Research reportCoastal lithofacies and biofacies associated with syndepositional dolomitization and silicification (Draken Formation, Upper Riphean, Svalbard)
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Cited by (35)
Mesoproterozoic biomineralization: Cyanobacterium-like filamentous siderite sheaths ∼1.4 Ga
2023, Journal of PalaeogeographyIodine incorporation into dolomite: Experimental constraints and implications for the iodine redox proxy and Proterozoic Ocean
2022, Geochimica et Cosmochimica ActaPrediction of carbonate diagenesis from well logs using artificial neural network: An innovative technique to understand complex carbonate systems
2020, Ain Shams Engineering JournalCitation Excerpt :Carbonate rocks are formed by chemical, biological, and detrital process that dominantly involve skeletal remains and supplementary biological constituents including lime mud (skeletal), fecal pellets and microbialy arbitrated cement/lime muds [1–3]. Biofacies often correlate lithofacies in carbonate sediments due to the fact that organisms usually produce typical lithofacies and substrates [4–6]. Water energy, depth, photic zone, and basin configuration are the main factors controlling organic productivity and carbonate deposition [7,8].
Carbonates before skeletons: A database approach
2020, Earth-Science ReviewsCitation Excerpt :The sheer volume of dolomite in the rock record compared with the paucity of modern dolomite, leads to an apparent paradox, the “dolomite problem” (Van Tuyl, 1915; Fairbridge, 1957; Hsu, 1966; Hsu and Siegenthaler, 1969; Given and Wilkinson, 1987; Arvidson and Mackenzie, 1999; Holland and Zimmermann, 2000). Observations of when and where modern dolomite does form—in low oxygen and low sulfate environments, associated with organic material or microbial activity (De Deckker and Last, 1988; Vasconcelos and Mckenzie, 1997; Warthmann et al., 2000; Wright, 2000; Roberts et al., 2013)—led to the suggestion that substantially different seawater chemistry during the Archean and Proterozoic eons allowed precipitation of dolomite as a primary or early secondary chemical sediment (Fairchild, 1980; Baker and Kastner, 1981; Kastner, 1983; Fairchild et al., 1991; Burns et al., 2000; van Smeerdijk Hood and Wallace, 2018). Supporting this suggestion, many workers have observed that the character of some Precambrian dolomite is distinct from most Phanerozoic counterparts (Plate 6, Fig. 8).