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Phytoplankton: below the salt at the global table

Published online by Cambridge University Press:  19 May 2016

Helen Tappan*
Affiliation:
Department of Earth and Space Sciences and Center for the Study of Evolution and Origin of Life, University of California Los Angeles, Los Angeles 90024

Abstract

The abundance and diversity of marine phytoplankton and the geologic timing of its major innovations and extinctions show a broad but inverse relationship to stages of terrestrial plant evolution. Successively, the first appearance of land plants, and the later major increases in global live terrestrial biomass and dead biomass in the form of plant litter, peat, coal, and soil humus, increased the retention on land of carbon, nitrogen, and phosphorus, and decreased the amount of these nutrients that was transported by rivers to the seas. Each major increase in terrestrial nutrient retention resulted in extensive changes in the marine ecosystem, as it adapted to the new conditions. From its time of origin in the early Paleozoic, the terrestrial biota figuratively occupied the position at the head of the table, and only the unutilized nutrient excess trickled down to the oceanic phytoplankton and its dependent food web.

Type
Research Article
Copyright
Copyright © The Paleontological Society 

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References

Ajtay, G. L., Ketner, P. and Duvigneaud, P. 1979. Terrestrial primary production and phytomass, p. 129181. In Bolin, B. et al. (eds.), The Global Carbon Cycle, Workshop on the Carbon Cycle, Ratzeburg, Germany, 1977. John Wiley & Sons, New York.Google Scholar
Berner, R. A. 1982. Burial of organic carbon and pyrite sulfur in the modern ocean: its geochemical and environmental significance. American Journal of Science, 282:451473.CrossRefGoogle Scholar
Bramlette, M. N. 1965. Massive extinctions in biota at the end of Mesozoic time. Science, 148:16961699.CrossRefGoogle ScholarPubMed
Broecker, W. S. 1973. Factors controlling CO2 content in the oceans and atmosphere, p. 3250. In Woodwell, G. M. and Pecan, E. V. (eds.), Carbon and the Biosphere, Proceedings of the 24th Brookhaven Symposium in Biology, Upton, New York.Google Scholar
Costain, T. B. 1957. Below the Salt. Doubleday & Company, Inc., Garden City, N.Y., 480 p.Google Scholar
Fischer, A. G. and Arthur, M. A. 1977. Secular variations in the pelagic realm, p. 1950. In Deep water Carbonate Environments, Society of Economic Paleontologists and Mineralogists, Special Publication 26.CrossRefGoogle Scholar
Hallock, P. 1982. Evolution and extinction in larger foraminifera. Third North American Paleontological Convention, 1982, Proceedings, I:221225.Google Scholar
Jennings, J. C. Jr., Gordon, L. I. and Nelson, D. M. 1984. Nutrient depletion indicates high primary productivity in the Weddell Sea. Nature, 309:5154.CrossRefGoogle Scholar
Keith, M. L. 1982. Violent volcanism, stagnant oceans and some inferences regarding petroleum, strata-bound ores and mass extinctions. Geochimica et Cosmochimica Acta, 46:26212637.CrossRefGoogle Scholar
Kerr, R. A. 1983. Are the ocean's deserts blooming? Science, 220:397398.CrossRefGoogle ScholarPubMed
McElroy, M. B. 1983. Marine biological controls on atmospheric CO2 and climate. Nature, 302:328329.CrossRefGoogle Scholar
Mackenzie, F. T. 1981. Global carbon cycle: some minor sinks for CO2 , p. 360384. In Flux of Organic Carbon by Rivers to the Ocean, Report of Workshop Woods Hole, Massachusetts, Sept. 21–25, 1980, Carbon Dioxide Effects Research and Assessment Program 016, U.S. Department of Energy, National Technical Information Service, U.S. Department of Commerce, Springfield, Virginia.Google Scholar
Meentemeyer, V., Box, E. O. and Thompson, R. 1982. World patterns and amounts of terrestrial plant litter production. BioScience, 32(2):125128.CrossRefGoogle Scholar
Meybeck, M. 1982. Carbon, nitrogen, and phosphorus transport by world oceans. American Journal of Science, 282:401450.CrossRefGoogle Scholar
Mooney, H. A. and Gulmon, S. L. 1982. Constraints on leaf structure and function in reference to herbivory. BioScience, 32:198201, 204–206.CrossRefGoogle Scholar
Mopper, K. and Degens, E. T. 1979. Organic carbon in the ocean: nature and cycling, p. 293316. In Bolin, B. et al. (eds.), The Global Carbon Cycle, Workshop on the Carbon Cycle, Ratzeburg, Germany, 1977. John Wiley & Sons, New York.Google Scholar
Olson, J. S. 1985. Cenozoic fluctuations in biotic parts of the global carbon cycle, p. 377396. In Sundquist, E. T. and Broecker, W. S. (eds.), The Carbon Cycle and Atmospheric CO2: Natural Variations Archean to Present. Geophysical Monograph 32, American Geophysical Union, Washington, D.C. Google Scholar
Platt, T., Subba Rao, D. V. and Irwin, B. 1983. Photosynthesis of picoplankton in the oligotrophic ocean. Nature, 301:702704.CrossRefGoogle Scholar
Post, W. M., Pastor, J., Zinke, P. J. and Stangenberger, A. G. 1985. Global patterns of soil nitrogen storage. Nature, 317:613616.CrossRefGoogle Scholar
Tappan, H. 1968. Primary production, isotopes, extinctions and the atmosphere. Palaeogeography, Palaeoclimatology, Palaeoecology, 4:187210.CrossRefGoogle Scholar
Tappan, H. 1971. Microplankton, ecological succession and evolution. Proceedings of the North American Paleontological Convention, 1969, Part H:10581103.Google Scholar
Tappan, H. 1979. Protistan evolution and extinction at the Cretaceous/Tertiary boundary, p. 1321. In Christensen, W. K. and Birkelund, T. (eds.), Cretaceous–Tertiary Boundary Events Symposium, II. Proceedings, University of Copenhagen.Google Scholar
Tappan, H. 1980. The Paleobiology of Plant Protists. W. H. Freeman and Co., San Francisco, xxiv + 1028 p.Google Scholar
Tappan, H. 1982. Extinction or survival: selectivity and causes of Phanerozoic crises. Geological Soceity of America Special Paper, 190:265276.CrossRefGoogle Scholar
Tappan, H. and Loeblich, A. R. Jr. 1971. Geobiologic implications of fossil phytoplankton evolution and time-space distribution. Geological Society of America Special Paper, 127:247340.CrossRefGoogle Scholar
Tappan, H. and Loeblich, A. R. Jr. 1972. Fluctuating rates of protistan evolution, diversification and extinction. International Geological Congress, 24th, Montreal, 1972, Section 7, Paleontology:205213.Google Scholar
Tappan, H. and Loeblich, A. R. Jr. 1973a. Evolution of the oceanic plankton. Earth-Science Reviews, 9:207240.CrossRefGoogle Scholar
Tappan, H. and Loeblich, A. R. Jr. 1973b. Smaller protistan evidence and explanation of the Permian-Triassic crisis, p. 465480. In Logan, A. and Hills, L. V. (eds.), The Permian and Triassic System and their Mutual Boundary. Canadian Society of Petroleum Geology, Calgary.Google Scholar
Tappan, H. and Loeblich, A. R. Jr. 1982. Fluctuations in marine productivity through time: inverse relation with terrestrial floras. American Association of Petroleum Geologists, Book of Abstracts, Annual Convention June 27–30, 1982, Calgary:117.Google Scholar
Taylor, W. P. 1934. Significance of extreme or intermittent conditions in distribution of species and management of natural resources, with a restatement of Liebig's Law of Minimum. Ecology, 15:374379.CrossRefGoogle Scholar
Wolfe, J. A. 1985. Distribution of major vegetational types during the Tertiary, p. 357375. In Sundquist, E. T. and Broecker, W. S. (eds.), The Carbon Cycle and Atmospheric CO2: Natural Variations Archean to Present. Geophysical Monograph 32, American Geophysical Union, Washington, D.C. Google Scholar
Wood, T., Bormann, F. H. and Voigt, G. K. 1984. Phosphorus cycling in a northern hardwood forest: biological and chemical control. Science, 223:391393.CrossRefGoogle Scholar
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