By Ruediger Stein

This research of natural carbon accumulation in marine environments starts off with a evaluate of mechanisms controlling natural carbon deposition, focusing on effects from expeditions into Baffin Bay and the Labrador Sea, in addition to the ocean of Japan and the northwest coast of Africa. significant gadgets of the examine have been the reconstruction of adjustments in palaeoceanic variables and the background of palaeoclimates in several environments. The members additionally built extra basic types for natural carbon accumulation and in comparison organic-carbon features derived from varied analytical strategies as a way to achieve the best-fitting interpretation version.

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Additional info for Accumulation of organic carbon in marine sediments: results from the Deep Sea Drilling Project Ocean Drilling Program (DSDP ODP)

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1989). , Fig. 21). Although most modern terrestrial plants belong to the C3 group with 613Corg values in the range of -34 to -24 °/o o (Fig. , grass) may become important occasionally (Smith, 1976; Waples, 1981). Because the source area of the terrigenous organic matter deposited at Site 658 was the Saharan desert, these sediments may contain significant amounts of C4-plant debris. This may also be reflected by relatively high C/N ratios (Fig. , 1983). 5 °/oo, too. From these results it is obvious that none of the methods described above can be used easily to estimate percentages of marine/terrigenous organic carbon.

In a van Krevelen-type diagram, a classification of the organic carbon similar to that based on H/C and O/C ratios is possible (Figs. , 1989a, b). Furthermore, the temperature at which pyrolysis yields the maximum of hydrocarbons (Tmax), can be used as an indicator of the thermal maturity of the kerogen. Immature organic matter has Tmax values of less than 435 °C. (3) Stable carbon isotopes The isotopic composition of organic carbon (613Corg) was measured by means of a Finnigan Delta m a s s spectrometer.

Although most modern terrestrial plants belong to the C3 group with 613Corg values in the range of -34 to -24 °/o o (Fig. , grass) may become important occasionally (Smith, 1976; Waples, 1981). Because the source area of the terrigenous organic matter deposited at Site 658 was the Saharan desert, these sediments may contain significant amounts of C4-plant debris. This may also be reflected by relatively high C/N ratios (Fig. , 1983). 5 °/oo, too. From these results it is obvious that none of the methods described above can be used easily to estimate percentages of marine/terrigenous organic carbon.

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Accumulation of organic carbon in marine sediments: results by Ruediger Stein
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