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Chapter 4 Marine Sedimentation ©2003 Jones and Bartlett Publishers.

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Presentation on theme: "Chapter 4 Marine Sedimentation ©2003 Jones and Bartlett Publishers."— Presentation transcript:

1 Chapter 4 Marine Sedimentation ©2003 Jones and Bartlett Publishers

2 EXAM and QUIZ #1 In 2 weeks, September 30. Exam on chapters 1-5 in Pinet’s text h length  Multiple choice, short answer.  Study material at end of chapters:  keywords  Review of basic concepts questions  Critical thinking essays questions  Discovering with numbers questions Quiz questions taken directly from laboratory exercises

3 Classification of marine sediments based upon size. SedimentTypeDiameter (mm) Gravel Boulder>256 Cobble Pebble4-64 Granule2-4 Sand Very coarse1-2 Coarse0.5-1 Medium Fine Very fine Mud (silt & clay) Colloid <0.0002

4 Classification of marine sediments based upon Mode of Formation. Terrigenous: Sands and mud produced by weathering and erosion of rocks on land. Biogenic : CaCO 3 (calcium carbonate) and SiO 2 (silica) muds and oozes composed of hard parts of organisms. Authigenic : formed by precipitation of minerals in seawater (Manganese (Mn) and Phosphorus (P) nodules). Volcanogenic : ejected from volcanoes (ash). Cosmogenous : pieces of meteorites that survive trip thru atmosphere.

5 Sediment Sampling Methods

6 Sediment Sampling Methods: CORING- preserves deep stratigraphy, or layering.

7 Hjulstrom’s Diagram graphs the relationship between particle size and energy for erosion, transportation and deposition.

8 Shelf Versus Basin Depths

9 Worldwide distribution of recent shelf sediments by composition is strongly related to latitude and climate. Calcareous biogenic sediments dominate tropical shelves. River-supplied sands and muds dominate temperate shelves. Glacial till and ice-rafted sediments dominate polar shelves.

10 Shelf Sedimentation Model

11 Shelf sedimentation is strongly controlled by tides, waves and currents, but their influence decreases with water depth.

12 Sea-level rise and fall



15 Geologic controls of continental shelf sedimentation must be considered in terms of a time scales. For a time scale up to 1000 (10 3 ) years, sedimentation controlled by: –Waves –Wind-induced currents –Tidal currents (all related to water depth)

16 Million-year time scale. For a time scale up to 1,000,000 (10 6 ) years, sedimentation controlled by: –Glaciation and its effect on position of coastline

17 Relict Sediment: deposited in the past under conditions that are no longer present.

18 Shelf Sedimentation Model

19 Hundred-million year time scale… For a time frame up to 100,000,000 (10 8 ) years, sedimentation controlled by: –Plate tectonics and its effect on type of margin.

20 Plate tectonics & sedimentation on shelf

21 If influx of terrigenous sediment is low and the water is warm, carbonate sediments and reefs will dominate. Carbonate Shelves

22 Passive (Atlantic) vs. Active (Pacific) Type Margins. Atlantic (passive) type margin:  Passive boundary  Long history of sedimentation  Sedimentation rate = subsidence rate  Broad, smooth continental shelf Pacific (active) type margin:  Convergent boundary  Sedimentary layers compressed and deformed  Volcanic sediment  Seismic activity causes slumps and slides of sediments to deep-sea trenches.

23 Passive (Atlantic) vs. Active (Pacific) Type Margins.

24 Passive (Atlantic) Type Margin.

25 Active (Pacific) Type Margin.

26 Deep-sea Sedimentation The Deep sea has two main sources of sediment: 1.External- terrigenous material transported to oceans via rivers and wind, 2.internal-biogenic and authigenic from the sea.

27 River transport of sediment

28 Wind transport of sediment

29 Deep-sea sedimentation processes

30 Bulk emplacement: –Slumps: sediment transport by mass with little deformation or folding of layers –Slurries: debris flows and mud flows- destroy any previous bedding or layering. Turbidity currents –Deep-Sea canyons formed by these processes. –Ice Rafting Polar latitudes, debris from melting icebergs. Glacial marine sediment Modes of sedimentation in deep sea

31 Bulk Emplacement: Slumps and Slurries

32 Bulk Emplacement: Ice Rafting

33 Deep-sea sedimentation processes

34 Modes of sedimentation in deep sea Pelagic sedimentation: –Pelagic muds: Inorganic red or brown clays and silt –Fine-grained ( – mm) –Quartz, feldspar, kaolinite & chlorite minerals –Terrigenous, wind- bourne, cosmogenous source –Kaolinite in tropical & subtropical waters –Chlorite in temperate & subpolar –Dominate below waters with little planktonic production.

35 Pelagic sedimentation: –Pelagic muds: biogenic oozes –>30% of debris from planktonic organisms –Calcareous oozes (CaCO 3 ) »Shells of foraminifera & pteropods (zooplankton) and coccolithophorids (phytoplankton). »Accumulate on seafloor above CCD. »Forms hard limestone under pressure –Siliceous oozes (SiO 2 ) »Shells of radiolaria (zooplankton) and diatoms (phytoplankton). »Accumulate on seafloor below CCD. »Accumulate below regions of high diatom production (equator, poles, upwelling areas) Modes of sedimentation in deep sea

36 CaCO 3 (calcite) is a solid material produced by biological or abiological processes in seawater: Ca 2+ + CO 3 2- CaCO 3 –The reaction can go both ways, depending on the pH, pressure. –When the seawater is undersaturated with respect to CaCO 3, calcite will dissolve: Ca 2+ + CO 3 2- CaCO 3 –But when seawater is saturated with respect to CaCO 3, calcite will remain in its solid form and not dissolve: Carbonate Chemistry

37 Depth in ocean at which seawater becomes undersaturated with respect to calcite and rate of dissolution of CaCO 3 equals its rate of delivery. –CCD ~ 4500 m (or deeper in regions of high surface productivity). –Depths below CCD: Seawater undersaturated w.r.t. CaCO 3 Chemical properties of deep water dissolves calcite CaCO 3 oozes less common than SiO 2 oozes. –Depths above CCD: Seawater saturated w.r.t. CaCO 3 CaCO 3 remains intact. CaCO 3 oozes more common than SiO 2 oozes. Question: Why is the CCD sometimes referred to as the “snow-line”? Carbonate Compensation Depth, CCD

38 Foraminifera (zooplankton with CaCO 3 shell) Size ~ 1mm

39 Diatoms (phytoplankton with SiO 2 shell) Size ~ 0.01mm

40 Deep-sea Sediment Distribution

41 TYPE COMPO- SITION ATLANTIC (%) PACIFIC (%) INDIAN (%) GLOBAL (%) Foram. oozeCarbonate Pteropod ooze Carbonate Diatom oozeSilica Radiolarian ooze Silica Red clayAluminum silicate

42 Formed by chemical or biochemical reactions on ocean floor Nodules of ferromanganese (Fe and Mn) or phosphorite (P). Concentric layers of metal oxides accrete on particles over millions of years (1-4 mm per 10 6 y). Contain economically important metals Cu, Zn, Co and Pb. (but too expensive to harvest). Origin uncertain (biological?) Authigenic deposits

43 Ferromanganese nodules Floor of South Pacific Ocean. Nodule size 1-5 cm diameter

44 Ferromanganese nodules Cross-section

45 Broad-scale layering of sediments that cover the basaltic crust. Strongly influenced by sea-floor spreading and direction of spreading centers with relation to latitude. Deep-sea stratigraphy


47 The Atlantic basin contains a “two-layer- cake” stratigraphy–a thick basal layer of carbonate ooze overlain by a layer of mud.

48 Pacific plate moves across latitudes…

49 The Pacific basin contains a “five-layer-cake” stratigraphy, because unlike the Atlantic its sea floor as it spreads crosses the equator where the CCD is lowered to the ocean bottom.

50 2-5Geophysical Surveying END OF LECTURE 3

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