Marine Sedimentation
• Sediment Defined:
• unconsolidated organic and inorganic particles that accumulate on the ocean floor
• originate from numerous sources
– weathering and
erosion of the continents
– volcanic eruptions
– biological activity
– chemical processes
within the oceanic crust and seawater
– impacts of extra-terrestrial objects
• classified by size according to the Wentworth scale
• grain size indicates condition under which sediment is deposited
– high energy environments characteristically yield sediments larger
in size
– small particles (silts, clays) indicate low energy environments
• considered well-sorted if most particles appear in the
same size classification
• poorly sorted sediments comprised of multiple sizes
• sediment maturity is indicated by several factors
– decreased silt and clay content
– increased sorting
– increased rounding of grains, as a result of weathering and abrasion
• particle transport is controlled by grain size and velocity
of transporting medium
•
• Average grain size reflects
the energy of
the depositional
environment.
• Hjulstrom’s
Diagram graphs the
relationship
between particle size
and energy for erosion,
transportation
and deposition.
4-1 Sediment in the Sea
Classification of marine sediments can be based upon size or origin.
• Size classification divides sediment by grain size into gravel, sand and clay.
– Mud is a mixture of silt
and clay.
• Origin classification divides sediment into
five categories: Terrigenous sediments, Biogenic sediments, Authigenic sediments,
Volcanogenic sediments and Cosmogenic sediments.
4-1 Sediment in the Sea
• Terrigenous (or Lithogenous Sediments):
• derived from weathering of rocks at or above sea level (e.g., continents, islands)
• two distinct chemical compositions
– ferromagnesian, or iron-magnesium bearing minerals
– non-ferromagnesian minerals – e.g., quartz, feldspar, micas
• largest deposits on continental margins (less than 40% reach abyssal plains)
• transported by water, wind, gravity, and ice
• transported as dissolved and suspended loads in rivers,
waves, longshore currents
• (LANDSAT images adapted from Geospace Images catalog).
• sediment delivered to the open-ocean by wind activity as particulate
matter (dust)
• primary dust source is
deserts in Asia and North Africa
• comprise much of the fine-grained deposits in remote open-ocean areas (red clays)
• volcanic eruptions contribute ash to the atmosphere which
settles within the oceans
• sediment also transported to the open-ocean by gravity-driven turbidity currents
• dense 'slurries' of suspended sediment moved as turbulent underflows
• typically initiated by storm activity or earthquakes
– first identified during 1929 Grand Banks earthquake
– seismic activity triggered turbidity current which severed telegraph lines
• initial flow often confined to submarine canyons of the continental shelf and slope
• form deep-sea fans where the mouth of the canyon opens onto the continental rise
20 m s-1
near Grand
Banks
• boulder to clay size particles also eroded and transported to oceans via glacial ice
• glacier termination in circum-polar oceans
results in calving and iceberg formation
• as ice (or icebergs) melt, entrained material is deposited on the ocean floor
• termed 'ice-rafted' debris
• Biogenous Sediments:
• composed primarily of marine microfossil remains
• shells of one-celled plants and animals, skeletal fragments
• median grain size typically less than 0.005 mm (i.e., silt or clay size particles)
• characterized as CaCO3 (calcium carbonate) or SiO2 (silica) dominated systems
• sediment with biogenic component less than 30% termed calcareous, siliceous clay
• calcareous or siliceous 'oozes' if biogenic component greater than 30%
• siliceous oozes (primarily diatom oozes) cover ~15% of the ocean floor
– distribution mirrors
regions of high productivity
– common at high latitudes, and zones of
upwelling
– radiolarian oozes more
common in equatorial
regions
• calcareous oozes (foraminifera, coccolithophores) cover ~50% of the ocean floor
– distribution controlled largely by dissolution processes
– cold, deep waters are undersaturated with respect to CaCO3
– deep water is slightly acidic as a result of elevated CO2 concentrations
– solubility of CaCO3 also increases in colder water and at greater pressures
– CaCO3 therefore readily dissolved at depth
• level below which no CaCO3 is preserved is the 'carbonate compensation depth'
• typically occurs at a depth of 3000 to 4000 m
•
Microfossils in
Paleoclimatology/
Paleoceanography
• Dissolution Calcium carbonate dissolves better in colder water, in acidic
water, and at higher pressures. In the deep ocean, all three of these conditions exist. Therefore, the
dissolution rate of calcium carbonate increases greatly below the thermocline. This change in dissolution
rate is called the lysocline. Below the lysocline, more and more calcium carbonate dissolves,
until eventually, there is none left. The depth below which all calcium carbonate is dissolved is called the carbonate
compensation depth or CCD.
• Hydrogenous (or Authigenic) Sediments:
• produced by chemical processes in seawater
• essentially solid chemical precipitates of several common
forms
• non-biogenous carbonates
– form in surface waters supersaturated with calcium carbonate
– common forms include short aragonite crystals and oolites
• phosphorites
– phosphate crusts (containing greater than 30% P2O5) occurring as nodules
– formed as large quantities of organic phosphorous settle to the
ocean floor
– unoxidized material is transformed to phosphorite deposits
– found on continental shelf and upper slope in regions of high productivity
• manganese
nodules
– surficial
deposits of manganese,
iron, copper,
cobalt, and
nickel
– accumulate
only in areas
of low sedimentation
rate (e.g., the
Pacific)
– develop
extremely
slowly (1 to 10
mm/million years)
•
• The term evaporites is used for all deposits, such
as salt deposits, mainly
chemical sediments that are composed of minerals
that precipitated from saline solutions
concentrated by
evaporation. Evaporite deposits are composed
dominantly of varying proportions of halite (rock
salt) (NaCl), anhydrite
(CaSo4) and gypsum (CaSo4.2H2O). Evaporites
may be classified as chlorides, sulfates or
carbonates on the basis of
their chemical composition (Tucker, 1991).
evaporites ('salt'
deposits')
occur in regions
of enhanced
evaporation
(e.g., marginal
seas)
evaporative
process removes
water and leaves
a salty brine
e.g.,
Mediterranean
'Salinity Crisis'
between 5 and 6
million years
ago
• Cosmogenous Sediments:
• sediments derived from extraterrestrial materials
• includes micrometeorites
and tektites
• tektites result from
collisions with extraterrestrial materials
– fragments of earth's
crust melt and spray
outward from impact
crater
– crustal material re-
melts as it falls back
through the atmosphere
– forms 'glassy' tektites
• Distribution of Marine Sediments:
• sediments thickest along continental margins, thin at mid-ocean ridges
• coastlines
– dominated by river-borne and wave reworked terrigenous sediments
– shelf and slope characterized by turbidites and authigenic carbonate deposits
– glacial deposits and ice-rafted debris common at high latitudes
– high input of terrigenous sediments 'dilutes' biogenous components
• deep-sea (pelagic) basins
– abyssal clays (wind blown deposits) common
– lower quantities of biogenic material
• distribution of biogenous sediments dependent upon three primary factors
– production in surface waters
– dissolution in deep waters – dilution by other sediments
types
• high productivity in zones of upwelling and nutrient-rich high latitude waters
• calcareous oozes more common in warmer or
shallower water
• siliceous oozes more
common in colder or deeper water
• terrigenous sedimentation rates range from ~1 mm to 10's cm/1000 years
• biogenous sedimentation rates typically ~1 cm/1000
years
Nearshore sediments, turbidites:Up to
km/my (kilometers/million years)
Hemipelagic deposits: Tens to hundreds
of m/myDrift deposits40-400 m/my
Mid-latitude eolian deposits: 3 to 10
m/my
Ice rafted material: 10+ m/my
Carbonate oozes: Up to 50 m/my
Siliceous oozes: Up to 10 m/my
Hydrothermal deposits: (off ridge
axes)About 0.5 m/my
Hydrogenous sediments: Rarely exceed
0.2 m/my
Ferromanganese nodules: 0.0002 to
0.005 m/my (0.2 to 5 mm/my)
Shelf sedimentation is strongly controlled by tides, waves and currents, but their influence decreases with depth.
• Shoreline turbulence prevents small particles from settling and transports them seaward where they
are deposited in deeper water.
• Particle size decreases seaward for recent sediments.
• Past fluctuations of sea level has stranded coarse sediment (relict sediment) across the shelf including
most areas where only fine sediments are deposited today.
4-2 Sedimentation in the Ocean
Geologic controls of continental shelf sedimentation must be considered in terms of a time frame.
• For a time frame up to 1000 years, waves, currents and tides control sedimentation.
• For a time frame up to 1,000,000 years, sea level lowered by glaciation controlled sedimentation and caused rivers to
deposit their sediments at the shelf edge and onto the
upper continental slope.
• For a time frame up to 100,000,000 years, plate tectonics
has determined the type of margin that developed and controlled sedimentation.
4-2 Sedimentation in the Ocean
60% of the
world’s shelves
are covered
with relict
sediments that
were formed
about 15,000 y
BP under a
different energy
regime.
• Gas Methane Hydrates
(Clathrates)
• Hydrates store immense
amounts of methane, with major implications for
energy resources and
climate, but the natural
controls on hydrates and
their impacts on the environment are very
poorly understood
• The worldwide amounts of carbon bound in gas
hydrates is conservatively
estimated to total twice the
amount of carbon to be
found in all known fossil fuels on Earth (USGS).
• Methane bound in hydrates
amounts to approximately 3,000 times the volume of
methane in the
atmosphere.