contents of REEs of bedded cherts range from 0.53 to 17.14 ppm (average 5.51 ppm) (Table 3). The PAAS-normalized REEs of the Maokou cherts and limestone show a flat REE pattern (Figure 8). All chert samples in the Maokou Fm. display slightly negative Ce/Ce* values ranging from 0.88 to 0.99 (average 0.95), similar to those of Maokou limestones (0.94 to 0.99, average 0.97). The Eu/Eu* values of the nodular chert samples exhibit high positive Eu/Eu* values ranging from 1.66 to 9.43 (average 5.38), whereas the Eu/Eu* values of the bedded chert samples exhibit slightly positive or negative values ranging from 0.95 to 2.73 (average 1.40). The Eu/Eu* values of the limestone samples exhibit slightly negative anomalies, ranging from 0.81 to 1.00 (average 0.91).

4.2.3. Stable Silicon Isotope Compositions

Nine bedded chert samples from four sections (EY, LSX, SH and ZY) were analyzed for silicon isotopes. The δ30Si values of the samples of the EY section are 1.1‰, 1.2‰ and 1.4‰, with an average value of 1.2‰. The δ30Si values of the two samples from the LSX section are 1.3‰ and 0.7‰ (Table 2). The δ30Si values of the two samples from the SH section are 0.2‰ and 1.1‰. The δ30Si values of the two samples from the ZY section are 0.6‰ and 1.1‰. The average δ30Si value of the bedded chert samples is 0.91‰ (Table 2), which is similar to that of the bedded cherts samples from the LSX section (average 0.77‰) [43]. The δ30Si values of the 14 chert samples from the ELB section are lower than those of the bedded cherts, ranging from −0.4‰ to 0.7‰ (average 0.14‰) [22].

5. Discussion

5.1. Origin of the Bedded Cherts

The petrographic and geochemical evidences indicate that the bedded cherts of the Maokou Fm. mainly originate from biological processes. The lamination of the bedded cherts suggests a continued depositional process of siliceous materials. Furthermore, the bedded cherts contain numerous siliceous fossil debris, including ostracodes, spicules and radiolarians (Figure 4E and Figure 5C,D), indicating a sedimentary accumulation of silica-secreting organisms, typically in the deep-water environment.
All the bedded chert samples were plotted in the biogenic-dominated zone in the Al-Fe-Mn ternary diagram, which also supported the biogenic origin of bedded cherts (Figure 6). The recorded depletion in Fe and Mn concentrations suggests that there are few significant signals of hydrothermal fluids [1,17,44]. In addition, the average values of Al/(Al + Fe + Mn) of the bedded cherts (0.56) are similar to the published values of biogenic cherts (ca. 0.6) [17,45]. The Si isotope compositions of bedded cherts also indicate that the siliceous materials originated from silica-secreting organisms in seawater. The silicon isotope fractionation is determined by the biological activity, precipitation rate, composition and temperature of the environmental solution during the inorganic precipitation of the dissolved silica [46,47,48,49,50]. The activities of radiolarians and sponges in shallow seas could preferentially remove δ28Si, leading to the enrichment of δ30Si in the seawater [22,51]. Therefore, the high δ30Si values of Maokou bedded cherts (average 0.91‰), similar to those reported for seawater-derived cherts (average 0.77‰) [43], also suggest that the origin of the bedded cherts is mainly from silica-secreting organisms in seawater.
The bedded cherts were mostly formed in a deep-water environment (e.g., troughs, slopes and basins) as suggested by the Fe2O3/TiO2 vs. Al2O3/(Al2O3 + Fe2O3) diagram (Figure 7), in which the bedded chert samples are plotted in the continental margin to pelagic fields [52]. Correspondingly, the location of the sections of these samples can also reflect the deep-water depositional environment (Figure 1B). Additionally, the flat REE patterns of bedded cherts (Table 3, Figure 8A) are comparable with those of limestone samples, suggesting that bedded cherts were formed in a seawater environment. However, the Eu/Eu* values of some bedded chert samples (e.g., LSX-1 and SH-3) display relatively high values (to a maximum of 2.7) in the SH and LSX sections, namely positive Eu anomalies, implying some degrees of hydrothermal influence. This is because Eu can be removed from other REEs by reducing from Eu3+ to Eu2+ under high temperature (especially >250 °C) and reducing conditions, leading to an increase of Eu in the sediments [53,54,55]. Therefore, we conclude that, although the bedded cherts largely originated from biological processes, the formation of some bedded cherts was influenced by hydrothermal activities.

5.2. Origin of Nodular Cherts

The nodular cherts from the Maokou Fm. are thought to be formed by hydrothermal effects, as evidenced by the petrographic and geochemical characteristics. The irregular non-stratified occurrence of nodular cherts in MEY and XY sections (Figure 1 and Figure 3G–I) suggests a diagenetic process rather than a depositional process. The almost totally silicification of the calcareous bioclasts in the nodular cherts, with well-preserved ghost outlines (Figure 4D and Figure 5A), indicates rapid metasomatism by Si-enriched diagenetic fluids, transferring from calcite to siliceous minerals [5]. In addition, the direct precipitation of hydrothermal silica was found in the XJG section near the basement deep fracture, which further explains the hydrothermal source of siliceous materials (Figure 4F). The nodular cherts are all located in the hydrothermal-dominated zone (Figure 6), suggesting a hydrothermal origin [1,17], which is consistent with the results that the average Al/(Al + Fe + Mn) ratios (~0.15) of nodular chert samples are comparable with the reported values of hydrothermal cherts (~0.1) [17,45]. Moreover, the obvious positive Eu anomalies, with a maximum value of 9.43, further confirm that the nodular cherts were formed under the influence of the hydrothermal fluids or by the rapid process of siliceous metasomatism by hydrothermal fluids [53,54,55]. Additionally, the formation of dolomite particles in the host limestone near the nodular cherts may be related to the same hydrothermal activity (Figure 4A). Thus, we conclude that the hydrothermal activities were the main triggering factor for the formation of the Maokou nodular cherts.
Si isotopes can further confirm that the hydrothermal fluids have influenced the formation of the nodular cherts (Figure 9). The δ30Si values of the nodular chert samples from the Erlangba (ELB) section (average 0.14‰) are significantly lower than those of the bedded cherts samples (average 0.79‰) [22], suggesting hydrothermal siginals. The low δ30Si values might be caused by the rapid precipitation of the supersaturated dissolved silica in the hydrothermal fluids, as it forms an amorphous siliceous gel once cooled. A massive amount of silicon isotope fractionation of △30Si (solid-aqueous) yields during this process [40,49]. Therefore, cherts of hydrothermal origin usually have a low δ30Si value, which is consistent with the suggestion stated above.
As shown in Figure 7, all the nodular chert samples fall into the “ridge” zone in the Fe2O3/TiO2 vs. Al2O3/(Al2O3 + Fe2O3) diagram [52], which is in agreement with the facts that the paleogeographic locations of the MEY and XY sections are adjacent to the active deep faults that have experienced significant hydrothermal activity (Figure 1C). These deep faults were activated because of the intense tectonic movements related to the ELIP during the late Guadalupian [29,56], accompanying massive hydrothermal fluids venting into the shallow-buried carbonate stratum or deep ocean seafloor. Therefore, the nodular cherts were formed by siliceous precipitation via cooling of the Si-enriched hydrothermal fluids or by the rapid hydrothermal metasomatism of the host carbonate rocks.

5.3. The Formation Mechanism of the Maokou Cherts

As noted above, the nodular cherts were mainly formed under the influence of hydrothermal fluids, and the bedded cherts originated from the biological processes with some extent of hydrothermal effects. Thus, we believe that the bedded and nodular cherts may share the same source, which is associated with the hydrothermal activities related to the ELIP events. The sedimentary environment was the main factor that led to the different occurrences of Maokou cherts. The nodular cherts occurred in the shallow-water carbonate platform and the bedded cherts occurred in the deep-water environments (e.g., trough, slope and shelf).
Despite the bedded cherts being significantly characterized by signals of biogenetic origins, some geochemical evidence (e.g., Eu anomalies) shows the effects of hydrothermal fluids. The bedded chert samples are all plotted in the upwelling zone of the Co × Mn vs. Cd/Mo diagram (Figure 10). This is because the sediments of upwellings are generally featured by high Cd/Mo values and low Co × Mn values [57,58]. The high primary productivity of upwellings leads to an increase in Cd contents through the flourishing of Cd-rich plankton, in contrast to the constant contents of the less bio-sensitive Mo elements [59]. Alternatively, the low contents of Co and Mn are attributed to their decrease in the oxygenated upwellings [60]. In contrast, the nodular chert samples fall outside the upwelling zones (Figure 10), which also indicates that the formation of nodular cherts did not occur in a deep-water environment and was directly associated with the hydrothermal fluids which carried high Mn contents.
The upwellings in the Upper Yangtze Block was caused by the venting of high-temperature hydrothermal fluids from deep faults during Guadalupian [5], which is entirely different from the upwellings caused by the melting of polar glaciers on the northwestern edge of Pangea during the Mid-Late Permian [7,8]. The activity of ELIP triggered strong tectonic movements, which led to the activation of deep faults and the overflow of hydrothermal fluids. The hydrothermal fluids were the results of the mixing of magmatic-derived fluids and modified seawater. Due to the high temperature of the hydrothermal fluids from under the seafloor, the cold bottom seawater was heated to reduce its density and went upward to form upwellings, namely volcanogenic upwellings [61,62,63]. The upwellings carried a large number of nutrients (including N, P, Ba and H4SiO4), which could promote the proliferation of siliceous organisms. These biologically sourced silica settled on the bottom of the seawater with the death of organisms, so bedded cherts were formed in deep water environments such as troughs [64,65,66] (Figure 11). In addition, the silicon-rich seawater could pour into the shallow-buried Maokou carbonate strata adjected to the deep-water area due to the power from the upwellings. Silicon-rich fluids tend to first metasomatize the argillaceous components of the carbonate rocks to form a siliceous nucleus, and then they grow into siliceous rocks under specific conditions [5,22] (Figure 11). The nucleation and growth of the siliceous rocks were accelerated when they were directly affected or heated by the hydrothermal fluid, forming large nodular or striped cherts. This process mainly occurred in the sedimentary environment of shallow-water carbonate platform, resulting in the facts that nodular cherts mainly distributed in shallower-water platform sediments (Figure 11).
Therefore, we believe that the bedded cherts of the Maokou Formation were formed by biological process caused by the upwelling related to tectonic–hydrothermal activities. Some of the nodular cherts might be directly metasomatized by hydrothermal fluids, and the others may have been the results of the water–rock reaction by the silicon-rich fluid in the strata, which had a similar siliceous source to the bedded chert.

6. Conclusions

In this study, the petrographic and geochemical data of cherts samples from six outcrop sections were presented to study the genesis of different types of cherts in the Maokou Formation in the Sichuan Basin.
The Maokou cherts occurred in nodular and bedded forms. The bedded cherts were mainly formed in a deep-water environment and are mainly formed by the biogenetic processes related to volcanogenic upwellings. Some bedded chert samples near the basement fractures show weak hydrothermal characteristics evidenced from geochemical data, suggesting that they were affected by the hydrothermal fluids. Nodular cherts commonly have characteristics of hydrothermal origins. Some nodular cherts were formed through direct hydrothermal metasomatism, and others formed from a similar siliceous source to bedded cherts that were affected by the hydrothermal fluids to a larger degree. To summarize, both the bedded and nodular Maokou cherts were influenced by hydrothermal activities, and both had a strong relationship with the tectonic movements and eruptions of the ELIP events.

Author Contributions

Conceptualization, H.Z.; methodology, H.T.; investigation, H.Z. and J.W.; resources, X.Y.; data curation, K.S.; writing—original draft preparation, H.Z.; writing—review and editing, Y.D.; supervision, B.L. and Y.D.; funding acquisition, K.L. and Q.Q. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the National Natural Science Foundation of China, grant number U19B6003 and the Wuxi Research Institute of Petroleum Geology, SINPEC, grant number 33550007-19-ZC0613-0085.

Acknowledgments

Thanks to Hangyu Liu, Xuefeng Zhang and Yuanchong Wang from Peking University for their help in writing this article.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. (A) Middle Permian (~255.7 Ma) global paleogeography and the location of Sichuan Basin, South China [34]. (B) Middle Permian paleogeography of the Upper Yangtze Block [22,35,36] and the location of the Sichuan Basin. (C) Maokou paleogeography of Sichuan Basin (basement faults from [37]). XY: Xiaoyan, EY: Erya, SH: Shuanghe, XBX: Xibeixiang, SDZ: Sanduizhen, ZY: Zhengyuan, LSX: Lengshuixi, XJG: Xinjigu; MEY: Maeryan.
Figure 1. (A) Middle Permian (~255.7 Ma) global paleogeography and the location of Sichuan Basin, South China [34]. (B) Middle Permian paleogeography of the Upper Yangtze Block [22,35,36] and the location of the Sichuan Basin. (C) Maokou paleogeography of Sichuan Basin (basement faults from [37]). XY: Xiaoyan, EY: Erya, SH: Shuanghe, XBX: Xibeixiang, SDZ: Sanduizhen, ZY: Zhengyuan, LSX: Lengshuixi, XJG: Xinjigu; MEY: Maeryan.
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Figure 2. The comprehensive stratigraphic column of the Middle Permian in the Sichuan Basin (modified from [38]).
Figure 2. The comprehensive stratigraphic column of the Middle Permian in the Sichuan Basin (modified from [38]).
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Figure 3. Photos of different outcrops showing bedded and nodular cherts of the Maokou Formation. (A) Bedded cherts at SH section; (B) bedded cherts at SH section; (C) nodular chert (length = 12 cm; height = 3 cm) is wrapped by host limestones at MEY section. A gastropod fragment is well preserved; (D) bedded cherts are interbedded with the argillaceous limestone at EY section; (E) nodular chert (L = 18 cm; H = 9 cm) is wrapped by limestone at LSX section. A calcareous brachiopod fragment is preserved; (F) nodular chert and calcareous dolomite are wrapped by host micrite limestone, MEY section; (G–I) nodular cherts show different sizes in the thick micrite–bioclastic limestone at the MEY section.
Figure 3. Photos of different outcrops showing bedded and nodular cherts of the Maokou Formation. (A) Bedded cherts at SH section; (B) bedded cherts at SH section; (C) nodular chert (length = 12 cm; height = 3 cm) is wrapped by host limestones at MEY section. A gastropod fragment is well preserved; (D) bedded cherts are interbedded with the argillaceous limestone at EY section; (E) nodular chert (L = 18 cm; H = 9 cm) is wrapped by limestone at LSX section. A calcareous brachiopod fragment is preserved; (F) nodular chert and calcareous dolomite are wrapped by host micrite limestone, MEY section; (G–I) nodular cherts show different sizes in the thick micrite–bioclastic limestone at the MEY section.
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Figure 4. Microscope photos show the characteristics of the Maokou cherts. (A) Dolomites in the silicified limestone, MEY section; (B) bioclasts are silicified into fine to medium crystalline quartz in the host limestone, MEY section; (C) silica recrystallization is found in microfracture, MEY section; (D) boundary between chert and host limestone, fusulinids and other bioclasts were partially silicified into microquartz, MEY section; (E) bedded chert contains a large number of siliceous organisms, including spicules, ostracodes and radiolarians, SH section; (F) precipitated quartz appears in the intergranular pores of dolomites, XJG section.
Figure 4. Microscope photos show the characteristics of the Maokou cherts. (A) Dolomites in the silicified limestone, MEY section; (B) bioclasts are silicified into fine to medium crystalline quartz in the host limestone, MEY section; (C) silica recrystallization is found in microfracture, MEY section; (D) boundary between chert and host limestone, fusulinids and other bioclasts were partially silicified into microquartz, MEY section; (E) bedded chert contains a large number of siliceous organisms, including spicules, ostracodes and radiolarians, SH section; (F) precipitated quartz appears in the intergranular pores of dolomites, XJG section.
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Figure 5. SEM photographs of studied Maokou cherts and host limestones. (A) Bioclasts were silicified into quartz in the host limestone, MEY section; (B) bedded chert composed of microquartz, EY section; (C) abundant sponge spicules (yellow arrows) in bedded chert, SH section; (D) radiolarians in bedded chert occurred as microquartz, LSX section; (E) silica recrystallization to medium crystalline quartz close to the microquartz, MEY section; (F) ghost dolomite in nodular chert, MEY section; (G) sepiolite occurs within intergranular pores of a calcitic nodular chert, MEY section; (H) calcite filled a microfracture in nodular chert, MEY section; (I) hematite in the nodular chert, MEY section.
Figure 5. SEM photographs of studied Maokou cherts and host limestones. (A) Bioclasts were silicified into quartz in the host limestone, MEY section; (B) bedded chert composed of microquartz, EY section; (C) abundant sponge spicules (yellow arrows) in bedded chert, SH section; (D) radiolarians in bedded chert occurred as microquartz, LSX section; (E) silica recrystallization to medium crystalline quartz close to the microquartz, MEY section; (F) ghost dolomite in nodular chert, MEY section; (G) sepiolite occurs within intergranular pores of a calcitic nodular chert, MEY section; (H) calcite filled a microfracture in nodular chert, MEY section; (I) hematite in the nodular chert, MEY section.
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Figure 6. The ternary diagram of Al–Fe–Mn of the Maokou cherts in the Sichuan Basin. The hydrothermal- and biogenetic-dominated distribution zones are according to Adachi et al. [1].
Figure 6. The ternary diagram of Al–Fe–Mn of the Maokou cherts in the Sichuan Basin. The hydrothermal- and biogenetic-dominated distribution zones are according to Adachi et al. [1].
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Figure 7. Fe2O3/TiO2 versus Al2O3/(Al2O3 + Fe2O3) diagram for the Maokou cherts in the Sichuan Basin.
Figure 7. Fe2O3/TiO2 versus Al2O3/(Al2O3 + Fe2O3) diagram for the Maokou cherts in the Sichuan Basin.
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Figure 8. PAAS-normalized REE patterns of cherts and limestones. (A) Bedded cherts of Maokou Fm.; (B) nodular cherts of Maokou Fm.; (C) limestones of Maokou Fm.
Figure 8. PAAS-normalized REE patterns of cherts and limestones. (A) Bedded cherts of Maokou Fm.; (B) nodular cherts of Maokou Fm.; (C) limestones of Maokou Fm.
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Figure 9. Correlation of δ30Si and Al2O3 concentrations of the Maokou cherts (data of ELB cherts from [22]; data of LSX cherts from [43]).
Figure 9. Correlation of δ30Si and Al2O3 concentrations of the Maokou cherts (data of ELB cherts from [22]; data of LSX cherts from [43]).
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Figure 10. Co*Mn versus Cd/Mo diagram for the Maokou cherts to identify upwelling settings.
Figure 10. Co*Mn versus Cd/Mo diagram for the Maokou cherts to identify upwelling settings.
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Figure 11. Conceptual models showing the formation mechanism of the Maokou cherts in the Sichuan Basin (the position of the cross-section is shown in Figure 1C). The bedded cherts of biological origin are mainly distributed in the deep-water environment, whereas the nodular cherts are mainly distributed in the shallow water platform environment.
Figure 11. Conceptual models showing the formation mechanism of the Maokou cherts in the Sichuan Basin (the position of the cross-section is shown in Figure 1C). The bedded cherts of biological origin are mainly distributed in the deep-water environment, whereas the nodular cherts are mainly distributed in the shallow water platform environment.
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Table
Table 1. Major elements of the Maokou cherts and limestones in the Sichuan Basin.
Table 1. Major elements of the Maokou cherts and limestones in the Sichuan Basin.
SampleOccurrenceSiO2 (wt%)Al2O3 (wt%)TFe2O3 (wt%)CaO (wt%)MgO (wt%)K2O (wt%)Na2O (wt%)MnO (wt%)TiO2 %P2O5 (wt%)
EY-1bedded81.5980.2560.1179.2781.9460.0250.0230.0040.0060.010
EY-2bedded82.360.40.489.50.080.120.030.010.020.01
EY-4bedded89.670.310.065.280.120.060.0600.010.02
LSX-4bedded//////////
LSX-5bedded//////////
LSX-1bedded77.960.10.1811.51.210.030.06000.02
SH-1bedded82.680.320.226.872.190.050.030.010.010.01
SH-3bedded92.730.120.043.360.10.030.0300.010
XBX-1bedded91.40.480.281.280.150.090.0400.020.06
ZY-1bedded92.40.150.164.010.030.020.03000.02
ZY-2bedded93.30.310.181.840.120.060.030.010.010.11
CJG-1limestone0.1150.050.0455.20.610.01/00.010
EY-3limestone0.1970.040.0355.50.340.01////
LSX-2limestone2.8990.060.0253.40.820.01/000
SDZ-1limestone0.1130.040.04560.350.01////
XY-2limestone0.3260.050.0255.40.730.01///0
ZY-3limestone0.3610.090.0554.60.950.01/00/
XY-1nodular79.491.190.266.583.30.010.0300.050.03
MET-1nodular74.890.060.212.52.610.01/0/0
MET-2nodular98.130.190.140.160.020.04/0.01/0.01
MET-3nodular87.140.191.514.751.450.04/0.180.010.01
MET-4nodular97.30.220.830.390.010.040.010.080.010.03
MET-5nodular89.550.280.812.20.140.040.060.070.030.01
Table
Table 2. Trace elements and stable silicon isotope compositions of the Maokou cherts and limestones in the Sichuan Basin.
Table 2. Trace elements and stable silicon isotope compositions of the Maokou cherts and limestones in the Sichuan Basin.
SampleOccurrenceCd(ppm)Mo(ppm)Mn(ppm)Co(ppm)δ30SiNBS-28‰
EY-1bedded0.0380.00436.2440.1771.1
EY-2bedded0.10.0346.631731.1
EY-4bedded////1.4
LSX-4bedded////1.3
LSX-5bedded////0.7
LSX-1bedded0.140.0115.01297/
SH-1bedded0.97074.560.690.2
SH-3bedded0.070.0215.183971.1
XBX-1bedded5.910.0113.830.42/
ZY-1bedded0.040.013.941830.7
ZY-2bedded3.730.0185.380.510.6
CJG-1limestone0.260.0135.90.52/
EY-3limestone0.10.016.3530.71/
LSX-2limestone0.1109.2630.62/
SDZ-1limestone0.150.016.4166.63/
XY-2limestone0.1706.9280.59/
ZY-3limestone0.290.0111.330.66/
XY-1nodular0.230.5216.5428.7/
MET-1nodular0.121.819.70.33/
MET-2nodular0.031.8634.590.09/
MET-3nodular0.063.412010.71/
MET-4nodular0.063.97653.51.12/
MET-5nodular/////
MET-6nodular0.1045.1101033.1662.165/
Table
Table 3. REE analysis results of the Maokou cherts and limestones in the Sichuan Basin (ppm).
Table 3. REE analysis results of the Maokou cherts and limestones in the Sichuan Basin (ppm).
SampleOccurrenceLaCePrNdSmEuGdTbDyHoErTmYbLuΣREECe/Ce*Eu/Eu*
EY-2bedded0.4910.8980.1140.4140.0910.0220.0850.0130.0820.0170.0500.0070.0530.0082.3470.9151.341
LSX-1bedded0.0820.1700.0220.0870.0230.0120.0220.0040.0210.0040.0120.0020.0120.0020.4740.9692.729
SH-1bedded2.6104.0000.3981.5510.3610.0620.3240.0470.2740.0570.1520.0210.1220.0119.9890.9270.965
SH-2bedded0.4350.6940.0820.2900.0640.0150.0600.0100.0640.0140.0380.0050.0350.0051.8110.8811.289
SH-3bedded0.0990.1930.0260.1010.0270.0080.0240.0040.0200.0040.0100.0020.0110.0020.5290.9241.614
XBX-1bedded4.0477.0570.7042.4890.6050.1060.5630.0850.5200.1150.3440.0490.3290.12917.1430.9980.974
ZY-1bedded0.0690.1310.0160.0640.0150.0030.0130.0020.0130.0030.0070.0010.0070.0010.3440.9531.314
ZY-2bedded2.7784.5030.4621.7920.4510.0780.4450.0640.3590.0750.2000.0290.1770.05511.4690.9470.946
CJG-1limestone0.3750.7260.0820.2930.0680.0110.0580.0090.0530.0100.0280.0040.0230.0031.7451.0000.939
EY-3limestone0.3210.5890.0660.2210.0490.0080.0410.0060.0400.0090.0260.0040.0270.0041.4110.9770.923
LSX-2limestone0.1770.3320.0390.1470.0350.0060.0320.0060.0380.0090.0270.0040.0310.0040.8860.9621.006
SDZ-1limestone0.4140.7750.0950.3430.0820.0130.0720.0100.0580.0120.0330.0050.0330.0051.9510.9420.922
XY-2limestone0.1170.2210.0280.1050.0250.0040.0230.0040.0240.0060.0170.0030.0200.0060.6030.9370.807
ZY-3limestone0.2820.5950.0760.2620.0550.0080.0440.0070.0400.0080.0250.0040.0270.0061.4400.9770.857
MET-2nodular0.0810.1450.0170.0640.0160.0250.0120.0020.0090.0020.0050.0010.0050.0010.3850.9419.433
MET-3nodular0.1350.3040.0410.1600.0420.0420.0400.0060.0370.0070.0200.0030.0200.0030.8620.9795.471
MET-4nodular0.2250.4570.0570.2210.0580.0520.0540.0080.0410.0070.0160.0020.0140.0021.2130.9704.945
MET-6nodular1.6783.1510.3601.4140.3610.1100.3530.0560.3410.0700.1930.0290.1880.0298.3330.9761.660
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Zheng, H.; Wu, J.; Tang, H.; Liu, B.; Yang, X.; Shi, K.; Luo, K.; Qiu, Q.; Dong, Y. Origin of the Multiple-Sourced Cherts in Maokou Carbonates in Sichuan Basin, South China. Minerals 2021, 11, 1269. https://doi.org/10.3390/min11111269

AMA Style

Zheng H, Wu J, Tang H, Liu B, Yang X, Shi K, Luo K, Qiu Q, Dong Y. Origin of the Multiple-Sourced Cherts in Maokou Carbonates in Sichuan Basin, South China. Minerals. 2021; 11(11):1269. https://doi.org/10.3390/min11111269

Chicago/Turabian Style

Zheng, Haofu, Junfeng Wu, Hailei Tang, Bo Liu, Xiangyang Yang, Kaibo Shi, Kaiping Luo, Qi Qiu, and Yixin Dong. 2021. "Origin of the Multiple-Sourced Cherts in Maokou Carbonates in Sichuan Basin, South China" Minerals 11, no. 11: 1269. https://doi.org/10.3390/min11111269

APA Style

Zheng, H., Wu, J., Tang, H., Liu, B., Yang, X., Shi, K., Luo, K., Qiu, Q., & Dong, Y. (2021). Origin of the Multiple-Sourced Cherts in Maokou Carbonates in Sichuan Basin, South China. Minerals, 11(11), 1269. https://doi.org/10.3390/min11111269

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