Letter sectionLoss of calcareous microfossils from sediments through gypsum formation
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Cited by (36)
Mineralogical characterization and diagenetic history of Permian marine tuffaceous deposits in Guangyuan area, northern Sichuan basin, China
2021, Marine and Petroleum GeologyCitation Excerpt :Solution pores were filled by albite and ferrodolomite/dolomite, indicating that dissolution occurred after the devitrification and argillization of tuff and before the appearance of albite (Fig. 10). Both bacterial sulfate reduction (BSR) (Berner and Raiswell, 1983) and thermochemical sulfate reduction (TSR) (Toland, 1960) can cause organic matter in sediments to react to form pyrite, and cause carbonate minerals to dissolve and form autogenous gypsum (Schnitker et al., 1980; Muza and Wise, 1983). Albite, as a diagnostic mineral in hot water deposition, is commonly seen in submarine hydrothermal diagenesis and is the product of submarine hydrotherm mixed with seawater (Mills and Elderfield, 1995).
An effective method to distinguish between artificial and authigenic gypsum in marine sediments
2019, Marine and Petroleum GeologyCitation Excerpt :For fresh sediments with preformed ferric (hydr)oxides and no authigenic gypsum, the molar ratios of gypsum sulfur and ferric (hydr)oxide iron (i.e., atomic S/Fe ratios above) should be lower than 2 after artificial oxidation of pyrite. However, Schnitker et al. (1980) suggested that the aerobic oxidation of pyrite may also happen in deep-water marine environments. For example, dissolved oxygen can penetrate into the anoxic zone from overlying aerobic bottom seawater by infaunal activities, giving rise to the elevated sulfate concentrations in the subsurface sediments (e.g., Iversen and Jørgensen, 1985; Fossing et al., 2000; Claypool et al., 2006).
Nonevaporative origin for gypsum in mud sediments from the East China Sea shelf
2018, Marine ChemistryCitation Excerpt :Nonetheless, authigenic gypsum crystals have already been reported in sediments in the absence of evaporative or volcanogenic materials. For example, gypsum occurs, in association with pyrite, in fine-grained sediments of the South West African continental slope (Siesser and Rogers, 1976) and is usually accompanied by carbonate dissolution (Briskin and Schreiber, 1978; Schnitker et al., 1980). On the basis of their isotopic compositions, gypsum crystals have been explained to be the result of pyrite oxidation, as observed in cold-water carbonate mounds in the Porcupine Seabight, off Ireland (Pirlet et al., 2010), and in the eastern Pacific oxygen minimum zone (Blanchet et al., 2012).
Comparison of living and dead benthic foraminifera on the Portuguese margin: Understanding the taphonomical processes
2018, Marine MicropaleontologyFormation mechanism of authigenic gypsum in marine methane hydrate settings: Evidence from the northern South China Sea
2016, Deep-Sea Research Part I: Oceanographic Research PapersCitation Excerpt :Elevated porewater Ca2+ concentrations also favor precipitation of authigenic gypsum crystals. Laboratory experiments with fresh marine sediments demonstrate that the dissolution of biogenic carbonates can play an important role in the formation of gypsum (Schnitker et al., 1980). For example, oxidation of sedimentary sulfide can strongly enhance the production of H+, leading to porewater acidification and dissolution of carbonate sediment (e.g., Z.Y. Lin et al., 2016; Pierre et al., 2012; 2014; Pirlet et al., 2010, 2012).
Multi-year life spans of high salt marsh agglutinated foraminifera from New Zealand
2014, Marine MicropaleontologyCitation Excerpt :The calcareous tests dissolve because of the low pH of the porewater as a result of the sulphate reduction reactions that decay dead plant detritus near the surface and dying roots beneath the surface (e.g., Howarth and Teal, 1979). In some salt marsh core sequences that are now above tide levels and above ground water level for long periods of time, all the agglutinated foraminiferal tests have also disappeared (e.g., Big Lagoon, Hayward et al., 2010) through oxidation and bacterial degradation of organic cements (e.g., Schnitker et al., 1980; Goldstein and Watkins, 1999; Berkeley et al., 2007). Where exposure to oxygen has been less, the more fragile agglutinated tests (e.g., E. tetrastomella, Miliammina spp.) are preferentially lost by organic cement breakdown with consequent enhanced relative abundance of more robust tests (e.g., T. inflata, T. salsa).