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[Objective] The dispute in the paleogeographic pattern of the carbonate platform and distribution of reservoir facies during the deposition of the Dengying Formation in the middle-upper area, hinders the expansion of the exploration domain from the Mianyang-Changning intracratonic sag to other areas. [Methods] Detailed lithofacies and facies analysis was conducted on more than 30 sections (wells), [Results] further confirming that the mound-shoal is marked by massive peloidal/ooidal dolograinstone and columnar, domal dolostromatolite, which were deposited around the platform (or inner ramp) margin of the Middle-Upper Yangtze Platform gradually shifting outward into tempestite of the middle-outer ramp or slump dolobreccia, argillaceous dolomite and chert of slope-basin facies. Owing to the mound-shoal barrier, its back was dominated by tidal flat and lagoon. Of these, the tidal flat facies were marked by microbial dololaminite, domal dolostromatolite, dolothrombolite with minor peloidal dolograinstone, and dolomudstone, which are commonly arranged into meter-centimeter scale cycles. The lagoon facies were composed mainly of dolomudstone and peloidal dolowackestone. In general, the mound-shoal facies is present in the lower Dengying Formation along the platform to slope transition (or inner ramp to middle ramp transition) . In the Upper Yangtze Platform, it occurs in the Deng 1 (e.g., wells Pengtan 1, Ziyang 1, and sections Qingping, Beidoushan) or Deng 2 members at the Baijiaba, Yulin, and Meiziwan sections, or in both the Deng 1 and Deng 2 members at the Songlin-Yankong areas. On Middle Yangtze Platform, it occurs in the Hamajing (e. g., sections Sancha, Bailuya, and Tianping) or Baimatuo members of the upper Dengying Formation at the Miaohe section. Specifically, the mound- shoal facies shows repeated transgressions and regressions and occurs in different stratigraphic position of the Dengying Formation at many sections (Baiguoping, Xiaofenghe, Dengyingxia, Wushan, Xuejiadian, and Dengjiaya) . In contrast, the tidal flat and lagoon facies are widely present on the whole Middle-Upper Yangtze Platform, commonly associated with the grape-like dolomite at the lower-middle part of the Deng 2 member (or correlated stratigraphy) . The spatiotemporal distributions of these facies show a progradational trend of the Dengying Formation on the Middle- Upper Yangtze Platform, which consists of 2.5 depositional sequences with three progradations (shallowing) and two retrogradations (deepening) . The regressive system tract of Sequence 1 is formed by the lower Dengying Formation (the Deng 1 to middle Deng 2 or Hamajing members), characterized by the upward evolution of lagoon or moundshoal facies into tidal flat facies. On the Upper Yangtze Platform, Sequence 2 occurs in the upper Deng 2 member, marked by the regression of mound-shoal facies and the presence of more lagoonal dolomudstone, followed by the reoccurrence of tidal flat facies. On the Middle Yangtze Platform, Sequence 2 is present in the Shibantan member, represented by the deepening into middle ramp limestone or lagoonal dolomudstone and then shallowing into moundshoal or tidal flat facies. Sequence 3 on the Middle Yangtze Platform shows a similar deepening (transgression) and shallowing (regression) cycle. On the Upper Yangtze Platform, the transgressive systems tract of Sequence 3 is located in the siliciclastic rock of the Deng 3 member and the following transgressive systems tract is marked by the transition of lagoonal dolomudstone to tidal flat dolomicrobialite. [Conclusions] Owing to the denudation of the Dengying Formation at the platform margin-slope area and Upper Yangtze Platform beyond the current plate boundary, the platform marginal mound-shoal facies are locally present in the Deng 4 member. In this case, certain areas (e.g., the Songlin-Yankong area and periphery of the Middle Yangtze Platform) with platform marginal mound-shoal facies in the lower-middle Dengying Formation (Deng 1 to 2 or Hamajing to Shibantan members) are important exploration targets. Moreover, the lower Deng 2 and upper Deng 4 members (or coeval strata) formed during progradations composed of microbial dolomite throughout the Middle-Upper Yangtze Platform (or inner ramp) interior are also important exploration targets. Because the microbial dolomite was widely developed throughout the Middle-Upper Yangtze Platform interior, decoding the formation mechanism and distribution pattern of high-quality reservoir is the key to finding new hydrocarbon provinces. [ABSTRACT FROM AUTHOR]

The identification markers of paleokarst have been described in detail and include a combination of surface geology, drilling data and the isotopic characteristics of carbon, oxygen and strontium. The relationships between the vertical zoning, plane distribution and karstification degree of paleokarst and the reservoir development were further analyzed. The study shows that karstic breccias are the most direct sign of paleokarst features. Karsts of different genetic types and the intensity of dissolution have different stable isotopic characteristics from the surrounding cements, and their formation and evolution are significantly influenced by fluid sources, fluid nature and isotopic fractionation. The identification markers of small scale pinholes are quite different from that of large scale holes. The development and evolution of palaeokarsts are mainly controlled by structure, palaeoclimate and lithology. The best lithology for the development of reservoirs is dolomite in the C2hl2 formation. The best zones for the development of the reservoir is located in the upper and lower dissolution intervals of the C2hl2 formation and the best position for the development of reservoir is located in the karst highlands, remnant hills and sloping fields in the karst slope. Key words: eastern Sichuan, Huanglong Formation, palaeokarst reservoir, geochemistry, karst topography, karst cycle

Magnesium (Mg) is a major rock-forming element and biological nutrient element, and is thus an important link between continents, oceans and the Earth' s interior. Marine carbonates are a major reservoir of Mg and an important component of the global Mg cycle. Using Mg isotopes to trace the deposition-diagenesis process of marine carbonate formation is the prerequisite for reconstructing the deep-time seawater Mg isotopic composition (δ26MgSW) and quantifying the Earth' s historical marine Mg cycle. Studies using this approach have made considerable progress in the past two decades; for example: (1) investigation of Mg isotope fractionation during the formation of different carbonate minerals has been enhanced; (2) numerical models of Mg isotopic behavior have been established, providing constraints on the dolomitization process; and (3) the use of Mg isotopes to trace the early diagenetic fluid system has been explored. These have provided a theoretical base for using marine carbonate data to reconstruct δ26MgSW. The deposition-diagenesis process and its effects on Mg isotopic composition should be considered when selecting information from marine carbonate archives to reconstruct the marine Mg cycle. Critical evaluation combined with geochemi-cal models are necessary when choosing an archive for reconstructing deep-time <526MgSW. [ABSTRACT FROM AUTHOR]

Studies of the sedimentary facies and sequence stratigraphy have indicated that the main depositional environments of the Lower Triassic Jialingjiang Formation in the eastern Sichuan Basin were a restricted platforms and evaporite platforms. Two third-order sequences (SQ1, SQ2) and five fourth-order sequences (SSQ1-SSQ5) were recognized. Sediments in the Jialingjiang strata evolved from a restricted platform to an evaporite platform, then to restricted platform again, and finally to an evaporite platform. The main hydrocarbon reservoirs and producing layers appear in the SSQ1-SSQ2 sequence. Sequences SSQ1-SSQ5 are further subdivided into transgressive systems tracts (TST) and highstand systems tracts (HST). Taking these sequences as mapping units, lithofacies paleogeographic maps were prepared for each of the fourth-order tracts. Evidence from the study of the distribution of favorable reservoirs indicates that the restricted platform-to-platform shoal in the SSQ1 and SSQ2 sequences are key areas for future exploration. [ABSTRACT FROM AUTHOR]

Dolostone-evaporite paragenesis systems (DEPS) have been widely found in Precambrian to Quaternary strata worldwide. However' despite its wide spatio-temporal distribution' the formation mechanism and controlling factors of DEPS remain poorly studied. By reference to copious literature from China and elsewhere combined with previous knowledge of DEPS in China' this study comprehensively summarizes the development characteristics' combination patterns and formation mechanism of DEPS. Firstly' its spatio-temporal distribution is clarified based on published studies: laterally' DEPS is known to be widely distributed in 51 regions globally' mainly in the northern hemisphere (mostly in Asia' followed by Europe and North America). Comparatively' it is found less often in Africa and is only scattered in South America and Oceania. Stratigraphically' although DEPS is found in many Precambrian to Quaternary strata' it appears mostly in the Permian. The combination patterns of evaporite and dolostone in DEPS include the interbedding of dolostone and evaporite' with thick dolostone overlying thick evaporite' thick evaporite overlying thick dolostone' thick dolostone mixed with thin evaporite' and thick evaporite mixed with thin dolostone. The formation process' distribution and main controlling factors of symbiotic differences as well as the particularity and universality of the paragenetic system development are discussed. Secondly' based on macro- to microscale characterization of mineral types in DEPS' six types of evaporites and five types of dolostones have been found and their genesis is discussed. Finally' the properties' characteristics' sources and evolution paths of diagenetic fluids in DEPS are summarized. DEPS studies provide new concepts for solving the "dolostone (or dolomite?) " question' and promote the understanding of the important basic geological problems associated with DEPS. Such studies also provide theoretical guidance for the exploration of oil and gas resources in the paragenetic system. [ABSTRACT FROM AUTHOR]

The Lower Permian Fengcheng Formation in the Mahu Sag of the Junggar Basin was developed in a volcanic-induced alkaline saline lacustrine environment, with deposition of thick-bedded sodium carbonates and high-quality source rocks, as well as the borosilicate reedmergnerite, which is a rare mineral globally but is very rich in the Fengcheng Formation. Based on petrography, fluid inclusion and boron isotope studies, the aim of this study was to discover the origin of the reedmergnerite which, in the Fengcheng Formation, often replaces carbonate minerals, including shortite, eitelite, northupite, calcite, trona, and even barytocalcite. The homogenization temperature of the primary inclusions in the reedmergnerite ranged from 100 to 116°C. Previous synthetic experimental studies have found that the δ11B values of reedmergnerite are 0.33-2.13‰. It is proposed here that, due to the limitations of temperature and pressure in surface or shallow burial processes, the source of boron in reedmergnerite was deep hydrothermal fluid in the original sedimentary environment, mainly in deep diagenetic environments (>3000 m). Therefore, the enrichment of reedmergnerite in the Fengcheng Formation is interpreted as the result of intense magmatic hydrothermal activity and a long diagenetic history. [ABSTRACT FROM AUTHOR]