Marine Geochemistry 1 Reference: Schulz and Zabel

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Presentation transcript:

Marine Geochemistry 1 Reference: Schulz and Zabel Marine Geochemistry Springer, New York 2000 453 pp. ISBN 3-540-66-453-X

The Organic Carbon Cycle Divided into two parts : 1. Biological cycle 2. Geological cycle

Biological cycle Photosynthesis in surface waters of oceans or lakes organic matter from carbon dioxide organic matter from bicarbonate Ends with metabolic or chemical oxidation of decayed biomass to carbon dioxide

Geological cycle Incorporation of biogenic organic matter into sediments and soils Leads to the formation of natural gas, petroleum and coal or metamorphic forms of carbon

Organic matter accumulation in sediments In the fossil record: Dark colored sediments periods of time favorable to organic matter accumulation White or red colored sediments or rocks devoid of organic matter

Causes leading to deposition of massive organic-matter rocks Good Preservation Sluggish circulation in the deep ocean Shallow epicontinental seas accompained by water column stratification Good Productivity High primary productivity in a dynamic system

Primary Production Photosynthetic plankton produce 20 to 30 billions tons/year of carbon fixation is not evenly distributed on the oceans but display zones of: Higher activity on continental margins Lower activity within the central ocean gyres

Export to the Ocean Bottom Of the total biomass formed only a very small portion reaches the underlying sea floor and is ultimately buried a sediment Most of the organic matter enters the biological food web and it is respired or used for new biomass production

Sedimentation Rate vs. Organic Matter Burial Oxic open-ocean conditions: 2X increase in organic carbon content for every 10X increase in sedimentation rate in marine sediments Anoxic conditions: no change in organic carbon content over a wide range of sedimentation rates

Organic Carbon Content of Marine Sediments Mean organic carbon content : 0.3% with a median value of 0.1% (data from deep sea drilling) Varies over several hundreds of magnitude

Organic Carbon Content of Marine Sediments Depends on: extend of supply of organic matter preservation conditions dilution by mineral matter

Chemical Composition of Biomass Chemical nature of biomass is commonly described by its elemental composition Marine phytoplankton Redfield et al. (1963) ratio C:N:P = 106:16:1 Ratio changes drastically : food chain processes early digenetic processes

Chemical Composition of Biomass Chemical composition can also be confined to a limited number of compound classes Their proportions will vary in the different groups of organisms (Romankevitch, 1984)

Principle of Selective Preservation Organic compounds and compound classes: differ in their potential to be preserved in sediments differ in their potential survive early diagenesis

Principle of Selective Preservation Low Preservation Potential = easily hydrolyzed Water-soluble organic compounds Organic macromolecules High Preservation Potential = low solubility in water Lipids Hydrolysis resistant molecules

Biological Markers Molecules with high degree of structural complexity provide the possibility of relating a certain product to a specific precursor EXAMPLE: 24-methylenecholesterol and dinoserol are preferentially biosynthesized by diatoms and dinoflagellates (Volkman et al., 1998)

Marine vs. Terrigenous Organic Matter Variations in marine and terrigenous organic matter proportions important for: paleoclimatic studies paleoceanographic studies

Parameters used to assess the organic matter sources Carbon / Nitrogen Ratio 10 in marine / 20 in terrigenous Hydrogen Indices (mg HC/g TOC) 150 in marine / 300-800 in terrigenous Stable Carbon Isotope Rations d13C = -27o/oo in marine / - 7o/oo in terrigenous

Molecular Paleo-Seawater Temperature and Climate Indicators Biosynthesis of Long-Chain Alkenones in the microalgae Class Haptophyceae depends on the water temperature during growth Coccolithoophorids belong to this class !