Figure
1.
Sketch of the study area.
| Citation: | Zhongyang Chen, Peep Männik, Junxuan Fan, Chengyuan Wang, Qing Chen, Zongyuan Sun, Dongyang Chen, Chao Li. Age of the Silurian Lower Red Beds in South China: Stratigraphical Evidence from the Sanbaiti Section. Journal of Earth Science, 2021, 32(3): 524-533. doi: 10.1007/s12583-020-1350-6
|
The concept of using microorganisms as a tool for mineral exploration was proposed almost 50 years ago (Slavnina, 1957). Two decades later, Watterson et al.(1985, 1983a, b) reported on a relationship between spore counts of Bacillus spp. (almost exclusively B. cereus) and heavy metal anomalies in soils over ore deposits. These findings suggested the possibility of using B. cereus as an index to underlying metal mineralization. Field studies were carried out in several locations of different climate conditions (Parduhn, 1991) and results were promising, especially in semiarid areas. Further application research on the bioexploration method was carried out in several countries including Belgium, Burkina Faso, France, Mexico and Sudan (Melchior et al., 1996, 1994; Melchior, 1993; Moureau et al., 1991; Neybergh et al., 1991, 1989). Based on the previous literature, it is hypothesized in this study that there is a common spatial association between B. cereus spore count and soil gold content in spite of the differences in the climate, geological setting and mineralizations. In China, research of microbial bioexploration is still in its infancy (Wang et al., 1999; Xie et al., 1997; Li et al., 1994). The purpose of this study is to screen soil samples at three mine sites located on the same tectonic crustal block (the Aba crustal block) in an effort to seek association between B. cereus spore counts and gold content as a prelude to developing a bioexploration index. This method has been tested in the gold deposits of Axi, Manaoke and Dongbeizhai, northwestern Sichuan Province of China (Fig. 1).
The sampling region is a typical canyon with elevations ranging from 1 800 to 4 300 m, located in the northeast of the Qinghai-Tibet plateau.A continental temperate altiplano climate prevailsin the region with an annual mean rainfall of 600-700 mm.The annual av-erage temperature increases gradually from Axi (0-3℃) to Manaoke (3-6℃) and to Dongbeizhai (5.7℃).Specifically, Axi has a sub-humid sub-frigid altiplano climate, while Dongbeizhai and Manaoke have a sub-humid temperate altiplano climate.The vegetation changes from mountainous boskage meadow in Axi to mountainous taiga in Dongbeizhai.
Slightly alkaline drab soil and brown soil developed in Dongbeizhai, while Axi is characterized by subacidity-neutral sub-alpine meadow soil (Zhang et al., 1997). The altitude of Manaoke is over 1 000 m higher than that of Dongbeizhai, which leads to the differences in climate and vegetation. The soil in the Manaoke gold deposit bears a mixed character of the soils developed in Dongbeizhai and Axi. Thus, the soil in Manaoke can be regarded as the transition of the two typical agro types, the drab/brown soil and sub-alpine meadow soil.
Geotectonically, the study area (the Aba crustal block) is in the triangle region bordered by the Yangtze platform, Yushu-Jinshajiang fold belt, and southern Qinling fold belt (Fig. 2). The crustal block has been characterized by active metamorphism, volcanism, magmatism and metallogenesis. Most of the discovered gold deposits developed in large-scale, regional deep-fracture zones along the boundary of the block in northwestern Sichuan. The host strata for these gold deposits vary from Cambrian, Silurian and Devonian to Triassic. However, 80 % of the gold deposits occurred in the Triassic, especially in the turbidite of Middle to Late Triassic (Yang et al., 1999).
The Manaoke gold deposit is hosted in the turbiditic sandstones and slates of Late Triassic.Gold mineralization occurs in strongly altered structural brecciasand hydrothermal quartz veins along an NW-SE trending reverse fault fracture system, dipping NW, paralleling to the strike of the stratigraphic bedding.The quartz veins and structural breccias are characterized by abundance of Au-bearing sulfides including pyrite, arsenopyrite and realgar.The individual lode extends several hundred meters in length and the thickness varies from several to tens of centimeters.The gangue minerals are quartz and calcite.The hydrothermal alteration is defined by silicification, carbonatization, pyritization and weathering by limonitization.For the detailed geology of the mineral deposit, refer to Lü et al. (1999), Wang and Fu (1999), Wang et al. (1999) and Zhang (1999).
The potential ore-bearing structures of the Axi gold deposit consist of crushed fracture systems in the exomorphic zone of Yanshanian diorite where skarn and metasomatic mineralization occur (Liao et al., 1999). The presence of intrusive rocks distinguishes the Axi gold deposit from the other two studied herein. Au mineralization is spatially related with the lithological contact between sedimentary rocks and dioritic intrusives. Gold is mainly hosted in pyrite, and the gangue minerals are quartz and calcite.
The Dongbeizhai disseminated gold deposit is one of the largest deposits in northwestern Sichuan. Gold is mostly found in pyrite, which is the most abundant sulfide; however, native gold, arsenic sulfides and antimonite also occur. The primary geochemical signature is defined by an assemblage of Au-As-S-Sb-Hg. Au-bearing sulfide lodes are closely associated with carbonaceous slates and phyllites in the Xinduqiao Formation of the Upper Triassic (Yin et al., 1999; Zhou et al., 1995; Zheng, 1989) and are generally confined to the clastic footwall block of a north-south trending fault (within a distance of 0-60 m from the fault), which is parallel to the strike of the stratigraphic bedding. The mineralization zone extends 4 km in length while the width of the Au-bearing sulfide veins can reach up to 4 m. Quartz and calcite are the gangue minerals. Hydrothermal alteration is characterized by strong silicification, pyritization, carbonatization and weak argillization.
Soil samples from five transects perpendicular to the strike of the orebodies were collected for microbiological and elemental analyses at 5 m intervals and at every 2.5 m when close to the zones of gold mineralization. All samples were collected in July.
Samples were taken at the depth of 10-25 cm in the horizon B of soil profiles to avoid surface contamination. Scoop used was ethanol sterilized and samples were kept in sterilized plastic bags to prevent the loss of moisture during the transportation. After air-drying in a super clean bench, which was sterilized with UV light, the samples (200-300 g each) were divided into two parts. One aliquot was sieved to -40 mesh for microbiological analysis. The other was sieved to -200 mesh for the quantitative analyses of the contents for Au, Ag, Cu, Pb and Zn. The methodology for microbiological analysis was similar to that employed by Watterson (1985). Samples were heated to 90 ℃ for 60 s to inactivate all vegetative cells and cooled in tap water before aliquots of diluted samples were pour plated on egg yolk agar (EYA). The plates were incubated at 30 ℃ for 15 h. Thus spores that resisted the heat pre-treatment germinated and grew as colonies on the EYA plates. B. cereus colonies are characterized by the presence of an opaque to translucent halo because of the hydrolysis of lecithin (added as egg yolk to the medium). In the initial phase of this study, bacteria from suspected B. cereus colonies were isolated and characterized by physiological and biochemical tests to ensure proper identification based on colonial morphology (Xie et al., 1997). The detection limit was 10 CFU (colony forming units) per gram air-dried soil for bacterial analysis.
To evaluate the background of B. cereus, soil samples from no-mining areas were also analyzed. The data were pooled for each area and the threshold was defined based on the frequency histogram.
Atomic absorption spectrometry (AAS) was used for the elemental analysis of Au, Ag, Cu, Pb and Zn in the soil samples. The Au and Ag analyses were carried out by graphite furnace AAS and Cu, Pb and Zn by flame-AAS. Au was analyzed after the sample was digested in an HCl/HNO3 mixture and the interfering organic compounds were removed by extraction with methylisobutyl ketone. Aqua regia was used to dissolve Ag and a hot HCl-HNO3-HF digestion was used for Cu, Pb and Zn. The detection limits for Au and Ag are 0.5 ng/g soil and 0.01 μg/g soil, respectively, and 0.5 μg/g soil for Cu, Pb and Zn.
Two parallel soil transects, designated as M1 and M2, perpendicular to the strike of the orebodies, were sampled in the Manaoke deposit.
In total, 23 soil samples from the B horizon were collected along the M1 geological transect. As shown in Fig. 3, five orebodies (designated as O1, O2, O3, O4 and O5) have been revealed by the 205 Geological Survey Team of Sichuan Province through routine geochemical and geophysical methods on the M1 transect. Two (O2 and O3) of these orebodies were evaluated to be high-grade. Corresponding to these orebodies, four sites of elevated gold content (G1, G2, G3 and G4) were found in overlying soils of the transect. Only four gold anomalies were identified because O4 and O5 could not be differentiated on the basis of the soil gold analysis.
The counts of B. cereus spores varied greatly on this profile and were characterized by a clustering of high and low counts (Fig. 3). A threshold value of 240 CFU/g air-dried soil based on frequency histogram of B. cereus spore counts was designated to differentiate background value and anomalous counts. The highest spore counts were two orders of magnitude higher than the background value. Only three distinct anomalies of B. cereus spore counts (B1, B2 and B3) were found in the overlying soils. Low spore counts occurred not only in the soil with low gold content (northeast of the transect) but also in soils with high gold contents overlying the orebodies (at the sites of 8-13 m and 42-47 m on the transect). The three spore anomalies (B1, B2 and B3) were associated with the three high soil gold anomalies (G1, G2, G3), which corresponded to the underlying medium- to high-grade orebodies (O1, O2, O3). No anomalous spore counts were detected in the soils associated with the low-grade orebodies O4 and O5.
The highest spore anomalies B2 and B3 flanked the highest soil gold anomaly G3, which corresponded to one of the two high-grade orebodies (O3). Spore anomaly B1 flanked the soil gold anomaly G2, which corresponded to the other high-grade orebody (O2). B1 may also be associated with G1 which corresponded to the orebody of O1, but further data southwest of the transect are not available. Thus the three spore anomalies flanked the soil gold anomalies with the highest grades of underlying gold mineralization. The soils between these spore anomalies were characterized by low spore counts. Consequently, spore count anomalies were clustered in the soils corresponding to the top and bottom walls of the underlying orebodies, whereas low soil spore counts exactly overlaid the orebodies. Figure 3 also shows multi metal analyses for the soil samples, but there was no apparent association between the spore counts and the concentrations of metals.
17 soil samples from the B horizon were collected along the M2 geological transect for both bacterial and gold analyses. Only one ore body was clearly revealed by the 205 Geological Survey Team of Sichuan Province through routine geoexploration methods on the profile. Low spore counts occurred in soils where the orebody (O1) outcropped and at the southwest of the transect (Fig. 4). High spore counts (B1 and B2) were detected in soils flanking the subsurface orebody (O1). The gold content in soils was higher in the southwest transect as compared to the northeast. Only one of the high values corresponded to the subsurface orebody (Fig. 4).
The results from two soil transects in the Axi deposit are shown in Fig. 5. High spore counts of B. cereus (B1 and B2; B3 and B4) were detected in soils flanking the orebodies of O1 and O2. The highest count was 13 000 CFU/g soil, while low counts of spores were found at the northeast of the profiles and in soils, which overlaid the orebodies. The soil gold content showed similar trends with the spore counts on the transects, although the corresponding peaks were slightly shifted from each other. The spore distributions in the two profiles are similar to that seen in the profiles of the M1 and M2 in the Manaoke deposit.
Seven orebodies were discovered on the geological transect by the Geological Team of Northwestern Sichuan through routine geoexploration methods. The variation of B. cereus spore counts along the transect is shown in Fig. 6. The highest spore count was 6 500 CFU/g soil, which is two orders of magnitude higher than the counts in most samples of the profile. The two spore anomalies (B1 and B2) corresponded to the outermost edges of the cluster of orebodies. However, B2 partially overlapping an underlying orebody may indicate the combined results from the adjacent underlying orebodies. The other counts between B1 and B2 on the transect could not resolve individual orebodies because they were so thin and in very close proximity to each other. The gold contentin soil was not analyzed for this profile.
As with most geochemical exploration methods, it is useful to employ the background value and abnormal value in this study to discriminate the low counts away from and overlaying auriferous orebodies, and the relatively high spore counts flanking subsurface mineralization. The results (Table 1) show the average background spore counts of the Axi deposit was 312 CFU/g soil with a range of < 10 to 800 CFU/g soil. The background spore count of the Dongbeizhai deposit varied from < 10 to 40 CFU/g soil. The background spore counts of the Manaoke deposit varied from < 10 to 240 CFU/g soil, averaging at 53 CFU/g soil. The data may suggest some association between the background spore counts and soil types (Table 1). The meadow soil (Axi) had the highest average background values and the drab soil (Dongbeizhai) had the lowest. The transitional soil in Manaoke had an intermediate average background. The threshold to discern gold mineralization varies from one deposit to another. For example, soils with spore counts of 400 CFU/g soil can be regarded as anomalies in Dongbeizhai but not in Axi because of the different thresholds.
|
DownLoad:
CSV
Relatively low spore counts were found in soils, which directly overlaid the gold containing orebodies. One reason for this association may be the high gold content in these soils. In a study of the El Real mineralization, Mexico, Melchior et al. (1994) reported that B. cereus spore counts peaked at locations where the auriferous quartz veins did not reach the surface. Low spore counts were found in soils where the orebodies outcropped, suggesting that metal toxicity may have suppressed B. cereus spores. However, the total metal contents analyzed except gold showed no apparent association with the spore counts in soils in the present work. Parduhn (1991) also reported low spore counts in soils where the orebody outcropped the surface at the Mesquite deposit, southern California. Insufficient information was given about the soil types in her study however, and therefore it might not be comparable to this present study.
In the M2 profile the spore counts decreased with increasing gold content in soils. Generally, the spore counts increased upslope, while soil gold content increased downslope. The increase in gold content may have resulted from the effect of creep.
Although the distribution trend of B. cereus spore counts in the Axi gold deposit is similar to that of the Manaoke deposit (low spore counts overlying outcropped areas of orebodies with spore anomalies at both sides), the relationship between the subsurface orebodies and the soil gold contents is somewhat different from each other. On the M1 profile in the Manaoke deposit, soil gold anomalies just overlay the underlying orebodies. However, in the Axi deposit, the soil gold anomalies flanked the subsurface orebodies. Thus the soil gold anomalies had a pattern of distribution comparable to that of spore counts in Axi. Further research is needed to examine the distribution patterns of soil gold contents and B. cereus spore counts at different gold deposits.
In general, the data of all soil transects show that the spore counts of B. cereus can indicate the soil gold anomaly and the underlying gold mineralization. The spore counts close to the underlying gold mineralized areas were two to three orders of magnitude higher as compared to the background. A spatial shift was apparent between the anomalies of B. cereus spore counts and the corresponding soil Au content.
These data suggest that the distribution pattern of spore counts can outline the subsurface mineralization, whereby orebodies underlay low spore counts with two spore anomalies. This kind of indication is particularly apparent in the two profiles of the Manaoke deposit and two soil profiles in the Axi deposit. This pattern was present in deposits characterized by different soil types (drab/brown soil for Dongbeizhai, meadow soil in Axi, and the transitional soil type in Maonaoke).
The signal intensity of B. cereus spore method in response to the underlying mineralization has yet to be elucidated. High counts associated with underlying gold mineralization were found in the Axi deposit that also had a higher background spore level. The signal to noise ratio (abnormal counts to background counts) seemed to be the highest at the Dongbeizhai gold deposit that had the lowest background of spore counts. The background of B. cereus spore counts is related to complex environmental factors such as the soil type, temperature, rainfall and humidity whilst the distribution pattern of spore count anomaly is mainly associated with the subsurface mineralization, and the anomaly intensity is affected by both the underlying mineralization and background.
No spore anomalies were found in the soils overlying the low-grade orebodies. It is conceivable that low-grade orebodies will be missed with this microbial geoexploration technique. In general, the technique presented in this paper is best suited for field application in combination with routine, conventional geoexploration methods.
We thank the Geological Team of Northwestern Sichuan and the 205 Geological Survey Team of Sichuan Province for their help with the fieldwork and providing the geological profile data. The participation of Zhang Jun, Wang Zhiping, Zhou Xuewu, Zhou Qiaowei, Xiong Wei and Zhang Xiaojun is gratefully acknowledged. We thank Olli H. Tuovinen for helpful comments on the manuscript. The work was supported by the Ministry of Land and Resources (No. 2000441 and 95-02-002-03), the Ministry of Education (Outstanding Youth University Teachers Fund), and the National Natural Science Foundation (No. 40202011) of China.
| Baily, W. H., 1871. Palaeontological Remarks. In: Traill, W. A., Egan, F. W., eds., Explanatory Memoir to Accompany Sheets 49, 50 and Part of 61 of the Maps of the Geological Survey of Ireland Including the Country around Downpatrick, and the Shores of Dundrum Bay and Strangford Lough, County of Down. Alexander Thom, Dublin & London. 22-23 |
| Bischoff, G. C. O., 1986. Early and Middle Silurian Conodonts from Midwestern New South Wales. Courier Forschungsinstitut Senckenberg, 89: 1-337 http://www.researchgate.net/publication/308340881_Early_and_Middle_Silurian_conodonts_from_midwestern_New_South_Wales |
| Chen, X., 1984. Silurian Graptolites from Southern Shaanxi and Northern Sichuan with Special Reference to Classification of Monograptidae. Palaeontologia Sinica (New Series B), 20: 1-102 (in Chinese with English Summary) |
| Chen, X., 1986. On Streptograptus and Its Paleoautecology. In: Palaeontological Society of China, ed., The Thirteenth and Fourteenth Academic Annual Meeting Symposium of Palaeontological Society of China. Anhui Science & Technology Publishing House, Hefei. 115-137 (in Chinese with English Summary) |
| Chen, X., Rong, J. Y., 1996. Telychian (Llandovery) of the Yangtze Region and Its Correlation with British Isles. Science Press, Beijing. 162 (in Chinese with English Abstract) |
| Chen, Z. Y., Wang, C. Y., Fan, R., 2016. Restudy of the Llandovery Conodont Biostratigraphy in the Xiushan Area, Chongqing City, China. Canadian Journal of Earth Sciences, 53(7): 651-659. https://doi.org/10.1139/cjes-2015-0189 |
| Editorial Group of Regional Stratigraphic Chart of Sichuan Province, 1978. Regional Stratigraphic Chart of Southwest China, Sichuan Province. Geological Publishing House, Beijing. 672 (in Chinese) |
| Epstein, A. G., Epstein, J. B., Harris, L. D., 1977. Conodont Color Alteration: An Index to Organic Metamorphism. Geological Survey Professional Paper, 995: 1-27. https://doi.org/10.3133/pp995 http://ci.nii.ac.jp/naid/10010125900 |
| Ge, Z. Z., Rong, J. Y., Yang, X. C., et al., 1977. Ten Silurian Sections in SW China. Stratigraphy and Palaeontology, 8: 92-111 (in Chinese) http://www.researchgate.net/publication/281323375_Ten_Silurian_sections_of_southwest_China |
| Ge, Z. Z., Rong, J. Y., Yang, X. C., et al., 1979. Silurian in SW China. In: Nanjing Institute of Geology and Palaeontology, Academia Sinica, ed., Carbonatite Biostratigraphy in SW China. Science Press, Beijing. 155-220 (in Chinese) |
| Geng, L. Y., 1986. Lower Silurian Chitinozoans from Bayu of Daozhen, Guizhou and Dazhongba of Yichang, Hubei. Acta Palaeontologica Sininca, 25(2): 117-128 (in Chinese with English Abstract) |
| Geng, L. Y., Qian, Z. S., Ding, L. S., et al., 1997. Silurian Chitinozoans from the Yangtze Region. Palaeoworld, 8: 1-152 |
| Geng, L. Y., Wang, Y., Zhang, Y. B., et al., 1999. Discovery of Post-Llandovery Chitinozoans in the Yangtze Region and Their Significance. Acta Micropalaeontologica Sinica, 16(2): 111-151 (in Chinese with English Abstract) |
| Jin, C. T., Ye, S. H., He, Y. X., et al., 1982. The Silurian Stratigraphy and Paleontology in Guanyinqiao, Qijiang, Sichuan. People's Publishing House of Sichuan, Chengdu. 84 (in Chinese with English Abstract) |
| Jin, C. T., Ye, S. H., Jiang, X. S., et al., 1989. The Silurian Stratigraphy and Paleontology in Erlangshan District, Sichuan. Geological Publishing House, Beijing. 224 (in Chinese with English Abstract) |
| Kiipli, E., 2004. Redox Changes in the Deep Shelf of the East Baltic Basin in the Aeronian and Early Telychian (early Silurian). Proceedings of the Estonian Academy of Sciences, Geology, 53(2): 94-124 |
| Lin, B. Y., Su, Y. Z., Zhu, X. F., et al., 1998. Stratigraphy Code of China: Silurian. Geological Publishing House, Beijing. 104 (in Chinese) |
| Loydell, D. K., 1990. On the Graptolites Described by Baily (1871) from the Silurian of Northern Ireland and the Genus Streptograptus Yin. Palaeontology, 33(4): 937-943 http://www.researchgate.net/publication/322805144_On_the_graptolites_described_by_Baily_1871_from_the_Silurian_of_Northern_Ireland_and_the_genus_Streptograptus_Yin |
| Loydell, D. K., 1992. Upper Aeronian and Lower Telychian (Llandovery) Graptolites from Western Mid-Wales, Part 1. Monograph of the Palaeontographical Society, 146: 1-180 |
| Loydell, D. K., Štorch, P., Melchin, M. J., 1993. Taxonomy, Evolution and Biostratigraphical Importance of the Llandovery Graptolite Spirograptus. Palaeontology, 36(4): 909-926 |
| Loydell, D. K., Männik, P., Nestor, V., 2003. Integrated Biostratigraphy of the Lower Silurian of the Aizpute-41 Core, Latvia. Geological Magazine, 140(2): 205-229. https://doi.org/10.1017/s0016756802007264 doi: 10.1017/S0016756802007264 |
| Loydell, D. K., Frýda, J., Gutiérrez-Marco, J. C., 2015. The Aeronian/Telychian (Llandovery, Silurian) Boundary, with Particular Reference to Sections around the El Pintado Reservoir, Seville Province, Spain. Bulletin of Geosciences, 90(4): 743-794. https://doi.org/10.3140/bull.geosci.1564 http://www.researchgate.net/publication/284187361_The_AeronianTelychian_Llandovery_Silurian_boundary_with_particular_reference_to_sections_around_the_El_Pintado_reservoir_Seville_Province_Spain |
| Männik, P., 2010. Distribution of Ordovician and Silurian Conodonts. In: Põldvere, A., ed., Estonian Geological Sections, Bulletin 10, Viki Drill Core. Geological Survey of Estonia, Tallinn. 21-24 |
| Männik, P., Tinn, O., Loydell, D. K., et al., 2016. Age of the Kalana Lagerstätte, Early Silurian, Estonia. Estonian Journal of Earth Sciences, 65(2): 105-114. https://doi.org/10.3176/earth.2016.10 |
| McLaughlin, P. I., Emsbo, P., Brett, C. E., 2012. Beyond Black Shales: The Sedimentary and Stable Isotope Records of Oceanic Anoxic Events in a Dominantly Oxic Basin (Silurian; Appalachian Basin, USA). Palaeogeography, Palaeoclimatology, Palaeoecology, 367/368: 153-177. https://doi.org/10.1016/j.palaeo.2012.10.002 http://www.sciencedirect.com/science/article/pii/S0031018212005500 |
| Mu, E. Z., Boucot, A. J., Chen, X., et al., 1986. Correlation of the Silurian Rocks of China. GSA Special Papers, 202: 1-80. https://doi.org/10.1130/spe202 http://ci.nii.ac.jp/ncid/BA01454539 |
| Nanjing Institute of Geology and Palaeontology, Academia Sinica, 1974. A Handbook of Stratigraphy and Palaeontology of Southwest China. Science Press, Beijing. 454 (in Chinese) |
| Ogg, J. G., Ogg, G. M., Gradstein, F. M., 2016. A Concise Geologic Time Scale. Elsevier, Amsterdam. 234. https://doi.org/10.1016/C2009-0-64442-1 http://www.researchgate.net/publication/303898618_A_Concise_Geologic_TimeScale_2016 |
| Rejebian, V. A., Harris, A. G., Huebner, J. S., 1987. Conodont Color and Textural Alteration: An Index to Regional Metamorphism, Contact Metamorphism, and Hydrothermal Alteration. Geological Society of America Bulletin, 99(4): 471-479. https://doi.org/10.1130/0016-7606(1987)99<471:ccataa>2.0.co;2 doi: 10.1130/0016-7606(1987)99<471:CCATAA>2.0.CO;2 |
| Rexroad, C. B., 1967. Stratigraphy and Conodont Paleontology of the Brassfield (Silurian) in the Cincinnati Arch Area. Indiana Geological Survey Bulletin, 36: 1-64 http://agris.fao.org/agris-search/search.do?recordID=AV20120116254 |
| Rong, J. Y., Chen, X., Wang, C. Y., et al., 1990. Some Problems Concerning the Correlation of the Silurian Rocks in South China. Journal of Stratigraphy, 14(3): 161-177 (in Chinese with English Abstract) http://www.researchgate.net/publication/284106218_Some_problems_concerning_the_correlation_of_the_Silurian_rocks_in_South_China |
| Rong, J. Y., Chen, X., Su, Y. Z., et al., 2003. Silurian Paleogeography of China. In: Landing, E., Johnson, M., eds., Silurian Lands and Seas: Paleogeography Outside of Laurentia. New York State Museum, Albany. 243-298 |
| Rong, J. Y., Wang, Y., Zhang, X. L., 2012. Tracking Shallow Marine Red Beds through Geological Time as Exemplified by the Lower Telychian (Silurian) in the Upper Yangtze Region, South China. Science China Earth Sciences, 55(5): 699-713. https://doi.org/10.1007/s11430-012-4376-5 |
| Song, H. J., Wignall, P. B., Song, H. Y., et al., 2019. Seawater Temperature and Dissolved Oxygen over the Past 500 Million Years. Journal of Earth Science, 30(2): 236-243. https://doi.org/10.1007/s12583-018-1002-2 |
| Štorch, P., Kraft, P., 2009. Graptolite Assemblages and Stratigraphy of the Lower Silurian Mrákotín Formation, Hlinsko Zone, NE Interior of the Bohemian Massif (Czech Republic). Bulletin of Geosciences, 84(1): 51-74. https://doi.org/10.3140/bull.geosci.1077 http://www.oalib.com/paper/2965732 |
| Sun, Z. Y., Fan, J. X., Wu, L., et al., 2019. Stratigraphy of the Lungmachi Black Shales from the Huaying Drill Core in Southwestern China and Its Palaeogeographic Implications. Palaeoworld, 28(3): 295-302. https://doi.org/10.1016/j.palwor.2019.01.001 |
| Tang, P., Xu, H. H., Wang, Y., 2010. Chitinozoan-Based Age of the Wengxiang Group in Kaili, Southeastern Guizhou, Southwest China. Journal of Earth Science, 21(S1): 52-57. https://doi.org/10.1007/s12583-010-0168-z |
| Walliser, O. H., 1964. Conodonten des Silurs. Abhandlungen des Hessisches Landesamt für Bodenforschung, 41(106S): 1-106 (in German) |
| Wang, C. Y., 1998. The Age of the Silurian Red Beds in South China. Journal of Stratigraphy, 22(2): 127-128 (in Chinese with English Abstract) |
| Wang, C. Y., Aldridge, R. J., 2010. Silurian Conodonts from the Yangtze Platform, South China. Special Papers in Palaeontology, 83: 1-136 |
| Wang, C. Y., Chen, L. D., Wang, Y., et al., 2010. Affirmation of Pterospathodus Eopennatus Zone (Conodonta) and the Age of the Silurian Shamao Formation in Zigui, Hubei as well as the Correlation of the Related Strata. Acta Palaeontologica Sinica, 49(1): 10-28 (in Chinese with English Abstract) |
| Wang, C. Y., 2011. Restudy on the Ages of Silurian Red Beds in South China. Journal of Stratigraphy, 35(4): 440-447 (in Chinese with English Abstract) |
| Wang, C. Y., 2013. Silurian Conodonts in China. University of Science and Technology of China Press, Hefei. 230 (in Chinese with English Summary) |
| Wang, G. X., 2011. Early Silurian Corals from the Baiyun'an Formation of Huaying Mountain, Sichuan, SW China: [Dissertation]. University of Chinese Academy of Sciences, Beijing. 1-79 (in Chinese with English Summary) |
| Wang, G. X., Deng, Z. Q., Zhan, R. B., 2011. Coral Fauna of the Baiyun'an Formation (Silurian; Llandovery) from Huaying Mountain, Eastern Sichuan. Acta Palaeontologica Sinica, 50(4): 450-469 (in Chinese with English Abstract) |
| Wang, G. X., Zhan, R. B., Deng, Z. Q., et al., 2013. Paleoecological Associations of Middle Llandovery (Silurian) Corals from Huaying Mountain, Eastern Sichuan Province. Science China Earth Sciences, 56(4): 640-646. https://doi.org/10.1007/s11430-012-4567-0 |
| Wang, H. Y., Guo, W., Liang, F., et al., 2015. Biostratigraphy Characteristics and Scientific Meaning of the Wufeng and Longmaxi Formation Black Shales at Well Wei 202 of the Weiyuan Shale Gas Field, Sichuan Basin. Journal of Stratigraphy, 39(3): 289-293 (in Chinese with English Abstract) |
| Wang, H. Y., Guo, W., Liang, F., et al., 2017. Black Shale Biostratigraphic Characteristics and Stratigraphic Correlation in the Wufeng and Longmaxi Fms of the Xuanhan-Wuxi Areas. Natural Gas Industry, 37(7): 27-33 (in Chinese with English Abstract) |
| Wang, L. T., 1976. The Silurian in Guizhou Province. Geological Bureau of Guizhou, Huishui. 68 (in Chinese) |
| Wang, X. F., Ni, S. Z., Zhou, T. M., et al., 1987. Silurian. In: Wang, X. F., Ni, S. Z., Zhen, Q. L., et al., eds., Biostratigraphy of the Yangtze Gorge Area 2: Early Palaeozoic Era. Geological Publishing House, Beijing. 143-197 (in Chinese with English Summary) |
| Wang, Y., Rong, J. Y., Zhan, R. B., et al., 2014. New Study of the Silurian System in the Butuo District, Southern Sichuan, SW China. Journal of Stratigraphy, 38(3): 257-267 (in Chinese with English Abstract) |
| Worsley, D., Baarli, B. G., Howe, M. P. A., et al., 2011. New Data on the Bruflat Formation and the Llandovery/Wenlock Transition in the Oslo Region, Norway. Norsk Geologisk Tidsskrift, 91: 101-120 |
| Ye, S. H., 1991. Discovery of Spirograptus Turriculatus in the Erlangshan Area, Sichuan. Journal of Stratigraphy, 15(1): 66 (in Chinese) |
| Yin, Z. X., Chen, Q. X., Li, P., et al., 1958. New Ideas of Geology at Qilian Mountains. Science Bulletin, 9(4): 113-115 (in Chinese) |
| Zhang, W. T., 1962. Ordovician System. Science Press, Beijing. 161 (in Chinese) |
| Zhang, X. L., Wang, Y., Rong, J. Y., et al., 2014. Pigmentation of the Early Silurian Shallow Marine Red Beds in South China as Exemplified by the Rongxi Formation of Xiushan, Southeastern Chongqing, Central China. Palaeoworld, 23(3/4): 240-251. https://doi.org/10.1016/j.palwor.2014.01.002 |
| Zhang, X. L., Liu, J. B., Wang, Y., et al., 2018. Onset of the Middle Telychian (Silurian) Clastic Marine Red Beds on the Western Yangtze Platform, South China. Palaeogeography, Palaeoclimatology, Palaeoecology, 497: 52-65. https://doi.org/10.1016/j.palaeo.2018.02.005 |
| Zhou, X. Y., Zhai, Z. Q., Xian, S. Y., 1981. On the Silurian Conodont Biostratigraphy, New Genera and Species in Guizhou Province. Oil and Gas Geology, 2(2): 123-140 (in Chinese with English Abstract) |
| Zhou, X. Y., Yu, K. F., 1984. Early Silurian Conodonts from Nanjiang, Chengkou and Yuechi, Sichuan. Journal of Stratigraphy, 8(1): 67-70 (in Chinese) |
| Zhou, Z. Y., Chen, P. J., 1990. Biostratigraphy and Geological Development of Tarim. Science Press, Beijing. 366 (in Chinese) |
Figures(7)
Copyright © 2013-2020 Journal of Earth Science 鄂ICP备15021562号-2
Tel: +86-27-67885075 Fax: +86-27-67885075 E-mail: xbb@cug.edu.cn
Address: Editorial Office of Journal, China University of Geosciences, Yujiashan, Wuhan, Hubei 430074, P. R. China
Supported by:
Beijing Renhe Information Technology Co. Ltd
E-mail:
info@rhhz.net
DownLoad:
DownLoad:
