Figure
1.
Geological map, outcrops, well, stratigraphic system and lithology from Upper Permian to Lower Triassic of western Sichuan depression. Sys. system; Form. formation; Mem. member.
| Citation: | Shengxiang Long, Shixiang Wu, Hongtao Li, Zhenrui Bai, Jinyu Ma, Hua Zhang. Hybrid Sedimentation in Late Permian-Early Triassic in Western Sichuan Basin, China. Journal of Earth Science, 2011, 22(3): 340-350. doi: 10.1007/s12583-011-0186-5
|
The so-called hybrid sedimentation is generally defined as the concurrent occurrence of different sedimentations, such as mechanical sedimentation of terrigenous clastics and chemical sedimentation of carbonates. In a narrow sense, hybrid sedimentation refers to the mixing of terrigenous clastics and carbonate components (i.e., grains or lime) in the same layer, i.e., hybrid rock (Yang and Sha, 1990). While in a broad sense, it also includes the alternating deposits of terrigenous clastics and carbonates, such as alternative interbed, intercalation and lateral facies change (Sha, 2001).
The hybrid sedimentations have been recognized a very long time ago, but specialized studies on them only began in the 1980s (Dott and Byers, 1981; Button and Vos, 1977; Maxwell and Swinchatt, 1970; Carozzi, 1955; Bruckner, 1953). Zuffa (1980) gave the classification of hybrid arenits. Mount (1984) gave a clear definition of mixed carbonate-siliciclastic sedimentation in a shallow shelf environment and recognized 4 types of hybrid sedimentations. Several researchers (Dong et al., 2007b; Zhang, 2003; Budd and Hurris, 1990; Zhang and Ye, 1989) argued that hybrid sedimentation can occur in different depositional en-vironments at different geological periods. Brett and Baird (1985), Mack and James (1986), and Myrow and Landing (1992) studied the mechanisms of hybrid sedimentation and their influencing factors. Shan-mugam and Moiola (1982) and Vail (1987) pointed out that most of the terrigenous clastics had been transported to the relatively deeper depositional environment at the age of lowstand systems tract, when the sediments cross over the shelf via fluvial transportation. Droxler and Schlager (1985) and Austin et al. (1988), however, argued that at the period of high-stand systems tract, drowning of carbonate platforms greatly enlarges the area for shallow carbonate production and muddy and sandy carbonate sediments are transported to a deeper water environment via turbid flow, resulting in the mixed carbonate-siliciclastic sedimentation. Haq et al. (1987), Sarg (1988) and Yose and Heller (1989) pointed out that in peritidal environment and so on, the terrigenous clastics and shallow water carbonate shelf are close and extensive mixed carbonate-siliciclastic sedimentation could occur. Yang and Sha (1990) and Jiang and Sha (1995) studied in detail the Middle Carboniferous hybrid sedimentations in eastern Yunnan Province and the Lower–Middle Cambrian hybrid sedimentations in western Shandong Province. Wang (2001) and Wang et al. (1991) studied the mixed biogenetic carbonates and terrigenous siliciclastics in the modern reef zones in South China Sea. Ma and Liu (2003) and Luo et al. (2004) analyzed the features and genesis of hybrid sedimentations in the first member of the Haisha Formation in Dagang and in the fourth member of the Shahejie Formation in the Bonan sag and Bohai Bay basin, respectively. Zhang (2000) presented a classification scheme of hybrid rocks and their genetic types. Dong et al. (2007a) also published their views on hybrid sedimentation. As a whole, studies on hybrid sedimentation are still few.
Hybrid sedimentation widely exists in western Sichuan basin. But experts (Li et al., 1997; Zhang et al., 1995) had discovered hybrid sedimentation only in Silurian and Devonian. During a research of the marine carbonates in western Sichuan basin, the authors recognized that mixed carbonate-siliciclastic sedimentations are common in the Upper Permian–Lower Triassic based on observations of a large amount of outcrops, cores and seismic interpretation. This article describes in detail the hybrid sedimentation, and analyzes the geological conditions and their effects on diagenesis and reservoir features of hybrid sedimentation.
The mixed carbonate-siliciclastic sedimentation mainly occurs in the Longtan Formation and Changxing Formation (Fig. 1).
In well You-1, the thickness of Longtan Formation is 141 m, of which the cumulative thickness of limestone is 49.5 m, accounting for 35.11%, that of muddy limestone is 10 m, accounting for 7.09%, that of mudstone and shale is 52.5 m, accounting for 37.22%, and that of basalt is 29 m, accounting for 20.85%. While the thickness of the Changxing Formation is 58 m, of which the cumulative thickness of mudstone and shale is 36.5 m, accounting for 62.93%, that of limestone is 13.5 m, accounting for 23.28%, and that of breccia-limestone is 8 m, accounting for 13.79%. The mixing of terrigenous siliciclastics and carbonates is obvious.
In well Nuji, the thickness of the Longtan Formation is 103.5 m, of which the cumulative thickness of shale is 86 m, accounting for 83.09%, that of muddy limestone is 12 m, accounting for 11.59%, and that of biolimestone is 5.5 m, accounting for 5.31%. While the thickness of the Changxing Formation is 118.5 m, of which the cumulative thickness of muddy limestone is 112 m, accounting for 94.51%, and that of shale is 6.5 m, accounting for 5.49%. The mixing of terrigenous siliciclastics and carbonates is also very obvious, and the hybrid rocks (muddy limestone) are predominant.
The mixed carbonates-siliciclastics sedimentations are common (Fig. 1).
In well Shoubao-1, the hybrid sedimentations occur in the fourth member of the Feixianguan Formation and consist of non-isopachous to slightly isopachous alternating beds of purple to light purple mudstone and silty mudstone with purplish red siltstone, muddy siltstone and grey limestone. The hybrid sedimentation is even more outstanding in the second member of the Jialingjiang Formation. The upper part consists of slightly isopachous alternating beds of grey, grayish green or purplish red limestone with grayish mudstone and muddy limestone, containing interbeds of purplish red mudstone, grey calcareous mudstone or grey-white anhydrite rock. The middle part is composed of purplish red muddy limestone and grey calcareous mudstone. The lower part is composed of purplish calcareous dolomite and dolomite. The hybrid sedimentation also occurs in the first member of the Jialingjiang Formation. The upper part consists of slightly isopachous alternating beds of purplish red or grey calcareous siltstone and argillaceous siltstone with purplish red mudstone or silty mudstone. The middle part is composed of slightly isopachous to non-isopachous alternating beds of purplish mudstone with light purplish red calcareous siltstone, containing interbeds of grey oolitic calcisiltite. The lower part is composed of grey limestone.
In well Dashen-1, the Feixianguan Formation is 213.5 m thick and is a set of alternating beds of dark purple mudstone with brownish purple lithic arkose. The upper part contains two brownish grey fine-micritic limestone, while the lower part contains light brownish grey coarse-silt crystalline oolitic limestone with mudstone interbeds. The Jialingjiang Formation is 483.5 m thick, and is dominated by gypsum and salt rocks, limestone and dolomite. The content of terrigenous clastics increases from top to bottom. Its second member is composed of grey-to-grayish fine-silt crystalline dolostone with dark grey (brownish) grain dolomite interbeds, gypsiferous dolomite and brown mudstone. Its first member consists of grayish grain limestone with purplish grey fine vitric arenite interbeds and dark purple mudstone. The bottom part is brownish grey oolitic limestone.
In well You-1, the thickness of the second to fourth members of Feixianguan Formation is 307 m, of which the cumulative thickness of limestone and biolithite is 32 m, accounting for 10.42%, that of mudstone and shale is 247.5 m, accounting for 80.62%, and that of conglomeratic siltstone, sand-stone and conglomeratic sandstone is 28.5 m, accounting for 9.28%. The thickness of the first member of Feixianguan Formation is 34 m, of which the cumulative thickness of limestone is 23 m, account-ing for 67.65%, and that of mudstone and shale is 11 m, accounting for 32.35%. The thickness of the second member of the Jialingjiang Formation is 78 m, of which the cumulative thickness of dolomite is 23.5 m, accounting for 30.13%, that of shale and mudstone is 30.5 m, accounting for 39.11%, that of limestone is 4 m, accounting for 5.13%, that of limy dolomite is 3 m, accounting for 3.85%, that of dolomitic limestone is 4 m, accounting for 5.13%, and that of muddy limestone and marl is 13 m, accounting for 16.66%. The thickness of the first member of Jialingjiang Formation is 100 m, of which the cumulative thickness of limestone is 17 m, and that of mudstone and shale is 83 m.
In the Tongkou-Huanglianqiao area, hybrid sedimentation mainly occurs in the second and third members of the Feixianguan Formation. The third member consists of purplish red mudstone with 3 thin interbeds of hoar oolitc limestone. The second member is composed of alternating purplish red or tawny calcareous mudstone with thin laminated muddy limestone. Hybrid sedimentation is relatively common in the Jialingjiang Formation. Its fourth and fifth members are mainly composed of yellowish grey thin laminated argillaceous dolomite and gypsum-karst breccia with a thickness of 13–15 m. Its third member consists of alternating grayish or yellowish grey thin to moderate laminated dolomite, limy dolomite, dolomitic limestone and limestone, with thin purplish red mudstone interbeds. The lower part of the second member consists of hoar moderate-to-thick laminated oolitic doloarenite and thin laminated purplish red or grayish green silty mudstone. Middle part is composed of alternating hoar thick massive oolitic dolomite and thin laminated doloarenite, with purplish or grayish green mudstone interbeds. The upper part is massive gypsum-bearing oolitic limestone. The lower part of the first member is hoar limy dolomite. The middle part is alternating thin grayish brown calcareous siltstone with purplish red mudstone, and the upper part is alternating moderate-to-thick laminated siltstone with thin limy mudstone.
In Dafeishui region, the second member of the Feixianguan Formation is yellowish grey moderate-thick laminated calcarenite with purplish red mud-stone interbeds. The first member is grey thin lami-nated limestone with grayish green thin shale inter-beds. The fourth and fifth members of the Jialingjiang Formation are thin-moderate laminated grey dolomite with marl and mudstone interbeds.
In Longmendong region, the fourth and fifth members of the Jialingjiang Formation are composed of grey limestone and dolomite with gypsum-karst breccia and thin shale interbeds (Fig. 2). Its second member consists of moderate-thick laminated grey dolomitic limestone with purplish grey shale and sandstone interbeds and ooides occur in the limestone. Its first member is purplish red sandstone with thin limestone and shale interbeds. The limestone interbeds in the upper part get thicker and are dominated by coarse-to-moderate crystalline limestone.
Hybrid rocks are also interpreted on seismic sections in this study. Seismic reflectance signatures are clear in the Upper Permian mixed carbonate-siliciclastic lithofacies, and are composed of 3 strong phases with high energy, good continuity and relatively low apparent frequency. The first phase may get weaker sometimes, but the second and third phases may have good continuity and high energy. In contrast, the seismic reflections in the carbonate lithofacies are composed of several phases, of which the top and bottom phases are high in energy and good in continuity, while the middle phases feature in relatively low energy, unstable continuity and relatively high apparent frequency. Abrupt contact and gradual contact occur in the mixed carbonate-silicilastic lithofacies and carbonate lithofacies (Fig. 3).
The boundaries between the mixed carbonate-siliciclastic facies tract and the terrestrial facies tract or carbonate facies tract can be defined by using the data of wells Zhougong-1, Han-1, You-1, Dashen-1 and Shoubao-1 and the outcrop data in Ebian, Niulangba and Longmendong areas and in combination with the seismic data.
Two major types of hybrid rock are recognized through microscopic observation. The first is the hybrid rocks composed of mud-silt-sized carbonate and silt-sized siliciclastics. In sandy mud-silt-sized dolostone, the terrigenous clastics are quartz and feldspar in uneven or scattered distribution, and there are horizontal beddings or no beddings (Fig. 4a), indicating that they were deposited in a low energy setting. Although dolomitic fine to silty sandstone with cross bedding deposited in local high energy areas (Fig. 4b), the grain size is small as a whole and the original pores were strongly influenced by the late compaction.Therefore, the properties of these hybrid rocks are too poor to form effective reservoirs.
The second type is hybrid rock dominated by terrigenous clastics of fine or silt grade (such as quartz and feldspar). These clastics are distributed in the intergranular spaces of carbonate ooides (without clear zonal structure) as interstitial matters (Figs. 4c and 4d) and their content commonly ranges from 3% to 6%, indicating a sedimentary setting with relatively high energy. Their initial intergranular porosity is relatively high and may be potential reservoir rocks. However, it depends on the modification of late diagenesis.
The western Sichuan basin is located at the western margin of the Yangtze plate. Most of the Yangtze plate was relatively stable during the tectonic evolution over several hundreds Ma to Hercynian, except for Longmenshan where the huge plate-marginal faults were active. In the Middle Permian, the western Sichuan basin experienced the largest transgression since the Paleozoic and was turned into a shallow marine environment where carbonate ramp deposits were formed. The thermal uplifting of the Emei mantle plume and Emei taphrogeny greatly modified and complicated the tectonic setting in this area at the end of Middle Permian.
The extensional movement was strong in the western Sichuan basin in the Late Permian which resulted in differential uplifting of fault blocks, and there was a wide range of regression. The Kangdian ancient land located at the southwest corner of Si-chuan basin began to show progressive uplift and enlarge, forming the major provenance of terrigenous clastics. At the same time, existence of Emeishan ba-salt at Kangdian ancient land frontier which greatly impacted the distribution of facies in the western Si-chuan basin provided important terrigenous clastics for the mixed sedimentary of carbonate and clastic rocks. In Changxingian age, terrigenous clastics sedi-mentary and Emeishan basalt were distributed along the margin of Kangdian ancient land to Dafeishui, wells Dashen-1 and Shoubao-1. Grey to grayish green silty to fine sandstone with shale and coal interbeds were deposited in an alluvial plain environment with volcanic eruption (Emeishan basalt). These facies turned into mixed terrigenous-carbonate sedimentation in the northeast direction to Beichuan and well Guanji. The terrigenous clastics sourced from Kangdian ancient land input into the relatively shallow water, resulting in an extensive limited platform-mixing tidal flat where moderately-thick laminated grey limestone, thin muddy limestone and purplish red sandy shale were deposited. Farther northward and eastward, open platform facies occurred and relatively pure grey bioclastic limestone and dark grey fine-silt crystalline limestone were deposited (Fig. 5).
The tectonic framework in the Early Triassic Feixianguanian stage was inherited from the Chang-xingian stage, and the Kangdian ancient land continued to develop because tectonic uplift had increased. Two transgression-retrogression cycles dominated by transgression occurred in this stage. The alluvial plain shrank to the west to Baoxing, Emei Mountain and the mixing tidal flat-limited platform also shrank to the south. The hybrid sedimentation of silty mudstone and siltstone interbedded gray limestone was limited to the south of Dujiangyan-Xindu. There were also no lack of shallow water exposed mark in mixed tidal facies, such as mud crack, tents structure and groove cast. Gradually to the northeast into the restricted platform facies, lithology was mainly the thick layered gray-purple oolitic limestone interbedded brown calcareous siltstone, gray thin-bedded calcarenite interbedded purple shale and gray dolomite interbedded gray shale bands, etc.. The area of the open platform was enlarged to some extent, while the reef-flat facies on the platform margin was unchanged, and dark gray argillaceous fine-silt-sized crystalline limestone interbedded thin-bedded marl, mudstone and gray oolitic limestone were deposited. At the end of the Feixian-guanian stage, water level lowered and purplish red mudstone was prevalent, indicating that short-term exposure occurred to some extent (Fig. 6).
In the Early Triassic Jialingjiangian stage, the paleogeographic features were also unchanged and were the succession and development of the Feixian-guan Formation. There were the sedimentary characteristics of southwest high, northeast low and deposition base slope facing east. Two complete transgression-retrogression cycles also occurred, which continued to provide favorable geological con-ditions for mixed sedimentary of carbonate and clastic rocks. However, the climate was dry and hot as a whole in this stage, thus the sedimentary facies changed to some extent. Water depth became larger progressively northeastward from the Kangdian acient land and the alluvial plain shrank farther to the ancient land. The mixing tidal flat was distributed to the west of Baoxing-Ya'an-Hongya-Leshan, where purplish red sandstone with thin limestone and shale interbeds and grey-dark grey silty mudstone with limestone were deposited. Most of the study area was covered by limited evaporite platform, several salt lake basins were developed, and platform margin facies was distributed along the Longmenshan Mountain (Fig. 7).
Physical property analysis and microscopic observation show that some oolitic limestone containing terrigenous clastics feature in very low porosity and strong cementation. Multiphase cementation features are clear. The first phase is fibrous or horse teeth-like rim cementation of calcite. The second phase is drusy mosaic of equant spar calcite, and cementation. The third phase is poikilotopic cementation of calcite (Fig. 8a). A twin structure can be observed under crossed polars. Replacement of siliciclastics by calcite cement occurred concurrently with cementation, resulting in harbor-shaped products (Fig. 8b). Compaction occurred after the first phase of cementation, leading to the deformation or fragmentation of the calcite cement formation in the first phase. Dolomitization can be observed in the core of some oolitic limestone. There-fore, the major diageneses include cementation, compaction, replacement and local dolomitization.
Microscopic observation reveals that the oolitic carbonates with terrigenous clastic commonly occur in the third member of the Feixianguan Formation and the first member of the Jialingjiang Formation. That is to say, they are common in the high energy facies of TST, while are relatively rare in HST. There are several possible causes. The input of terrigenous clastics was sufficient at the early stage of transgression due to relatively low sea level and large area of land. The eroded terrigenous clastics began to get mixed in the carbonate deposits with the transgression. In contrast, the input of terrigenous clastics was less in HST due to the relatively high sea level and small area of land. The diagenesis was obviously controlled by the sedimentation and diagenetic environment. The oolitic limestone or dolomite containing terrigenous clastics did not experience significant exposure due to the continuous transgression, thus the diagenesis was dominated by cementation in buried or marine diagenesis environment. In addition, as the hybrid sedimentation was relatively strong in the study area, non-permeable purplish red mudstone of tidal flat facies often occurs on the oolitic limestone or dolomite containing terrigenous clastics. The overlying mud-stone prevented the meteoric water from percolating downward during exposure, leading to weak dissolution but strong cementation. Taking the oolitic dolo-mite in the third member of the Feixianguan Formation on the Tongkou Section as an example, inter-granular calcite cementation of three stages is clear in the oolite or sand-sized intraclastic grain spaces. The cementation of the two stages basically filled inter-granular pores and the surviving pores were also filled by the poikiolopic calcite during burial (Fig. 8c), thus almost all the original pores disappeared.
Comparison shows that the diagenesis of the hybrid sedimentary is different to the equivalent strata carbonates in the adjacent carbonate facies and that the latter is more favorable for the development of effective reservoirs. For example, the oolitic carbonates in the Feixianguan Formation on the Yudongliang Section in the Northwest Sichuan basin contained no terrigenous clastics and were deposited in the carbonate facies. The dissolution of the oolites or sand-sized intraclastic grains was strong, resulting in well-developed geopetal structures and moldic dissolution pores. This indicates that oolitic shoal or sand-sized intraclastic shoal was exposed to meteoric water in the early diagenetic stage and the unstable minerals in the oolites (such as aragonite or high magnesian calcite) were dissolved. The existence of crystal grain cements inside and on the outer edge of the micrite envelops is also evidence of meteoric water influencing the oolites. After the dissolution of the unstable minerals in the carbonates, the concentrations of CO32- and Ca2+ in the diagenetic fluid increased, leading to the deposition of stable low-magnesian calcite cements on the edge and in the intergranular spaces of oolites. For example, the moldic pores in Fig. 8d were the products of granular cementation in the intergranular spaces of oolites after the oolites were completely leached by the meteoric water. On platforms without mixed terrigenous clastic deposits, the depositional model consists of shallowing-upward cycles. Gypsum rocks of evaporite platform facies were developed on the top and provided sufficient Mg2+ for late dolomitization, resulting in the quality dolomite reservoirs (such as the Feixianguan Formation in the Puguang gas field). Therefore, we predict that the carbonates in the mixed facies tract have few primary pores preserved and poorly-developed secondary pores due to the relatively high content of terrigenous clastics, strong compaction and weak dissolution, thus they are unfavorable for the development of effective reservoirs.
(1) Hybrid sedimentation widely exists in western Sichuan basin. Observation of large amounts of outcrops, cores and seismic interpretation shows that mixed carbonate-siliciclastic sedimentations are common in the Upper Permian–Lower Triassic.
(2) The extensional movement was strong in the western Sichuan basin in the Late Permian, resulting in differential uplifting of fault blocks and an extensive retrogression. The Kangdian ancient land progressively uplifted and enlarged, forming the major provenance of terrigenous clastics which greatly impacted the distribution of facies in the western Sichuan basin. This is the geological setting of hybrid sedi-mentation.
(3) In Changxingian stage mixed terrigenous-carbonate sedimentation was distributed in the area between Dafeishui-well Dashen-1-well Shoubao-1 and Beichuan-well Guanji. The terrigenous clastics sourced from Kangdian ancient land input into the relatively shallow water, resulting in an extensive limited platform-mixing tidal flat where moderately-thick laminated grey limestone, thin muddy limestone and purplish red sandy shale were deposited. The tectonic framework in Feixianguanian stage was inherited from the Changxingian stage. The hybrid sedimentation was limited to the south of Dujiangyan-Xindu. At the end of the Feixianguanian stage, water level lowered and purplish red mudstone was prevalent, indicating that short-term exposure occurred to some extent. In Jialingjiangian stage, the paleogeographic features were also unchanged and two complete transgression-retrogression cycles also occurred. The mixing tidal flat was distributed to the west of Baoxing-Ya'an-Hongya-Leshan, where purplish red sandstone with thin limestone and shale interbeds and grey-dark grey silty mudstone with limestone were deposited.
(4) The carbonates in the mixed facies tract have few primary pores preserved and poorly-developed secondary pores due to the relatively high content of terrigenous clastics, strong compaction and weak dissolution, thus they are unfavorable for the development of effective reservoirs.
ACKNOWLEDGMENT: All authors are gratefully acknowledged Mr. Guo Xushen and Mr. Guo Tonglou for their help in providing data and discussing the result of this research.| Austin, J. A., Schlager, W., Palmer, A. A., et al., 1988. Leg 101—An Overview. In: Austin, J. A., Schlager, W., eds., Proceedings of the Occan Drilling Program. Scientific Results, 101: 455–472 |
| Brett, C. E., Baird, G. C., 1985. Carbonate-Shale Cycles in the Middle Devonian of New York: An Evaluation of Models for the Origin of Limestones in Terrigenous Shelf Sequences. Geology, 13: 324–327 doi: 10.1130/0091-7613(1985)13<324:CCITMD>2.0.CO;2 |
| Bruckner, W. D., 1953. Cyclic Calcareous Sedimentation as an Index of Climatic Variation in the Past. Journal of Sedimentary Petrology, 23: 235–237 |
| Budd, D. A., Harris, P. M., 1990. Carbonate-Siliciclastic Mixtures. SEPM, Tulsa, Oklahoma. 272 |
| Button, A., Vos, R. G., 1977. Subtidal and Intertidal Clastic and Carbonate Sedimentation in a Macrotidal Environment: An Example from the Lower Proterozoic of South Africa. Sedimentary Geology, 18(1–3): 175–200 http://www.sciencedirect.com/science?_ob=ShoppingCartURL&_method=add&_eid=1-s2.0-0037073877900112&originContentFamily=serial&_origin=article&_ts=1433190017&md5=095547692f1de132fdc67a0732ff32c2 |
| Carozzi, A., 1955. Some Remarks on Cyclic Calcareous Sedimentation as an Index of Climatic Variations. Journal of Sedimentary Petrology, 25(1): 78–79 doi: 10.1306/D4269814-2B26-11D7-8648000102C1865D |
| Dong, G. Y., Chen, H. D., He, Y. B., et al., 2007a. Some Problems on the Study of the Mixed Siliciclastic-Carbonate Sediments. Advances in Earth Science, 22(9): 931–939 (in Chinese with English Abstract) http://en.cnki.com.cn/Article_en/CJFDTOTAL-DXJZ200709007.htm |
| Dong, G. Y., He, Y. B., Chen, H. D., et al., 2007b. Mixed Sedimentation of Carbonates of Lagoonal Facies and Terrigenous Clastics of the Middle Submember of Menber 1 of Shahejie Formation in Huimin Sag: Taking Shanghe Area in Shandong Province for an Example. Acta Sedimentologica Sinica, 25(3): 343–350 (in Chinese with English Abstract) http://en.cnki.com.cn/Article_en/CJFDTOTAL-CJXB200703002.htm |
| Dott, R. H., Byers, C. W., 1981. SEPM Research Conference on Modern Shelf and Ancient Cratonic Sedimentation—The Orthoquartzite Carbonate Suite Revisited. Journal of Sedimentary Petrology, 51(1): 329–346 |
| Droxler, A. W., Schlager, W., 1985. Glacial versus Interglacial Sedimentation Rates and Turbidite Frequency in the Bahamas. Geology, 13: 799–802 doi: 10.1130/0091-7613(1985)13<799:GVISRA>2.0.CO;2 |
| Haq, B. U., Hardenbol, J., Vail, P. R., 1987. Chronology of Fluctuating Sea Levels since the Triassic. Science, 235(4793): 1156–1167 doi: 10.1126/science.235.4793.1156 |
| Jiang, M. S., Sha, Q. A., 1995. Research Advances in the Mixed Siliciclastic-Carbonate Sedimentary Systems. Advance in Earth Sciences, 10(6): 551–554 (in Chinese with English Abstract) http://www.adearth.ac.cn/EN/abstract/abstract2245.shtml |
| Li, X. H., Liu, W. J., Zheng, R. C., 1997. Hybrid Facies and Mechanism for the Formation of the Mixed Devonian Carbonate-Siliciclastic Sediments in the Longmen Mountain Area, Sichuan. Sedimentary Facies and Palaeogeography, 17(3): 1–10 (in Chinese with English Abstract) http://search.cnki.net/down/default.aspx?filename=TTSD199703002&dbcode=CJFD&year=1997&dflag=pdfdown |
| Luo, S. S., Liu, K. Y., He, Y. B., et al., 2004. Mixed Sedimentary Characteristics and Mode of Terrigenous Clastics and Carbonate in Es4 of Bonan Depression. Journal of Jianghan Petroleum Institute, 26(4): 19–21 (in Chinese with English Abstract) |
| Ma, Y. P., Liu, L., 2003. Sedimentary and Diagenetic Characteristics of Paleogene Lacustrine "Hunji" Rock in Beach District, Dagang. Acta Sedimentologica Sinica, 21(4): 607–613 (in Chinese with English Abstract) http://en.cnki.com.cn/Article_en/CJFDTOTAL-CJXB200304010.htm |
| Mack, W. G., James, W. C., 1986. Cyclic Sedimentation in the Mixed Siliciclastic-Carbonate Abo-Hueco Transition Zone (Lower Permian), Southwestern New Mexico. Journal of Sedimentary Petrology, 56(5): 635–647 doi: 10.1306/212f89f9-2b24-11d7-8648000102c1865d |
| Maxwell, W. G. H., Swinchatt, J. P., 1970. Great Barrier Reef: Regional Variation in a Terrigenous-Carbonate Province. Geological Society of American Bulletin, 81: 691–724 doi: 10.1130/0016-7606(1970)81[691:GBRRVI]2.0.CO;2 |
| Mount, J. F., 1984. Mixing of Siliciclastic and Carbonate Sediments in Shallow Shelf Environments. Geology, 12(7): 432–435 doi: 10.1130/0091-7613(1984)12<432:MOSACS>2.0.CO;2 |
| Myrow, P. M., Landing, E., 1992. Mixed Siliciclastic-Carbonate Deposition in an Early Cambrian Oxygen-Stratified Basin, Chapel Island Formation, Southeastern Newfoundland. Journal of Sedimentary Petrology, 62(3): 455–473 http://www.researchgate.net/profile/Ed_Landing/publication/256116635_Myrow_P.M._and_E._Landing._1992._Mixed_siliciclastic-carbonate_deposition_in_a_Lower_Cambrian_oxygen-stratified_basin_Chapel_Island_Formation_southeastern_Newfoundland._Journal_of_Sedimentary_Petrology_62455473_Figs._18/links/00463521d0ed4445fc000000.pdf |
| Sarg, J. F., 1988. Carbonate Sequence Stratigraphy. In: Wilgus, C. K., Hastings, B. S., Kendall, C. G. S. C., et al., eds., Sea-Level Changes: An Integrated Approach. SEPM Special Publication, 42: 155–182 |
| Sha, Q. A., 2001. Discussion on Mixing Deposit and Hunji Rock. Journal of Palaeogeography, 3(3): 63–66 (in Chinese with English Abstract) http://en.cnki.com.cn/Article_en/ http://search.cnki.net/down/default.aspx?filename=GDLX200103008&dbcode=CJFD&year=2001&dflag=pdfdown |
| Shanmugam, G., Moiola, R. J., 1982. Eustatic Control of Turbidites and Winnowed Turbidites. Geology, 10(5): 231–235 doi: 10.1130/0091-7613(1982)10<231:ECOTAW>2.0.CO;2 |
| Vail, P. R., 1987. Seismic Stratigraphy Interpretation Using Sequence Stratigraphy. In: Bally, A. W., ed., Atlas of Seisimic Stratigraphy. AAPG Studies in Geology, 27(1): 1–3 |
| Wang, G. Z., Quan, S. Q., Lü, B. Q., 1991. Evolution of Modern Sedimentary Environments and Sedimentations in the Weizhou Inland Area, South China Sea. Marine Geology & Quaternary Geology, 11(1): 69–82 (in Chinese with English Abstract) http://en.cnki.com.cn/Article_en/CJFDTOTAL-HYDZ199101010.htm |
| Wang, G. Z., 2001. Mixed Sedimentation of Recent Reefoid Carbonates and Terrigenous Clastics in the North Continental Shelf of the South China Sea. Journal of Palaeogeography, 3(2): 47–54 (in Chinese with English Abstract) http://en.cnki.com.cn/Article_en/CJFDTOTAL-GDLX200102007.htm |
| Yang, C. Q., Sha, Q. A., 1990. Sedimentary Environment of the Middle Devonian Qujing Formation, Qujing, Yunnan Province: A Kind of Mixing Sedimentation of Terrigenous Clastics and Carbonate. Acta Sedimentologica Sinica, 8(2): 59–65 (in Chinese with English Abstract) http://en.cnki.com.cn/Article_en/CJFDTOTAL-CJXB199002008.htm |
| Yose, L. A., Heller, P. L., 1989. Sea Level Control of Mixed Carbonate-Siliciclastic Gravity Flow Deposition, Lower Part of the Keeler Canyon Formation (Pennsylvanian), South eastern California. GSA Bulletin, 101: 427–439 doi: 10.1130/0016-7606(1989)101<0427:SLCOMC>2.3.CO;2 |
| Zhang, J. Q., Ye, H. Z., 1989. A Study on Carbonate and Siliciclastic Mixed Sediments. Journal of Chengdu College of Geology, 16(2): 87–92 (in Chinese with English Abstract) http://en.cnki.com.cn/Article_en/CJFDTOTAL-CDLG198902012.htm |
| Zhang, T. S., Lan, G. Z., Chen, X. H., et al., 1995. Early Silurian Siliciclastic-Carbonate Ramp Deposits in NW Sichuan. Acta Sedimentologica Sinica, 13(4): 27–36 (in Chinese with English Abstract) http://en.cnki.com.cn/Article_en/CJFDTOTAL-CJXB504.002.htm |
| Zhang, X. H., 2003. The Upper Carboniferous Mixed Siliciclastic and Carbonate Sediments on the Margin of the Xuefeng Ancient Land. Journal of Stratigraphy, 27(1): 54–58 (in Chinese with English Abstract) http://www.cqvip.com/Main/Detail.aspx?id=7634278 |
| Zhang, X. H., 2000. Classification and Origin of Mixosedimentite. Geological Science and Technology Information, 19(4): 31–34 (in Chinese with English Abstract) http://www.researchgate.net/publication/313189755_Classification_and_origin_of_mixosedimentit |
| Zuffa, G. G., 1980. Hybrid Arenites: Their Compostition and Classification. Journal of Sedimentary Petrology, 50(1): 21–29 http://eurekamag.com/pdf.php?pdf=019152655 |
Figures(8)
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
Shengxiang Long, Shixiang Wu, Hongtao Li, Zhenrui Bai, Jinyu Ma, Hua Zhang. Hybrid Sedimentation in Late Permian-Early Triassic in Western Sichuan Basin, China. Journal of Earth Science, 2011, 22(3): 340-350. doi: 10.1007/s12583-011-0186-5
DownLoad:
DownLoad:
