The latest Carboniferous to Triassic Sydney-Gunnedah-Bowen basin system in the eastern Australia is an elongate structural basin that loCates between the Lachlan Caledonian Fold Belt in the west and the New England Fold Belt in the east. Extending from the Gunnedah district in the north to the Batemans Bay in the south, the Sydney Basin is a sub-basin loCated in the southern part of the Sydney-Gunnedah-Bowen Basin system. The Permian in Sydney basin consists of sedimentary sequences of fluvial, delta, littoral and shallow marine environments, as well as volcanic rocks. In the southwest of southern Sydney basin, the Permian unconformably onlaps the highly deformed and metamorphosed Lachlan fold Belts. The Permian System from the southern Sydney Basin comprises the Lower Permian Tallaterang Group (consisting of Clyde Coal Measures and Wasp Head Formation), Shoalhaven Group (consisting of the Lower Permian Yadboro & Tallong Conglomerate, Yarrunga Coal Measures, Pebbly Beach Formation, Snapper Point Formation and the Middle Permian Wandrawandian Siltstone, Nowra Sandstone, Berry Siltstone and Broughton Formation) and the Upper Permian Illwarra Coal Measures. From the latest Carboniferous to the Middle Triassic, the Sydney-Bowen Basin had experienced different tectonic phases from a back-arc extensional regime to a typical foreland basin: a back-arc extensional phase, a passive thermal sag phase and a flexural loading and increased compressional phase.

The carbonate rocks of the Cambrian in Yichang area are well developed. Limestone is mainly distributed in the Tianheban Formation and Shuijingtuo Formation of the lower Cambrian, as well as the Shipai Formation of the lower Cambrian and Keqibao Formation and Guanshannao Formation of the middle Cambrian. It can be divided into grain limestone (oolitic limestone, oncolitic limestone, calcirudite and calcarenite), grain-bearing micritic limestone (bioclast-bearing micritic limestone) and micritic limestone. Dolostone is the main rock type of this area. According to the mechanism of dolomitization, it can be divided into penecontemporaneous dolostone and post-penecontemporaneous dolostone.  Micritic dolostone distributes widely in the middle and upper Cambrian and is yellowish brown and brick-colored red, in which parallel laminae, bird’s-eyes and mud-cracks are developed. According to whether remnant grains exist, post-penecontemporaneous dolostone can be divided into remnant grain dolostone and crystalline dolostone. Crystalline dolostone is formed by seepage-reflux dolomitization and burial dolomitization.    According to petrology, biological assemblage and structural features of carbonate rocks, the auther reconstructed the sedimentary environments of formations of the carbonates in Yichang area.

The Dongpu Depression is a sub-tectonic unit of the Bohai Bay Basin. In the depression, four sets of salt rock  developed in two depositional cycles of the Paleogene, which occurred respectively in the fourth submember(S34),third submember(S33) and second submember(S32) of member III(S3) of  the Shahejie Formation, and member I of the Shahejie Formation (S1 ) . They are mainly distributed in the north part of the Dongpu Depression. In the center of the depression, salt rock is the thickest. Every set of salt contains many salt rhythms,  and each rhythm is composed of salt bed and mud bed. Laterally, salts grade into mudstones and sandstondes. The salt is formed in deep basin in arid climate. The salt material is derived from the uprising brine from deep underground. Layered brine is the basic form for the formation of salt. The upwelling path of the brine is large basement faults. Magmatism provides the dynamic force. Because of insulation of the salt layers, the temperature and pressure beneath should be affected, and this will quicken the maturation and evolution of organic matter. Salt is excellent cap-rock, witch is plastic under high temperature and pressure. Previous exploration showed that the lithologic reservoir is closely related with salt deposition. So for further exploration, it is very important to understand the distribution laws of the salts in the Dongpu Depression.

Lishui36-1 structure lies in the middle-eastern part of western subsag of Lishui Sag, Taibei Depression , East China Sea Shelf Basin. The subsag is a Cenozoic faulted basin and elongated in north-east direction. The Upper Paleocene Lingfeng Formation and Mingyuefeng Formation are main oil-gas bearing formations. On the basis of systematic sedimentology and well-logging facies studies of 3 Wells in Lishui 36-1 Structure, clastic sediments in the Upper Palaeocene were mainly from the Minzhe Uplift Area to the west of Lishui Sag and Lingfeng Uplift Belt in middle Lishui Sag, and probably also from the Yandang Uplift Area in the north part of the sag. Different provenances controlled the development and distribution of depositional systems by synsedimentary faulting and sea-level changes.  In the subsidence stages of the Lishui Sag and rapid sea-level rise,  terrigenous clastics derived from the Lingfeng Uplift Belt were transported across the eastern boundary faults to the margin of the western subsag to form fan delta deposits, and further  into the center of the subsag to form deepwater turbidite fan deposits and neritic deposits. Meanwhile, clastics from the Minzhe Uplift Area were poured onto the western slope of the western subsag from different inlets to form fan delta deposits which might be further delivered to deepwater area to form deepwater turbidite fan deposits. According to the theory of oil-gas accumulation and provenance analysis, deepwater turbidite fan deposits and fan delta front deposits can form favorable source-reservoir-cap rock associations for oil-gas and are the most prospective areas for exploration.

Duyun movement occurred between the late Ordovician and early Silurian, which resulted in an united uplift belt (commonly called Qian Zhong Oldland) from Dian Zhong uplift to Qian Zhong uplift. This uplift belt separated southeast Yunnan--south Guizhou region from northeast Yunnan--north Guizhou--south Sichuan region, which belong to two different depositional--tectonic domains, one in the south, and another in the north. In the south domain, lower and middle Cambrian, middle and upper Silurian, and lower Devonian series developed. There is an unconformity between the Cambrian and Silurian, and the Ordovician and Early Silurian are missing. On the contrary, in the Luquan --Wuding region of the  north domain, the Ordovician is complete, and is unconformably overlain by the Devonian, with the Silurian missing. The two different depositional sequences in north and south domains indicate that these two domains developed independently. In the middle--late Silurian, the area south of the Qian Zhong uplift should belong to  the Upper Yangtze Plate and the foreland flexural basin in Yunnan--Guizhou--Guangxi block. This area extended northeast from Qujing via Yadu of Hezhang--Guiyang to west Hunan, and southward linked with Huchun Sea in Yunnan. The area  north of the Qian Zhong uplift should belong to the marginal facies of the foreland basin (Sichuan south--Guizhou north) in the Upper Yangtze Plate.

Based on the systematic research of the composition, distribution and taphonomy characteristics of trace fossils in the Shahejie Formation of Paleogene in Chezhen and Zhanhua Sags, Jiyang Depression , Shandong province, this paper suggests three kinds of ichnocoenoses in the paleo-lacustrine sediments: (1) Scoyenia Ichnocoenosis, which consists of Scoyenia, Beaconites, Taenidium, Planolites, Palaeophycus, Macaronichnus, Gordia, Skolithos, Ophiomorpha, Sagittichnus and Favreina and so on, may serve to represent a regularly desiccated sandy and muddy shore and extremely shallow lacustrine sedimentary environment;(2)Mermoides Ichnocoenosis, which is characterized by such deeper water pattern fossils as Mermoides, Neonereites, Planolites, Helminthopsis, Helminthoidichnites, Vagrichnus and Cochlichnus, may display deeper lacustrine sedimentary environment;(3) Macaronichnus Ichnocoenosis, which mainly includes some common trace fossils as Macaronichnus, Planolites, Palaeophycus, Skolithos, Monocraterion, Arenicolites, Brevitubus, Margaritichnus, cf.Thalassinoides and other Rhizoliths, generally occurs in the interchange sedimentary setting between middle and low energy water bodies, such as lacustrine delta plain, delta-front sand bar, sand bank and storm sediments in the shallow lacustrine environment, and middle to outer fan turbidite deposits in the deeper lacustrine environment.

In the Kuqa River area, the kerogen maceration of the Triassic-Jurassic may be divided into 5 assemblages and 12 subassemblages based on its distribution characteristics. The evolution of paleoclimate during sedimentation of the Triassic-Jurassic inferred on the basis of ecology of sporopollen’s plants is: semi-arid (Ehuobulake Formation)→semi-humid (Lower Karamay Formation)→humid (Upper Karamay Formation－Kezilenur Formation)→semi-arid, semi-humid (Upper Kezilenur Formation－Lower Qigu Formation)→semi-arid (Middle-upper Qigu Formation－Kalaza Formation); and the evolution of paleoclimate type is: tropic-subtopic (Ehuobulak Formation－Taliqike Formation)→subtropic－warm temperate (Ahe Formation－Kezilenur Formation)→subtropic (Qiakemake Formation－Kalaza Formation). On the basis of maceration of kerogen, sedimentary characteristics and other data, it is inferred that lacustrine deposition was most developed in the Ehuobulake Formation, Upper Marker Member of the Karamay Formation, middle-lower part of members 2 to 4 of the Huangshanjie Formation, Upper Marker Member of the Yangxia Formation and Qiakemake Formation of the Triassic-Jurassic in this area. The Qigu Formation is the principal period of  flood lake development, and the Taliqike Formation, lower Yangxia Formation and Kezilenur Formation  are three principal periods of swamp development (mainly fluvial swamps, such as back-bank swamp and interdistributary swamp).

Based on the study of the characteristics of magnetic susceptibility and grain-size of the loess on the top of some typical sections including Haojiatai(HJT), Xiaochangliang(XCHL) and Donggutuo(DGT) in the Nihewan basin, we try to demonstrate the palaeogeographic status of the basin from the Late Pleistocene. The results indicated that the loess can be divided into three layers: S1, L1, and S0, which have the perfect correlation with those in the Loess Plateau of China and the marine oxygen isotope stage MIS1~MIS5. It recorded the short-term variations of climatic and environmental evolution over the last 130 ka. of North China. Loess of these sections shows the diversity of evolution of the basin. The uplift of the eastern part of the basin due to faulting made the lake vanish and loess was deposited, however, the western part of the basin was still lake during this period.

 Late Pliocene palynofloras of both Yangyi and Longling are dominated by angiosperms, along with a moderate number of ferns and gymnosperms, and a few algae. Compared with Yangyi playnoflora, Longling palynoflora contains more abundant subtropical elements of angiosperms, more ferns and less gymnosperms. Based on comparison with the vertical zones of modern vegetations, most elements of Longling palynoflora derived from the montane humid evergreen broad-leaved forest at elevation of 1600—2500m, with less contributions of the evergreen coniferous and broad-leaved mixed forest from 2300 to 2900m, whereas most of Yangyi palynoflora derived from the evergreen coniferous and broad-leaved mixed forest at elevation of 2800—3100m, with less contributions of evergreen coniferous forest above 3200m. Both Late Pliocene vegetations reflect a mountain subtropical climate with humidity.

The south coastal plain of the Laizhou Bay is a wide coastal area which lies between the outlet of the Xiaoqinghe River and that of the Jiaolaihe River. In this area , the industry and agriculture has developed quickly in recent years and the intrusion of underground saline water is very serious. In historic times , there existed three lakes in the south coastal plain of the Laizhou Bay: Judian Lake , Qingshuibo Lake and Biehua Lake. But they have already disappeared. To study the causes of disappearance of these ancient lakes is important to restore the palaeogeographic environments of the south coastal plain of the Laizhou Bay and establish the development direction of the lake-trace areas. Based on the data of the historical geography, the analysis of stratigraphic section, the textual research of the place name and satellite photographic interpretation, the authors studied the cause of disappearance of the ancient lakes in the south coastal plain of the Laizhou Bay, and pointed out that the causes are the drying climate, the migration of river and the activity of human beings. Among the three causes, the drying climate is the fundamental one. The migration of river is the direct cause and the activity of human beings speeds up the process of disappearance of ancient lakes.

 Based on core observation, thin section and SEM analysis and seismic interpretation of the Paleogene in western Qaidam basin, the study on sequence stratigraphy and forecast  of subtle oil reservoirs of the Paleogene was completed. The  basement structural framework and large deep faults in different locations and related palaeogeography and climate controlled distribution of sedimentary facies. The basin tectonics controlled sedimentary evolution obviously. Multiple unconformities led to multiple clastic sediment supplies to the basin, but the  supply was not sufficient to fill up the basin. Continuous existence of accomodation space led to well-developed lacustrine transgressive system tracts(LTST).  During deposition of lacustrine transgressive systems tracts,  the oil reservoirs and pools related to LTST were easily formed in the Paleogene of western Qaidam basin, which included delta front sandstone updip wedging-out lithologic pools, carbonate fissure pools, deep-lake turbidite pools, subtle pools near to sequence boundary and composite subtle pools controlled by structure and fault.

In this paper the pore texture characteristics of the  Dalinghe reservoir of  Shahejie Formation,of Paleogene in Shuguang Oil Field were analyzed from the lithology, diagenesis, pore types and clay minerals of the reservoir, and reservoir micro-heterogeneity and its affection on development effect were studied. The textural and compositional maturation of the Dalinghe reservoir is low. The upper part of the Dalinghe reservoir consists of feldspathic litharenite and the lower part consists of lithic arkose. Intergranular pores are the major pore type , and there are also some secondary solution pores in reservoir. Pore texture is mainly large pore with medium throat , and next is medium pore with thin throat and thin pore with thin throat. Clay minerals include montmorillonite, kaolinite and illite, and  montmorillonite is the most abundant especially in lower oil formations.  To prevent damaging pore structure and oil reservoir heavily during development, different exploiting schemes should be adopted and the flowing velocity of injected fluid in oil formation should be controlled considering the heterogeneity of upper and lower formations. While injecting steam whose PH should be 9 or so, certain amount of k+ should be added .