1
The Solid Phase of Marine Sediments
24
1.5
Problems
Problem 1
Is there any correlation between the distribution
of calcareous and siliceous sediments, terrigenous
sediments and deep-sea clay?
Problem 2
Explain the distribution pattern of clay minerals
kaolinite, illite, chlorite and smectite in the world
ocean. Why should be illite more common in the
North Atlantic than in the South Atlantic?
Problem 3
What are the reasons why sediments of the
Atlantic Ocean are thicker along the continental
margin than near the mid-Atlantic ridge?
Problem 4
What causes the variability of sedimentation
rates?
Problem 5
Summarize and explain the main aspects of deep
sea sediment classification.
References
Berger, W.H., 1974. Deep-sea sedimentation. In: Burk,
C.A. and Drake, C.L. (eds) The geology of
continental margins. Springer Verlag, Berlin,
Heidelberg, New York, pp 213-241.
Berger, W.H., 1976. Biogenic deep sea sediments: Production, preservation and interpretation. In: Riley,
J.P. and Chester, R. (eds) Chemical Oceanography,
Academic, 5. Press, London, NY, San Francisco, pp
266-388.
Berger, W.H. and Herguera, J.C., 1991. Reading the sedimentary record of the ocean’s productivity. Pimary
productivity and biogeochemical cycles in the sea. In:
Falkowski, P.G. and Woodhead, E.D. (eds) Plenum
Press, New York, London, pp 455-486.
Biscay, P.E., 1965. Mineraloy and sedimentation of recent
deep-sea clay in the Atlantic Ocean and adjacent seas
and oceans. Geol. Soc. Am. Bull., 76: 803-832.
Bruns, P. and Hass, H.C., 1999. On the determination of
sediment accumulation rates. GeoResearch Forum Vol.
5, Trans Tech Publication, Zürich, 244 pp.
Chamley, H., 1989. Clay sedimentology. Springer Verlag,
Berlin, Heidelberg, New York, 623 pp.
Davies, T.A. and Gorsline, D.S., 1976. Oceanic sediments
and sedimentary processes. In: Riley, J.P. and Chester,
R. (eds) Chemical oceanography, 5. Academic Press,
London, New York, San Francisco, pp 1-80.
Dean, W.E., Leinen, M. and Stow, D.A.V., 1985. Classification of deep-sea fine-grained sediments. Journal of
Sediment Petrology, 55: 250-256.
Elderfield, H., 1976. Hydrogeneous material in marine
sediments; excluding manganese nodules. In: Riley,
J.P. and Chester, R. (eds) Chemical Oceanography, 5.
Academic Press, London, New York, San Francisco,
pp 137-215.
Emery, K.O., 1968. Relict sediments on continental
shelves of the world. Bull. Am. Assoc. Petrol.
Geologists, 52: 445-464.
Fabricius, F., 1977. Origin of marine ooids and
grapestones. Contributions to sedimentology, 7,
Schweizerbart, Stuttgart, 113 pp.
Flügel, E., 1978. Mikrofazielle Untersuchungsmethoden
von Kalken. Springer Verlag, Berlin, Heidelberg, New
York, 454 pp.
Flügel, E., 2004. Microfacies of carbonate rocks:
analysis, interpretation and application. Springer
Verlag, Berlin, Heidelberg, New York, 976 pp.
Folk, R.L., 1980. Petrology of sedimentary rocks.
Hemphill. Publ. Co., Austin, 182 pp.
Garrels, R.M. and Mackenzie, F.T., 1971. Evolution of
sedimentary rocks. Norton & Co, New York, 397 pp.
Gibbs, R.J., 1977. Transport phase of transition metals in
the Amazon and Yukon rivers. Geological Society of
America Bulletin, 88: 829-843.
Gingele, F., 1992. Zur klimaabhängigen Bildung biogener
und terrigener Sedimente und ihre Veränderungen
durch die Frühdiagnese im zentralen und östlichen
Südatlantic. Berichte, Fachbereich Geowissenschaften,
Universität Bremen, 85, 202 pp.
Velocity of sedimentation or deposition of
material through time, i.e. sedimentation rate in
this chapter is given solely as millimeter per 1000
years (mm/1000 y or mm ky -1 ). This describes the
vertical thickness of sediment deposited in a
certain period of time. It assumes more or less
linear and constant processes – not regarding any
inconsistency hiatuses – between two datum
levels and is, therefore, often referred to as linear
sedimentation rate. This term has to be distinguished from mass accumulation rate which
refers to a sediment mass deposited in a certain
period of time within a defined area, usually
given as grams per centimeter square per 1000
years (g cm -2 ky -1 ). For further reading see Bruns
and Hass (1999).
The Solid Phase of Marine Sediments
24
1.5
Problems
Problem 1
Is there any correlation between the distribution
of calcareous and siliceous sediments, terrigenous
sediments and deep-sea clay?
Problem 2
Explain the distribution pattern of clay minerals
kaolinite, illite, chlorite and smectite in the world
ocean. Why should be illite more common in the
North Atlantic than in the South Atlantic?
Problem 3
What are the reasons why sediments of the
Atlantic Ocean are thicker along the continental
margin than near the mid-Atlantic ridge?
Problem 4
What causes the variability of sedimentation
rates?
Problem 5
Summarize and explain the main aspects of deep
sea sediment classification.
References
Berger, W.H., 1974. Deep-sea sedimentation. In: Burk,
C.A. and Drake, C.L. (eds) The geology of
continental margins. Springer Verlag, Berlin,
Heidelberg, New York, pp 213-241.
Berger, W.H., 1976. Biogenic deep sea sediments: Production, preservation and interpretation. In: Riley,
J.P. and Chester, R. (eds) Chemical Oceanography,
Academic, 5. Press, London, NY, San Francisco, pp
266-388.
Berger, W.H. and Herguera, J.C., 1991. Reading the sedimentary record of the ocean’s productivity. Pimary
productivity and biogeochemical cycles in the sea. In:
Falkowski, P.G. and Woodhead, E.D. (eds) Plenum
Press, New York, London, pp 455-486.
Biscay, P.E., 1965. Mineraloy and sedimentation of recent
deep-sea clay in the Atlantic Ocean and adjacent seas
and oceans. Geol. Soc. Am. Bull., 76: 803-832.
Bruns, P. and Hass, H.C., 1999. On the determination of
sediment accumulation rates. GeoResearch Forum Vol.
5, Trans Tech Publication, Zürich, 244 pp.
Chamley, H., 1989. Clay sedimentology. Springer Verlag,
Berlin, Heidelberg, New York, 623 pp.
Davies, T.A. and Gorsline, D.S., 1976. Oceanic sediments
and sedimentary processes. In: Riley, J.P. and Chester,
R. (eds) Chemical oceanography, 5. Academic Press,
London, New York, San Francisco, pp 1-80.
Dean, W.E., Leinen, M. and Stow, D.A.V., 1985. Classification of deep-sea fine-grained sediments. Journal of
Sediment Petrology, 55: 250-256.
Elderfield, H., 1976. Hydrogeneous material in marine
sediments; excluding manganese nodules. In: Riley,
J.P. and Chester, R. (eds) Chemical Oceanography, 5.
Academic Press, London, New York, San Francisco,
pp 137-215.
Emery, K.O., 1968. Relict sediments on continental
shelves of the world. Bull. Am. Assoc. Petrol.
Geologists, 52: 445-464.
Fabricius, F., 1977. Origin of marine ooids and
grapestones. Contributions to sedimentology, 7,
Schweizerbart, Stuttgart, 113 pp.
Flügel, E., 1978. Mikrofazielle Untersuchungsmethoden
von Kalken. Springer Verlag, Berlin, Heidelberg, New
York, 454 pp.
Flügel, E., 2004. Microfacies of carbonate rocks:
analysis, interpretation and application. Springer
Verlag, Berlin, Heidelberg, New York, 976 pp.
Folk, R.L., 1980. Petrology of sedimentary rocks.
Hemphill. Publ. Co., Austin, 182 pp.
Garrels, R.M. and Mackenzie, F.T., 1971. Evolution of
sedimentary rocks. Norton & Co, New York, 397 pp.
Gibbs, R.J., 1977. Transport phase of transition metals in
the Amazon and Yukon rivers. Geological Society of
America Bulletin, 88: 829-843.
Gingele, F., 1992. Zur klimaabhängigen Bildung biogener
und terrigener Sedimente und ihre Veränderungen
durch die Frühdiagnese im zentralen und östlichen
Südatlantic. Berichte, Fachbereich Geowissenschaften,
Universität Bremen, 85, 202 pp.
Velocity of sedimentation or deposition of
material through time, i.e. sedimentation rate in
this chapter is given solely as millimeter per 1000
years (mm/1000 y or mm ky -1 ). This describes the
vertical thickness of sediment deposited in a
certain period of time. It assumes more or less
linear and constant processes – not regarding any
inconsistency hiatuses – between two datum
levels and is, therefore, often referred to as linear
sedimentation rate. This term has to be distinguished from mass accumulation rate which
refers to a sediment mass deposited in a certain
period of time within a defined area, usually
given as grams per centimeter square per 1000
years (g cm -2 ky -1 ). For further reading see Bruns
and Hass (1999).