Silurian of Northern Qilian Mountains- Hexi Corridor consists of the Early Silurian Lujiaogou Conglomerate and Formation, the Middle Silurian Quannaogoushan Formation and the Late Silurian Hanxia Formation. Devonian consists of the Early and Middle Devonian Laojunshan Formation and the Late Devonian Shaliushui Formation. Lujiaogou Conglomerate is intermittently distributed over the western section of the Northern Qilian Mountains and is the deposits of submarine alluvial fan. Angzanggou Formation is widely distributed over the Northern Qilian Mountains- Hexi Corridor and is mainly bathyal flysch deposits. Quannaogoushan Formation and Hanxia Formation are distributed the western regions of the Northern Qilian Mountains- Hexi Corridor. Quannaogoushan Formation is composed of the neritic deposits of sandstone, mudstone and marlite, and Hanxia Formation of the littoral and neritic sandstone and mudstone. Laojunshan Formation is dispersed over the piedmont and intermountainous basin of paleo-Qilian Mountains and is composed of coarse clastic molasse. Shaliushui Formation is distributed over the eastern region of the Hexi Corridor and is composed of sandstone and mudstone of lacustrine facies. Silurian and Devonian regional palaeogeography is controlled by the irregular orogenic process of North Qilian from Caledonian to Early Hercynian. Lujiaogou Conglomerate is the sedimentary response to arc-continental collision during the earliest of Silurian. In the Early Silurian，the Northern Qilian Mountains- Hexi Corridor transforms from back-arc survival basin to foreland basin. In the middle and late Silurian, the orogeny in eastern part of North Qilian is strong. Connection between the eastern part of the orogenic belt and Alashan paleo-continental formed a disintegrating area. Foreland basin is merely located in the western region of North Qilian and Hexi Corridor. The Latest Silurian is main orogenic stage of North Qilian. Devonian Qilian mountains is high and the Early and Middle Devonian molasse formed in the piedmont and intermountainous basin of paleo-Qilian Mountains. In the Late Devonian the orogenic process is strong in the western part of the orogenic belt and formed a disintegrating area. The Late Devonian deposits of lacustrine facies formed in the eastern region of the Hexi Corridor.

 Qiangtang Basin can be divided into Northern Qiangtang Depression，the Center Uplift and Southern Qiangtang Depression. During the Early and Middle Triassic, Qiangtang Basin has the same framework of lithofacies and palaeogeography. Affected by marine transgression of Kekexili-Bayankala ocean trough, the Northern Qiangtang Depression depositted epicontinental sea sediments. At the same time, Southern Qiangtang and the Center Uplift were being denuded. Till to the Late Trassic, except to the west part of the Center Uplift, Qiangtang Basin was covered with water owing to the spreading of Bangonghu—Nujiang Ocean. Although the Northern Qiangtang Basin and Southern Qiangtang Basin were connected through Shuanghu strait, the origins of them were different, and their components of the tectonic and lithofacies were also different. The Southern Qiangtang Basin was an extensional marginal basin to the north of Bangonghu-Nujiang ocean, While the Northern Qiangtang Basin showed the character of foreland basins affected by Kekexili-Bayankala orogenic movement. The framework of lithofacies and palaeogeography had the feature of “Zonation along E-W,blocks in zones”, which was resulted from the regional tectonic evolution and basal faulting.

The Paleogene Shahejie Formation is the main petroliferous stratum in the Bonan Sag of Jiyang Depression in Bohai Gulf Basin.The features of the distribution of sedimentary facies of every member of the Shahejie Formation are various and the evolution of sedimentary facies is clear. During the early period of the fourth subage of the Shahejie Age, it is characterized by well-developed fan delta facies, which located in the south part of the Bonan Sag. Inshore-submerged fan was developed in the north margin, braided delta facies was lain in the east and west, and deposits of salty lacustrine were located in the center. During the late period of the fourth subage, it is characterized by well-developed salty lacustrine facies, which located in the deep-water area of the Bonan Sag. Semi deep-lake subfacies, shallow lake subfacies and lakeshore subfacies were developed respectively around the salty lacustrine facies. Moreover, there were some small-scale braided deltas locally. The third subage of the Shahejie Age was the period of full bloom of braided deltas. During this period, braided deltas were located in the southeast part of Bonan Sag. The main source area was Gudao Salient. Sandstone bodies of braided delta front are the most principal reservoir in which almost oil of Bonan Sag was preserved. The lacustrine facies was also developed throughout the third subage, especially the deep-lake subfacies and semi deep-lake subfacies were well developed. Through the uplift, erosion and sedimentation during the post third subage, the lacustrine basin of the second subage shallowed and mainly composed of shallow lake subfacies. Braided deltas with an extensive area were developed in the southeastern and northwestern of the study area. During the first subage, source area retreated with a large scale transgression of the lake. There only was lacustrine facies developed in the study area, in which the deep lake subfacies and semi deep lake subfacies were over prevailed.

Carbonate rocks are the most widespread deposits in the marine facies, and also distributed in the lacstrine and arid exposed environments. Carbonate rocks of Lower Paleogene Kumugeliemu Group in Kuqa Depression deposited in the typical tide flat of semi-closed bay, a part of northern edge of Neo-Tethys Ocean. These carbonate rocks include gypsiferous dolomites deposited in upper-tidal flat, bioclastic shoal, bioarenitic bank, oolites deposited in the mid-tidal flat, micritic limestones, lime mudstones and micritic dolomites deposited in the lower-tidal flat. Blackish lenticular marlites of the lower part of Cretaceous Bashijiqike Formation deposited in the deep lacstrine, localized merely distributed in Well Kela 201. The grayish lenticular marlites of the middle part of Cretaceous Bashijiqike Formation were deposited in the arid exposed environment, merely distributed in Kuchehe Section. Lacustrine carbonate facies mostly distributed in Qiakemake Formation and secondly in Yangxia Formation and Kezilenver Formation. There developped stromatolitic limestones deposited in the high-energic littoral lacstrine environment in the upper of Jurrasic Qiakemake Formation in Kapushalianghe Section. Blackish micritic limestones frequently accreted with grayish mudstones. They were the results of deep to semi-deep lacstrine environments. These carbonate rocks deposited in the different periods and different environments possess the various disciplinary characters of trace elements and carbon—oxygen isotopes. It is important to interpret depositional environment variety and basin evolution for these carbonate rocks. The chemistry data’s deviation of individual sample cannot influence whole sedimentary environments distinguished. The depositional environments of Carbonate rocks should be distinguished by integrating sedimentary structures of associated rocks, sedimentary assemblages, paleotology, sedimentary geochemistry and etc.

Taking the Minghuazhen Formation of Neogene in Gangxi Development area of Huanghua depression as an example, the paper is mainly focused on the method of sedimentary microfacies 3D modeling towards the area with a relatively sparse well network using the quantitative geometrical data obtained from the area with a dense well network with the similar sedimentary environment during the oilfield development stage. The result of the study on the area with dense well network shows, the width of the single channel sand body ranges from 50 to 300 meters , generally from 100 to 200 meters, and the thickness ranges from 5 to 15 meters , generally from 6 to 10 meters. The length and width of the overflow sand body are less than 200 meters. Jigsaw—puzzle and labyrinth are the two main sand architecture types. Based on the quantitative geometrical data obtained from the dense well network area, we adopt marked point process  method, carry out 3D sedimentary microfacies modeling study aiming at the target area with a relatively sparse well network, and achieve better effctiveness .

 The sedimentary system，tectonic features, lithological features and diagenesis of Palaeogene of Shahejie Formation in the eastern Chezhen Depression of Shandong Province are studied in detail. The characteristics of compaction and solution, cementation, secondary porosity during diagenesis processes and the distribution of secondary porosity zone in Chenzhen depression are described. The features of the cementation of carbonate cements and clay minerals indicates that the transition of the clay minerals montmorillonite—illite has evolutionary pattern of obvious gradation and mutation, and that the evolutionary processes experienced montmorillonite zone, gradation zone, rapid transition zone and illite zone. According to the relation of transition from montmorillonite to illite, the diagenesis of Shahejie Formation is divided into the early diagenetic stage (stage A, stage B), and the late diagenetic stage(stage A, stage B, stage C). The dividing indexes of the diagenetic stages are proposed.

Lacustrine sediments can record environmental changes,therefore analyzing their geochemical characters can reconstruct palaeoenvironment around lake basin. This paper makes in detail a geochemical analysis of lacustrine sediments from a core profile collected in the lacuster of Angulinao Lake, Bashang Plateau, North China. The environmental changes are confirmed by variations in concentrations of chemical elements such as Mg, Ca, Fe et al. and variations of  Mg/Ca, Ca/K, Fe/Al et al.. Combining with the varve chronology, Holocene environmental changes around Angulinao Lake can be speculated. In 8507—7453a BP, the climate was a little dry and cold, but turned to warm and humid; In 7453—4617a BP, the climate was warm and humid, but the short stage of arid exists(5137—4617a BP); In 4617—574a BP, the climate was cold and dry, but the stronger cold and dry climates arose at 4617a BP and In 1924—2494a BP. Since 574a BP, climate drives to humid in the earlier stage, but turns to dry since 383a BP. The climate changes around Angulinao Lake coincided with the other areas in North China at the same time.

Fossil woods collected from Pliocene sediments of western Yunnan are studied. Two type woods are identified. One is Rhododendron cf. racemosum Franchet belonging to Ericaceae. Its key characters include wood diffuse-porous, growth rings indistinct, vessel outline angular, perforation plates of vessel scalariform, helical thickenings throughout body of vessel element and ray heterogeneous type II. The other is Pinus armandii Franchet belonging to Pinaceae. Its key characters include cross-fields pitting window-like, normal axial and horizontal resin canals with thin epithelial cells present. Both fossil woods are firstly described from China. Based on anatomical features and ecological condition of extant taxa and vegetation distribution, growth environment of fossil woods is subtropical humid upland climate at altitude of 1800m or so.

The formation and evolution of Liaohe Meso-Cenozoic Basin was controlled by the variation of different regional stress field. Based on the analysis of structural features, volcanic activities, sequence construction and so on, Liaohe Basin has experienced the period of dextral transtensional stress field in Late Jurassic-Early Cretaceous, Middle and Late Paleocene, Late Eocene, Miocene, and also the period of sinistral compresso-shear stress field in Late Cretaceous, Early Paleocene, Early and Middle Eocene, Oligocene, Pliocene.  The variation of regional stress field can be genetically interpreted by the rotation speed variation of the earth and its impact on the movement of lithosphere plate and deep processes of the earth, it is also related to the earlier structural feature and boundary of the basin. This variation results not only in the cyclicity of basin evolution, also in the formation of multiple oil bearing sequence in Meso-Cenozoic in Liaohe Basin and adjacent area.

 Ichnosedimentologic evidence of periodic anoxic shelf in the Early—Middle Ordovician transition includes lower ichnodiversity, shallower bioturbation and burrowing depth (? 4 cm), rare domichnia, tiny Chondrites occupying shallower or shallowest tiering, wide distributed nodules of limonite pseudomorphs after pyrite, occurrence of trace fossils being closely associated with the storm event layers, and stratigraphic successions with orbital cyclostratigraphic architecture. We suggest that lower atmospheric oxygen level during the Early Paleozoic, the Ordovician radiation, dramatic transgression and warmer temperatures would result in the periodic anoxia in the Early—Middle Ordovician transition. This episode began at the later Early Ordovician and lasted about 3.4 Ma on the basis of orbital cyclostratigraphy.

 Now in the development of oilfields, it is far from enough to determine only the sedimentary facies of sandbodies, and the width, length and other parameters of the sandbodies should be predicted precisely.—This is quantitative study of sedimentary facies referred to in this paper. On the basis of drilling data and fine division and correlation of strata, quantitative study  was made on the sedimentary facies of the lower member of Lower Tertiary Xiaganchaigou Formation of Shaxi Oilfield, Qinghai Province. The lower member of the Ganchaigou Formation consists of clastic rocks, about 250m thick. It is divided into four oil-containing formation sets, i.e. I, II, III and IV. Formation set IV is deposited in delta plain environments of a braided river delta, and formation sets I, II and III are deposited in delta plain environments of a meandering river delta.  In the delta plain of the braided river delta, sandbodies are mainly deposited in distributary channels. These sandbodies are wide ribbons in shape and SW-NE in trend. They are commonly 1200-3000m wide and 5-10m thick. Their width/thickness is commonly 200-280. In the delta plain of the meandering river delta, sandbodies are mainly deposited in distributary channels. These sandbodies are narrow ribbons in shape. They are commonly 400-700m wide and 3-6m thick. Their width/thickness is commonly 80-110. Sandbodies of the braided delta plain are wider and thicker than those of meandering delta plain. This is because frequent shifting of braided distributary channels leads to lateral combining and vertical superimposing of sandbodies. Due to diffenrent width of sandbodies of different facies,  inter-well distance of development wells should be different for braided delta plain and meandering delta plain.