Evaporites diagenesis

Diagenesis and catagenesis can alter the evaporite minerals after burial. For example, high temperatures, pressures, and pore-water salinities characteristic of deep burial lead to the conversion of gypsum into anhydrite. Thus, evaporite mineralogy reflects not only the environmental conditions under which the evaporite was formed, but also those under which diagenesis and catagenesis occurred. 

Poinsot J, Adam P, Trendel JM, Connan J, Albrecht P, Diagenesis of higher plant triterpenes in evaporitic sediments, Geochim Cosmochim Acta 59 4653—4661, 1995. 

McLennan, S. M. plus 31 coauthors (2005) Provenance and diagenesis of the evaporite-bearing Bums formation, Meridiani Planum, Mars. Earth and Planetary Science Letters, 240, 95-121. 

Machel H.G. (1989) Relationships between sulfate reduction and oxidation of organic compounds to carbonate diagenesis, hydrocarbon accumulations, salt domes, and metal sulfide deposits. Carbonates and Evaporites 4,137-151. 

Kushnir, J. (1981) Formation and early diagenesis of varved evaporite sediments in a coastal hypersaline pool. Journal of Sedimentary Petrology 51, 1193-1203. 

Morad, S., Al-Aasm, I.S., Longstaffe, F.J., Marfil, R., De Ros, L.F., Johansen, H. Marzo, M. (1995) Diagenesis of a mixed siliciclastic/evaporitic sequence of the Middle Muschelkalk (Middle Triassic), the Catalan Coastal Range, NE Spain. Sedimenlology, 42, 749-768. 

Purvis, K. (1992) Lower Permian Rotliegend sandstones, southern North Sea a case study of sandstone diagenesis in evaporite-associated sequences. Sediment. Geol., 77, 155-171. 

Thermocatalytic sulfate reduction probably is the main source of H2S in the deep subsurface (25.81). The reactions in Table II, based on the evolution of H2S and CO2 by sulfate reduction of hydrocarbons in clastic sequences where there is available SO42- (i.e. sequences with evaporite beds or cements), illustrate the importance of this process to diagenesis. Not only does it provide a diagenetic sink for Fe via pyrite, but depending on the relative availability of reactants, can either cause precipitation or dissolution of calcite and alter feldspars to clay minerals. 

The main factors controlling a sandstone compaction are shales diagenesis and subsequent overpressures, the presence of evaporite formations which permit heat loss due to their high thermal conductivity, and early quartz overgrowths which resulted in a solid sandstone skeleton before Mesozoic subsidence. These overgrowths have impeded further reservoir compaction. Mapping such early quartz overgrowth devel-... 

Smith. G. I. I. Friedman, 1986. Seasonal diagenetic changes in salts of Owens Lake, California, 1970-77. In Mumpton, F. A. (ed.) Studies in Diagenesis. U. S. Geol. Survey Bull. 1578 21-29. Smoot, J. P. T. K. Lowenstein. 1991. Depositional environments of non-marine evaporites. In Melvin, J. L. (ed.) Evaporites, Petroleum and Mineral Resources. Elsevier, New York 189-348. Snyder, R. L. D. L. Bish, 1989. Quantitative analysis. In Bish, D. L. J. E. Post (eds.) Modem Powder Diffraction. Mineralogical Society of America, Reviews in Mineralogy, Volume 20 101-144. 

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