Pore water evolution during sediment burial from isotopic and mineral chemistry of calcite, dolomite and siderite concretions

Curtis, C. D.; Coleman, Max; Love, Leonard G.

doi:10.1016/0016-7037(86)90085-2

Cited by 228 publications

(136 citation statements)

References 21 publications

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“…The Ca 2+ content of the K4 core has a fairly uniform background level of 5 wt.%, with values of 15-20 wt.% occurring in the concretionary layer (Middelburg, 1990 Curtis et al, 1986) may owe their origin to extremely slow rates of sedimentation (~0.001 cm yr -1 ) in waters with a high primary productivity (Fisher and Wignall, 2001). Larger masses of cement would clearly result during a pause in deposition which allows additional time for increased supply by diffusion and advection.…”

Section: Non Steady State Diagenetic Effectsmentioning

confidence: 99%

Rates of carbonate cementation associated with sulphate reduction in DSDP/ODP sediments: implications for the formation of concretions

Raiswell

Fisher

2004

Chemical Geology

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Abstractduring sulphate depletion over these depth ranges are equivalent to a dispersed phase of approximately 1.5 wt.% CaCO 3 or 3 wt.% dolomite in a compacted sediment. The complete occlusion of sediment porosity observed in concretions with isotopic signatures suggesting carbonate sourced from sulphate reduction therefore requires more time (a depositional hiatus), 1 more rapid sulphate reduction (possibly by anaerobic methane oxidation) and/or the continued transport of isotopically light carbonate to the concretion site after sulphate reduction has ceased.

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Section: Non Steady State Diagenetic Effectsmentioning

confidence: 99%

Rates of carbonate cementation associated with sulphate reduction in DSDP/ODP sediments: implications for the formation of concretions

Raiswell

Fisher

2004

Chemical Geology

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“…8) would be consistent with conditions in fluvial sandstone units with associated carbonaceous materials altered by shallow microbial degradation (e.g. [12]; [13]; [14]). The relative similarities of the oxygen isotope compositions for the shallow calcite cement throughout the fluvial sandstone units suggests that the water in these sandstones were fairly uniform in composition and would be consistent with a fresh water origin.…”

mentioning

confidence: 74%

The Stable Isotope Composition of the Calcite Cement in the Fluvio-Deltaic Reservoir Sandstones of the Lower Acacus Formation, Ghadames (Hamada) Basin, NW Libya

Elfigih¹

2017

International Journal of Petroleum and Petrochemical Engineerin

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“…11.-Geochemical zones in the studied sediments as reconstructed in analogy to modern environments and fossil counterparts (equations in lines 1, 6, 7, 8, and 9 after Whiticar (1996), in lines 2, 3, and 5 after Spears (1989), in line 4 after Canfield and Raiswell (1991), and in line 10 after Raiswell (1987); however, this reaction takes place only if sufficient iron is available). (e.g., Claypool and Kaplan 1974;Curtis et al 1986;Balzer et al 1987;Coleman 1993;Middleton and Nelson 1996;Whiticar 1996; and references therein) and is summarized in Figure 11. The amount of buried organic matter and the sedimentation rate control the vertical extent of these zones.…”

Section: Geochemical Zonesmentioning

confidence: 99%

The Significance of Hiatus Beds in Shallow-Water Mudstones: An Example from the Middle Jurassic of Switzerland

Wetzel

Allia

2000

Journal of Sedimentary Research

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Limestone beds formed in nearly carbonate-free shallow-water mudstones by discontinuous sedimentation and erosion are called hiatus beds. Anaerobic oxidation of organic matter by microbes provided excess alkalinity, inducing carbonate precipitation. A multiphase history of such beds is documented from the Swiss Jurassic by several cementation and dissolution phases. Four cement types occur: micrite as earliest cement (␦ 13 C Ϫ10 to Ϫ20‰), stellate calcite between micrite-cemented parts (␦ 13 C Ϫ5 to Ϫ10‰), fibrous calcite cement in dissolution cavities (␦ 13 C Ͻ Ϫ30‰), and blocky calcite in remaining pores (␦ 13 C Ϫ5‰). Except for the late blocky cement, all cements contain pyrite, indicating carbonate precipitation within the sulfate reduction zone. After early cementation by micrite, the beds moved relatively upwards into a shallower geochemical zone and some even to the seafloor because of erosion. Cavities formed during reburial by dissolution in the upper part of the sulfate reduction zone and in the upper part of the methanogenic zone. Strongly reduced sedimentation rates provided the requisite stable geochemical conditions for at least several thousands of years, which permitted precipitation and dissolution of carbonate by biochemical processes and diffusion. This happened on short-lived swells caused by differential subsidence and rotation along listric faults when basement structures became reactivated during the extensional stress regime from opening of the Tethys. During the Jurassic and Cretaceous breakup of Pangea the shelf area increased, and differential subsidence on these newly formed shelves was the main factor responsible for the observed postPaleozoic maximum in hiatus beds and hiatus concretions.

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Pore water evolution during sediment burial from isotopic and mineral chemistry of calcite, dolomite and siderite concretions

Cited by 228 publications

References 21 publications

Rates of carbonate cementation associated with sulphate reduction in DSDP/ODP sediments: implications for the formation of concretions

Rates of carbonate cementation associated with sulphate reduction in DSDP/ODP sediments: implications for the formation of concretions

The Stable Isotope Composition of the Calcite Cement in the Fluvio-Deltaic Reservoir Sandstones of the Lower Acacus Formation, Ghadames (Hamada) Basin, NW Libya

The Significance of Hiatus Beds in Shallow-Water Mudstones: An Example from the Middle Jurassic of Switzerland

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