This paper is a continuation from the papers on lithofacies palaeogeography of the Early, Middle and Late Cambrian and Early Ordovician in China. It is based on the present writers’ achievements of study and mapping of quantitative lithofacies palaeogeography of the Cambrian and Ordovician in North China, South China and Northwest China. On such a basis, in combination with geological data of other areas, mainly Mongolia-Xinganling, Kunlun-Qinling, Tibet, Hainan Island and Taiwan areas, through comprehensive analysis and judgment, the lithofacies palaeogeography map of the Middle Ordovician in China is compiled and this paper is completed. In this paper, the lithofacies palaeogeography in North China, South China and Northwest China is quantitative and the description is in detail, while the lithofacies palaeogeography in other areas is qualitative and the description is general. In the Middle Ordovician, the lithofacies palaeogeography framework of “two troughs alternating with three platforms”in the Early,Middle and Late Cambrian and Early Ordovician was unchanged. The two troughs are Tianshan-Beishan-Mongolia-Liaoning-Jilin Trough and Kunlun-Qinling Trough. The three platforms are Junggar-Mongolia-Xinganling Platform, Tarim-Qaidam-North China Platform and Tibet-South China Platform. The scope of these palaeogeographic units in the Middle Ordovician are basically the same with those in the Early, Middle and Late Cambrian and Early Ordovician, but the Characteristics of their second-rank palaeogeographic units are different from those.

Sediments of Paleozoic, Mesozoic and Cenozoic with a huge thickness were deposited in the Pre-Caspian Basin, which can be divided into three groups vertically, i.e Pre-salt Sediment Group, Salt Sediment Group and Post-salt Sediment Group. The Pre-salt Sediment Group is composed of the Lower Paleozoic—Lower Permian, including thick clastic and carbonate rocks. From Devonian to Early Permian, carbonates were deposited widely in the Pre-Caspian Basin, and in many palaeo-uplifts, bioherms well developed, which indicates that during this period, the offshore and shallow sea areas of the Basin belonged to shallow-water sedimentary environment with clear sea water and warm climate, with little terrestrial input of sediments from outside of the Basin. In middle and late periods of the Early Permian, the Pre-Caspian areas rose successively, the climate became dry, and the environment turned to be supratidal zone (evaporitic environment), resulting in the spread sedimentation of salts and the formation of the Salt Sediment Group (upper part of the Lower Permian) which consists mainly of halite and anhydrite. There are many salt dome structures within the Salt Sediment Group. In Late Permian and Triassic, the Basin underwent once again a large-scale transgression, and the depositional environment was shelf sea with delta locally. In Jurassic and Cretaceous, generally it was also the shelf sea (shallow sea), but there were lacustrine and lagoonal environments in different parts of the Basin. The Post-salt Sediment Group formed (Upper Permian—Quaternary) is composed mainly of clastic rocks, with carbonates locally.

Liuzan Oilfield , located at the boundary of Luannan County and Tanghai County of Hebei Province , frontal zone of Yanshan fold belt and eastern of Nanpu Sag of Bohaiwan Basin , is one of the most important oil fields of JiDong Oilfield . Influenced by Baigezhuang Fault and inclined palaeotopography , the stratigraphy of Member 3 of Shahejie Formation of Paleogene is characterized with low sorting , low maturity and complicated lithofacies , and as a result fan delta deposition model is built . By method of stratigraphic sequence , stratigraphic boundaries (unconformity surface and lake flooding surface ) and sedimentary cycle of Member 3 of Shahejie Formation in Liuzan Oilfield are recognized with seismic and logging data , and  high resolution sequence frame is made , i.e , 4 parasequence sets and 12 parasequences . The paper analyses  parasequences’ superposition style , divides parasequence sets into progradational sequence and retrograding sequence and  determines the location of excellent reservoirs in parasequences  and parasequence sets . On the basis of  palaeotopography , palaeoclimate , palaeecology and sedimentary facies  analysis , Lithofacies  palaeogeography of Member 3 of Shahejie Formation in Liuzan Oilfield is renewed with isopath map of sandstone . For Member 3 of Shahejie Formation in Liuzan Oilfield , the deposition environment is fan delta front and branch channel is the main sandstone microfacies. Sandstone distributes along north-east direction ,which is identical with that of palaeoprovenance .

Siwujiazi oilfield of Songliao Basin, located in the City of Gongzhuling in Jilin Province, is a part of Yangdachengzi Anticline at Southeast upwelling area. The reservoir of oilfield is mainly composed of Quantou Formation in Lower Cretaceous, which is deposited in dry and oxidized environment at Late Cretaceous. The source provenance area is central ancient-uplift. The reservoir is mainly composed of lithic arkoses and some lithic feldspathic sandstone, feldspathic litharenite sandstone. Based on the analysis of single well facies, the main facies marker include sedimentary structure and granularity distribution reflecting the traction current sedimentary mechanism. Through the analysis of facies marker, the reservoir is meandering river. There are 4 microfacies, i.e. meandering point bars, crevasse-splays, natural levees and flood plains. The vertical combination of the river is point bars-natural levees-crevasse-splays-flood plains from below to top. In setting up the logging facies, the microfacies of 136 non-sampling wells were identified, and then the inter-well sedimentary microfacies were forecasted by applying sequential indicator simulation. The research shows that there are two meander rivers stretching from NNE to SSW and the 6 and 7 layers of Quantou Formation which have the character of point bars. This study is an important foundation for next oilfield development.

The different views on the age, lithofacies and contact relationship of the strata related to the ophiolite melange belt in northeastern Jiangxi Province lead to the different explanations on the history of geological evolution of South China. The isotopic ages obtained from igneous blocks of the melange were mostly between 900 to 1000 Ma. On the other hand, some Paleozoic microfossils were found from a volcanic-sedimentary sequence (Dengshan Group) associated with the ophiolitic belt, but the exact ages of those fossils could not be determined. The paleogeographic analysis indicates that in Early Paleozoic there was not a “Jiangnan Paleocontinent”, but a deep-water “Jiangnan Basin” in northeastern Jiangxi Province . Late Ordovician pyroclastic deposits widely spread in South China, but their source is still unclear. Based on the lithofacies paleogeographic analysis, the eruptive center probably located in northeastern Jiangxi at that time, that just matched with the Dengshan Group formed in the volcanic island-arc environment. So that implies the Late Ordovician age to the Dengshan Group. In early Silurian the Jiangnan Basin closed and a Caledonian fold belt formed between the Yangtze Block and Cathaysian Block. The ophiolitic belt in northeastern Jiangxi Province was a suture between the fold belt and the Cathaysian Block. Here the distance between the two blocks are smallest in South China and rocks were strongly compressed, resulting in major uplift and stronger erosion. Therefore, Lower Paleozoic were difficult to be preserved in the area, and the Dengshan Group was just their remains.

A special phenomenon, ice-carrying-particles vertical movement, resulted from interactions among ice, water and silt (mud) particles is found in the Yellow river delta through field observations and simulation experiments. In late winter and early spring, ice melts and the fine sediments (silt or mud particles) under the ice layer are carried upwards with the melting of ice. Studies show that the processes of ice-carrying-particles vertical movement may be divided into three stages, i.e. fragmentation of sediments, part melting of ice and vertical carrying of silt or mud particles, silt or mud particles falling and some ice induced sedimentary structures forming. These sedimentary structures, ice-split seams, ice-induced pellets and ice-induced silt or mud slices, are important records for existing of ice and reconstruction of sedimentary environment and climate. In addition, the dynamical mechanism of this special movement is discussed in this paper, and two dynamical mechanisms are worked out. The first one is capillary action, and the second thermal convection of ice-melt water. Capillary action is the only dynamics in the open system where the ice-melt water can be discharged or leaked out, and the two dynamical mechanisms contribute together to the special movement in the close system where the ice-melt water can not be discharged or leaked out.

The aquatic biota from the late Late Pleistocene was sampled below 46m in the well Dacan 1 of Qaidam Basin.They showed a high abundance and high diversity. The ostracoda was Cyprideis torosa-Ilyocypris inermis assemblage and associated with Carophyta, Gastropoda, Pelecypoda, plants and fishes. The aquatic biota from 46 ~10 m of depth in the well Dacan 1 was the sediments from the Great Ice Age of the Last Glacial Stage. In that time, the climate was rather arid and iciness, so that the geological event of playa occurred. The deposits rapidly developed from lake facies mudstone to halite. It was hard to find fossils,and most of biota disappeared completely. The Three-Lake Depression (Taijinaier Lake、Dabusun Lake and Huobusun Lake ) was entirely covered by about 40 m of salt bed, which became the last barrier for preserving natural gas, namely the cover of the gas reservoir. The deposits above 10m in the well Dacan 1 gradually developed into shallow lake mud- stone and silt gypsiferous salt,which wrere formed in the Holocene warm stage (modern interglacial stage) , or the first stage of oxygen stable isotope. In this stage the salinity of the region decreased and the biota abundance and the biota diversity increased again. The ostracoda was replaced by an assemblage of Candona neglecta-Candoniella lactea, which was adapted to the environment of  the slight brackish and fresh water. It also associated richly with Carophyta, Gastropoda, Pelecypoda,etc.
Up to now, there has been abundant aquatic biota in the south of Taijinaier Lake、Dabusun Lake and Huobusun Lake because of the supply of freshwater from Kunlun Mountains. However, the water is relatively salty in the north of Taijinaier Lake、Dabusun Lake and Huobusun Lake due to the great distance away from the main supply of freshwater. The ostracoda was replaced by the typical salty-lake ostracoda Eucypris inflata assemblage. The distribution of gypsum-saline beds in the north is obviously more than that in the south of Taijinaier Lake,Dabusun Lake and Huobusun Lake.

The diagenetic process, porosity evolution , factors of controlling reservoir quality, the time and duration of entering and undergoing each diagenetic stage, of Donghe sandstones in central Tarim basin are studied. The relative primary and secondary porosity volume is gotten from microscopic measurement. According to the regional structural evolution, the factors controlling solution are discussed. Combined with the hydrocarbon filling and escaping history, the factors of secondary porosity surviving and disappearing are analyzed. The results indicate that Donghe sandstones in central Tarim basin went through the compaction, clay cementation, quartz overgrowth, carbonate cementation, solution and authentic kaolinite precipitation during the diagenesis, and now it is in the late diagenesis. There are some differences in diagenesis between east and west area. In the west area, the Donghe sandstones entered the early diagenesis B and late diagenesis A earlier than in east, and is with a clear lower solution-upper cementation sequence section. The eureservoir mainly distributed in the places which is of pure lithological components, low clay, continuing uplift, early hydrocarbon filling, and no carbonate cementation. That is the foreshore—shoreface area which has been being uplift since Permian.