Hostname: page-component-586b7cd67f-gb8f7 Total loading time: 0 Render date: 2024-11-23T18:57:13.448Z Has data issue: false hasContentIssue false
  • English
  • Français

Segregation and speciation in the Neogene planktonic foraminiferal clade Globoconella

Published online by Cambridge University Press:  08 April 2016

Cynthia E. Schneider  and
James P. Kennett
Cynthia E. Schneider
Affiliation:
Department of Geological Sciences and Marine Science Institute, University of California, Santa Barbara, California 93106. E-mail: [email protected]
James P. Kennett
Affiliation:
Department of Geological Sciences and Marine Science Institute, University of California, Santa Barbara, California 93106. E-mail: [email protected]
Get access Rights & Permissions [Opens in a new window]

Abstract

The origin of the Neogene planktonic foraminifer Globorotalia (Globoconella) pliozea in the subtropical southwest Pacific has been attributed to its isolation resulting from intensification of the Subtropical Divergence (Tasman Front). Oxygen isotopic analyses suggest that, although the Subtropical Divergence may have played a role, the evolution of Gr. (G.) pliozea was facilitated by depth segregation of Gr. (G.) conomiozea morphotypes (low and high conical) during an interval of near-surface warming and increasing thermal gradient. Oxygen isotopic analyses suggest that low conical morphotypes of Gr. (G.) conomiozea inhabited greater depths than high conical morphotypes. Low conical forms of Gr. (G.) conomiozea are considered ancestral to the low conical species, Gr. (G.) pliozea. Oxygen isotopes indicate that Gr. (G.) pliozea inhabited greater depths than its ancestor, Gr. (G.) conomiozea.

These data are consistent with depth-parapatric and depth-allopatric models, but not with a sympatric model of speciation. In the allopatric model, reproduction at different water depths acts as a barrier between morphotypes. In the parapatric model, clinal variation along a depth gradient acts as a barrier between morphotypes living at the limits of the gradient. Depth segregation in both models results in genetic isolation and evolutionary divergence. Our data support a correlation between morphological evolution and habitat changes in the Globoconella clade, implying separation of populations as a driving force for morphological evolution.

Ecological segregation of morphotypes and species may be related to morphology (height of the conical angle), based on the data from Gr. (G.) conomiozea and Gr. (G.) pliozea. However, morphological differences alone do not necessarily produce depth differences. Large morphological differences between Gr. (G.) pliozea and closely related Gr. (G.) puncticulata did not result in isotopic and therefore depth differences between these species. These species coexisted at the same water depths for nearly 1 m.y. Thus, it is unlikely that the extinction of Gr. (G.) pliozea in the middle Pliocene resulted from competition with Gr. (G.) puncticulata, as previously suggested.

Type
Articles
Information
Paleobiology , Volume 25 , Issue 3 , Summer 1999 , pp. 383 - 395
Copyright
Copyright © The Paleontological Society 

Access options

Get access to the full version of this content by using one of the access options below. (Log in options will check for institutional or personal access. Content may require purchase if you do not have access.)

References

Literature Cited

Bandy, O. L. 1975. Messinian evaporite deposition and the Miocene/Pliocene boundary, Pasquasia-Capodarso Sections, Sicily. Pp. 49–63in Saito, T. and Burckle, L. H., eds. Late Neogene epoch boundaries. American Museum of Natural History Micropaleontology Press, New York.Google Scholar
Barton, V. R., and Bloemendal, J. 1986. Paleomagnetism of sediments collected during Leg 90, southwest Pacific. Pp. 1273–1316in Kennett, , von der Borch, , et al. 1986.Google Scholar
Berger, W. H., Killingly, J. S., and Vincent, E. 1978. Stable isotopes in deep sea carbonates: box core ERDC-92, west equatorial Pacific. Oceanologic Acta 1:203–216.Google Scholar
Curry, W. B., and Matthew, R. K. 1981. Equilibrium 18O fractionation in small size fraction of planktic foraminifera: evidence from Recent Indian Ocean sediments. Marine Micropaleontology 6:327–337.Google Scholar
Elmstrom, K. M., and Kennett, J. P. 1986. Late Neogene paleoceanographic evolution of Site 590: Southwest Pacific. Pp. 1361–1381in Kennett, , von der Borch, , et al. 1986.Google Scholar
Fairbanks, R. G., Sverdlove, R. F., Free, R., Wiebe, P. H., and Bé, A. W. H. 1982. Vertical distribution and isotopic composition of living planktonic foraminifera from the Panama Basin. Nature 298:841–844.Google Scholar
Hodell, D. A., and Kennett, J. P. 1986. Late Miocene-early Pliocene stratigraphy and paleoceanography of the South Atlantic and southwest Pacific oceans: a synthesis. Paleoceanography 1:285–311.Google Scholar
Hodell, D. A., and Vayavananda, A. 1993. Middle Miocene paleoceanography of the western equatorial Pacific (DSDP Site 289) and the evolution of Globorotalia (Fohsella). Marine Micropaleontology 22:279–310.Google Scholar
Hornibrook, N. de B. 1982. Late Miocene to Pleistocene Globorotalia (Foraminiferida) from Deep Sea Drilling Project Leg 29, Site 284, Southwest Pacific. New Zealand Journal of Geology and Geophysics 25:83–99.Google Scholar
Hornibrook, N. de B. 1984. Globorotalia (planktic foraminifera) at the Miocene/Pliocene boundary in New Zealand. Palaeogeography, Palaeoclimatology, Palaeoecology 46:107–117.CrossRefGoogle Scholar
Jenkins, D. G., and Srinivasan, M. S. 1986. Cenozoic planktonic foraminifers from the equator to the subantarctic of the southwest Pacific. Pp. 795–834in Kennett, , von der Borch, , et al. 1986.Google Scholar
Kennett, J. P., and Srinivasan, M. S. 1983. An atlas of Neogene planktonic foraminifera: phylogenetic approach. Hutchinson and Ross, Stroudsburg, Penn.Google Scholar
Kennett, J. P., and von der Borch, C. C. et al. 1986. Initial reports of the Deep Sea Drilling Project 90. U.S. Government Printing Office, Washington, D.C.Google Scholar
Lazarus, D. B., Hilbrecht, H., Spencer-Cervato, C., and Thierstein, H. 1995. Sympatric speciation and phyletic change in Globorotalia truncatulinoides. Paleobiology 21:28–51.Google Scholar
Lipps, J. H. 1970. Plankton evolution. Evolution 24:1–22.CrossRefGoogle ScholarPubMed
Lipps, J. H. 1979. Ecology and paleoecology of planktic foraminifera. Pp. 62–104in Lipps, J. H. and Berger, W. H., eds. Foraminiferal ecology and paleoecology. Society of Economic Paleontologists and Mineralogists, Houston.Google Scholar
Lohman, W. H. 1986. Calcareous nannoplankton biostratigraphy of the southern Coral Sea, Tasman Sea, and southwestern Pacific Ocean, Deep Sea Drilling Project leg 90: Neogene and Quaternary. Pp. 763–793in Kennett, , von der Borch, , et al. 1986.Google Scholar
Malmgren, B. A., and Berggren, W. A. 1987. Evolutionary changes in some late Neogene planktonic foraminiferal lineages and their relationships to paleoceanographic changes. Paleoceanography 2:445–456.CrossRefGoogle Scholar
Malmgren, B. A., and Kennett, J. P. 1981. Phyletic gradualism in a late Cenozoic planktonic foraminiferal lineage: DSDP Site 284, southwest Pacific. Paleobiology 7:230–240.Google Scholar
Norris, R. D., Corfield, R. M., and Cartlidge, J. E. 1993. Evolution of depth ecology in the planktonic foraminifera lineage Globorotalia (Fohsella). Geology 21:975–978.Google Scholar
Norris, R. D., Corfield, R. M., and Cartlidge, J. E. 1994. Evolutionary ecology of Globorotalia (Globoconella) (planktic foraminifera). Marine Micropaleontology 23:1–26.Google Scholar
Norris, R. D., Corfield, R. M., and Cartlidge, J. E. 1996. What is gradualism? Cryptic speciation in globorotalid foraminifera. Paleobiology 22:386–405.Google Scholar
Oppo, D. W., and Fairbanks, R. G. 1989. Carbon isotope composition of tropical surface water during the past 22,000 years. Paleoceanography 4:333–351.Google Scholar
Pearson, P. N., Shackleton, N. J., and Hall, M. A. 1997. Stableisotopic evidence for the sympatric divergence of Globigerinoides trilobus and Orbulina universa (planktonic foraminifera). Journal of the Geological Society, London 154:295–302.Google Scholar
Schneider, C. E., and Kennett, J. P. 1990. Oxygen isotopic evidence for seasonal or vertical segregation of ancestor and descendant species within the Neogene planktonic foraminiferal lineage Globorotalia (Globoconella). Geological Society of America Abstracts with Programs 23:A34.Google Scholar
Schneider, C. E., and Kennett, J. P. 1996. Isotopic evidence for interspecies differences in depth habitat during evolution of the Neogene planktonic foraminiferal lineage, Globoconella. Paleobiology 22:282–303.CrossRefGoogle Scholar
Scott, G. H. 1983. Biostratigraphy and histories of upper Miocene-Pliocene Globorotalia, South Atlantic and South West Pacific. Marine Micropaleontology 7:369–383.Google Scholar
Shackleton, N. J., Crowhurst, S., Hagelberg, T., Pisias, N. G., and Schneider, D. A. 1995. A new late Neogene time scale: application to Leg 138 Sites. In Pisias, N. G., Meyer, L. A., Janecek, T. R., Palmer-Julson, A., and van Andel, T. H., eds. Scientific results of the Ocean Drilling Program 138:73–101. College Station, Tex.Google Scholar
Spero, H. J., and DeNiro, M. 1987. The influence of symbiont photosynthesis on the δ18O and δ13C values of planktonic foraminiferal shell calcite. Symbiosis 4:213–228.Google Scholar
Wei, K.-Y. 1987. Multivariate morphometric differentiation of chronospecies in the late Neogene planktonic foraminiferal lineage. Marine Micropaleontology 12:183–202.Google Scholar
Wei, K.-Y. 1992. Evolution of the planktic foraminiferal clade Globoconella during the late Neogene: paleoceanographic modulation. Pp. 181–202in Tsuchi, R. and Ingle, J. Jr., eds. Pacific Neogene: environment, evolution, and events. University of Tokyo Press, Tokyo.Google Scholar
Wei, K.-Y., and Kennett, J. P. 1988. Phyletic gradualism and punctuated equilibrium in the late Neogene planktonic foraminifera clade Globoconella. Paleobiology 14:345–363.Google Scholar
Williams, D. F., Bé, A. W. H., and Fairbanks, R. G. 1981. Seasonal stable isotope variations in living planktonic foraminifera from the Sargasso Sea off Bermuda. Palaeogeography, Palaeoclimatology, Palaeoecology 33:71–102.Google Scholar
Williams, D. F., Ehrlich, R., Spero, H. J., Healy-Williams, N., and Gary, A. C. 1988. Shape and isotopic differences between conspecific foraminiferal morphotypes and resolution of paleoceanographic events. Palaeogeography, Palaeoclimatology, Palaeoecology 64:153–162.Google Scholar
Wold, S. 1976. Pattern recognition by means of disjoint principal components models. Pattern Recognition 8:127–139.Google Scholar
Wold, S., and Sjostrom, M. 1977. SIMCA: a model for analyzing chemical data in terms of similarity and analogy. Pp. 243–252in Kowalski, B. R., ed. Chemometrics: theory and application. American Chemical Society Symposium Series No. 52.Google Scholar