Late Neogene foraminiferal record and geological history inferred from ...
In southern Victoria Land, the occurrences of primary radioactive minerals appear to be associated with large-scale, often concentric, circular structures which are clearly visible in the January 1986 field season when we attempted to locate the radioactive veins in relation to major structural features of the area. The circular structures range in size from nearly 50 kilometers to smaller features only about 20 kilometers in diameter. Gamma-ray survey flight lines from previous years cross the outer boundaries of other circular structures at a number of locations, and they also show increased radioactivity in the boundary zones. We believe that the genesis of the uranium and thorium deposits is related to, and most probably contemporaneous with, the emplacement of the large-scale circular features. This research was supported in part by National Science Foundation grant DPI 82-16902 and the University of Kansas.
Late Neogene foraminiferal record and geological history inferred from Dry Valley Drilling Cores 10 and 11, Taylor Valley, Antarctica S.E. ISHMAN and P.N. WEBB Institute of Polar Studies
and Departtnen t of Geology and Mineralogy 0/no State University Columbus, 0/lu) 43210
The Late Cenozoic history of the dry valley region of Antarctica has been a focus of study for many workers over the past three decades. Drilling projects in the region—Deep Sea Drilling Project (DsDP) (Hayes, Frakes et al. 1975; Leckie and Webb 1983, 1985), Dry Valley Drilling Project (DvDP) (McGinnis 1981; Webb and Wrenn 1982), Ross Ice Shelf Project (risP) (Webb et al. 1979), McMurdo Sound Sediment and Tectonic Study (MSSTS-1) (Webb and Harwood in preparation; Barrett 1986), and Cenozoic Investigation of the Ross Sea 2 (CIROS-2) (Barrett 1985)—have contributed to gaining a better understanding of the Cenozoic history of the Ross Sea region. Of these projects, DVDI' drillholes 10 and 11 provide the most complete late Miocene/early Pliocene record for this sector. Preliminary reports on foraminifera (Wrenn 1977; Webb and Wrenn 1982), stratigraphy and sedimentology (McKelvey 1975; Powell 1981), geophysics (Hicks and Bennett 1981), paleomagnetics (Elston and Bressler 1981), and diatoms (Brady 1979) indicate fjord conditions in th Late Neogene Taylor Valley. This nearshore environment, close to the Transantarctic Mountains and outlets of the east antarctic ice sheet, is sensitive to glaciation, tectonic uplift, and glacio-eustatic fluctuations. Benthic foraminifera are reliable indicators of environmental change 1986 REVIEW
References Claridge, G.G.C., and I.B. Campbell. 1968. Origin of nitrate deposits. Nature,217, 428-130. Friedmann, E.I. 1977. Microorganisms in antarctic desert rocks from dry valleys and Dufek Massif. Antarctic Journal of tilt' U.S., 12(5), 26. Laird, C.M. 1983. Solar particle flux and nitrate in South Pole snow. In B. McCormac, (Ed.), Weather and climate responses to solar activity variatimis. Boulder: Colorado Associated University Press.
Miotke, F.D., and R. l-lodenberg. 1980. Salt fracturing and chemical weathering in the Darwin Mountains and the Dry Valleys, Victoria Land, Antarctica. Polarforschung, 50(1/2) 45-80. (In German) Ugolini, F.C. and M.L. Jackson 1982. Weathering and mineral synthesis in antarctic soils. In C. Craddock, (Ed.), Antarctic geoscience. Madison: University of Wisconsin Press. Zeller, E., and B.C. Parker. 1981. Nitrate ion in antarctic firn as marker for solar activity. Geophysical Research Letters, 8, 895.
(Phleger 1960; Murray 1973; Boltovskoy and Wright 1976). Assemblage fluctuations observed in the DVD1' 10 and 11 faunas are related to the Late Neogene tectonic and glacial history of the Ross Sea region. Ninety-four samples from the lower parts of DVDP 10 and 11 (sub-133 meters and sub-193 meters, respectively) yielded a total of 43 genera and 88 species of foraminifera. The fauna is dominated by calcareous benthic taxa. No agglutinated forms are present and only three planktonic species occur. Diversity for individual samples ranged from 3 to 42 species. The biostratigraphic zonation erected for DVDP 10 and 11 is composed of four assemblage zones (based on species present and equitability) (figure 1). Assemblage zones are separated by interval zones that are barren of foraminifera. The Troc/ioelphidieila uniforamina zone (figure 1) contains the only planktonics recovered from DVI)P 10 and 11; Streptochilus latuin Brönniman and Resig, Neogloboquadrina pacizyderma (Ehrenberg), and Candeina antarctica Leckie and Webb. This is the first report of S. latum in the high latitudes. In the southwest Pacific its range is restricted to the late Miocene (BrOnnimann and Resig 1971) making it valuable for dating these cores (approximately 7 million years). In addition, diatom data support the age for this assemblage zone with the occurrence of Thalassiosira torokina and Actinocyclus ingens as well as the absence of Pliocene marker species Nitzsc/iia praeinterfrigidaria and Thalassiosira oestrupi. Although it has no biostratigraphic utility here, Candeina antarctica occurs in the T. uniforamina zone, marking its youngest occurrence (previously believed to be early Miocene; Leckie and Webb 1985). The benthic species Troc/ioelphidiella uniforamina Leckie and Webb is the middle/late Miocene representative of the late Oligocene/Pliocene Trochoelphidiella Webb lineage, a group endemic to the antarctic region (Webb 1974; Leckie and Webb 1985). This zone represents relatively deep water (600-900 meters) with bathymetric fluctuations indicated by increase in Ehrenbergina spp. abundances (up to 25 percent). The Epistominella vitrea zone (figure 1) exhibits low species diversity (fewer than 20 species), poor equitability, and lacks Trochoelphidiella uniforatnina Leckie and Webb and members of the Miliolidae. With exception of E. vitrea, Astrononion echolsi 13
0. melo d'Orbigny. These species compose up to 50 percent of the assemblage. Assemblages of this zone are also characterized by a pronounced increase in species test size. Greatest diversity occurs in this zone (44 species), although many of these are rare occurrences of Nodosariidae. This zone represents relatively shallower conditions (100-500 meters) than interpreted for the underlying zones. Separation of assemblage zones by interval zones points to fluctuating marine paleoenvironmental conditions throughout the successions. These changing conditions are produced by glacial oscillations within the fjord basin. Sedimentology and diatom distribution suggest a contrasting environment for DVDP 10 and 11, based on their proximity to the grounding line of the Late Neogene Taylor Glacier. DVDP 11 represents a nearshore facies proximal to a grounding line as suggested by the occurrence of massive diamictites and poor distribution of diatoms. Conversely, DVDP 10 represents a more marine facies, located further from the grounding line, and characterized by varied lithologies and higher occurrence of marine diatoms. Diatom distribution in DVDP 10 and 11 also serves as a sea-ice indicator, absence often indicating thick and semipermanent ice-cover. Interval zones, sedimentology, foraminiferal assemblage
Palsopositlon (—GM.) 400
Present 401
S.). 0
-400
- .vD. II
-BOB-
-4-sc -500
-1200
ISIIU S.i-L...) (.)
-leo
Uplift Nate. DVDP 11
-I.. -4.. Figure 1. Schematic presentation of ages for the lower part of DVDP 10 and 11 (sub-135 meters and sub-195 meters, respectively), foraminiferal biozonations, and foraminiferal distribution (occurrences designated by stippled pattern).
Kennett and Globocassidulina suhglohosa (Brady) are the most abundant taxa at 17 percent and 37 percent, respectively, in this zone. The Trochoelphidiella onyxi zone is recognized only in DVDP 10 (figure 1). Because the assemblage is very similar to the mid- to late-Pliocene fauna described from Wright Valley (Webb 1972, 1974) and Brown Peninsula (Eggers 1979; Leckie and Webb 1979; Webb and Andreasen, (Antarctic Journal, this issue), a mid- to late-Pliocene age has been assigned to this zone. The faunal distinction of this zone is the occurrence of Trochoelphidiella onxyi Webb. The Trifarina spp. zone (figure 1) occurs only in DVDP 11. Four species have their first appearance in this zone; Trifarina earlandi (Parr), Trifarina pauperata (Heron-Allen and Earland), Stainforthia concava (Hoglund), Gyroidina subplanulata Echols, and Oolina aff 14
-I.. -I.. ir
-700
-$00
-coo 5.0 5.0 4.0 3.0 3.0 1.0 0 V..,. (N.)
Figure 2. (Upper) Cartoon depicting paleoposition of DVDP site 11 with respect to its present position; (Lower) calculated uplift rates showing high- and low-end values (stippled area) and the sporadic uplift values (geniculate line) interpreted from foraminiferal bathymetric data. ("Ma" denotes "million years ago:' "m" denotes "meter.") AN1ARCTIC JOURNAl.
zones, and distribution of diatoms indicate a series of environmental cycles up-core in DVDP 10 and 11. These cycles reflect the faunal and floral sensitivity to subtle environmental fluctuations (figure 1). Paleoenvironmental conditions recognized in DVDP 10 and 11 indicate a major overall shallowing trend in the early Pliocene, overprinted by late Miocene/Pliocene glacio-eustatic fluctuations. The tectonic history of the dry valley region involves a period of uplift from the late Jurassic. Uplift for the past 55 million years (Cenozoic) is calculated at approximately 100 meters per million years (Fitzgerald and Gleadow 1985) based on apatite fission-track techniques. Paleodepths of Taylor fjord indicated by Miocene/Pliocene benthic foraminifera and sediments suggest an uplift rate of approximately 87 meters per million years (Ishman 1985) with respect to present sea-level (figure 2). Bathymetric stability indicated in the lowermost Trochoelphidieila uniforamina zone (figure 1), and distinct bathymetric shallowing initiated with the Epistominelia vitrea zone and continuing through the Trifarina spp. zone, provide evidence for the onset of rapid uplift in the early Pliocene. Environmental cycles observed throughout the late Miocene succession of DVDP 10 and 11 represent regional eustatic events related to oscillations in the east antarctic ice sheet outlet glaciers penetrating the dry valleys. This work was supported in part by National Science Foundation grant DFP 82-14174.
References Barrett, P.J. 1985. Plio-Pleistocene glacial sequence cored at CIROS 2, Ferrar Fjord, Western McMurdo Sound. New Zealand Antarctic Record, 6(2), 8-19. Barrett, P.J. (Ed.) 1986. Antarctic Cenozoic history from the MSSTS-1 drilIhole, McMurdo Sound. (New Zealand Department of Scientific and Industrial Research, Wellington: Department of Scientific and Industrial Research Bulletin.) Boltovskoy, E., and R. Wright. 1976. Recent foraminifera. The Hague: Dr. W. Junk b.v. Publishers. Brady, H.T. 1979. The dating and interpretation of diatom zones in Dry Valley Drilling Project Holes 10 and 11 Taylor Valley, South Victoria Land, Antarctica. In T. Nagata (Ed.), Memoirs of National Institute of Polar Research, Vol. 13. Tokyo: National Institute of Polar Research. Bronnimann, P., and J . Resig. 1971. A Neogene Globigerinacean biochronologic time-scale of the southwestern Pacific. In E. L. Winterer et al. (Eds.), Initial Reports of the Deep Sea Drilling Project, Vol. 7. Washington, D.C.: U.S. Government Printing Office. Eggers, A.J. 1979. Scallop Hill Formation, Brown Peninsula, McMurdo Sound, Antarctica. New Zealand Journal of Geology and Geophysics, 22(3), 353-361. Elston, D.P., and S.L. Bressler. 1981. Magnetic stratigraphy of DVDI' Drill Cores and Late Cenozoic history of Taylor Valley, Transantarctic Mountains, Antarctica. In L.D. McGinnis (Ed.), Dry Valley Drilling Project, Vol. 33. Washington, D.C.: American Geophysical Union.
1986 REVIEW
Fitzgerald, P.G., and A.J.W. Gleadow. 1985. Uplift history of the Transantarctic Mountains, Victoria Land Antarctica. (Abstract) Workshop on Cenozoic Geology of the Southern High Latitudes, 1, 16. Hayes, D.E., Frakes, L.A., et al. 1975. Initial Reports of the Deep Sea Drilling Project, Vol. 28. Washington, D.C.: U.S. Government Printing Office. Hicks, SR., and D.J. Bennett. 1981. Gravity models of the lower Taylor Valley, Antarctica. New Zealand Journal of Geology and Geophysics, 24, 555-562. Ishman, S.E. 1985. Foraminiferal hiostratigraphy and paleoecology of Dry Valley Drilling Cores 10 and 11, Taylor Valley, Antarctica. (Masters thesis, Ohio State University, Columbus, Ohio.) Leckie, R.M., and P.N. Webb. 1979. The Scallop Hill Formation and associated Pliocene marine deposits of southern McMurdo Sound. Antarctic Journal of the U.S., 14(5), 54-56. Leckie, R.M., and P.N. Webb. 1983. Late Oligocene and early Neogene foraminifers of Deep Sea Drilling Project Site 270 Ross Sea, Antarctica. Geology, 11, 578-582. Leckie, R.M., and P.N. Webb. 1985. Late Paleogene and early Neogene foraminifers of Deep Sea Drilling Project Site 270 Ross Sea, Antarctica. In J.P. Kennett, C.C. von der Borch, et al. (Eds.), Initial Reports of the Deep Sea Drilling Project, Vol. 90. Washington, D.C.: U.S. Government Printing Office, 1093-1119. McGinnis, L.D. 1981. Dry Valley Drilling Project. Antarctic Research Series, Vol. 33. Washington, D.C.: American Geophysical Union. McKelvey, B.C. 1975. Preliminary site reports DVDI' Sites 10 and 11, Taylor Valley. Dry Valley Drilling Project Bulletin, 5, 16-60. Murray, J.W. 1973. Distribution and ecology of living hent/iic foraminifera. New York: Crane, Russak and Company, Inc. Phleger, F.B. 1960. Ecology and distribution of Recent foraniinifera. Baltimore: Johns Hopkins Press. Powell, R.D. 1981. Sedimentation conditions in Taylor Valley, Antarctica, inferred from textural analysis of DVDP cores. In L.D. McGinnis (Ed.), Dry Valley Drilling Project, Vol. 33. Washington, D.C.: American Geophysical Union. Webb, P.N. 1972. Wright Fjord, Pliocene marine invasion of an antarctic dry valley. Antarctic Journal of the U.S., 7(5), 225-234. Webb, P.N. 1974. Micropaleontology, paleoecology and correlation of the Pecten Gravels, Wright Valley, Antarctica, and description of Trochoelphidiella onxyi, n. gen., n. sp. Journal of Foraminiferal Research, 4, 184-199. Webb, P.N., T.E. Ronan, J.H. Lipps, and T.E. Delaca. 1979. Miocene glaciomarine sediments from beneath southern Ross Ice Shelf, Antarctica. Science, 203, 43537. Webb, P.N., and J.H. Wrenn. 1982. Upper Cenozoic micropaleontology and biostratigraphy of Eastern Taylor Valley, Antarctica. In C. Craddock (Ed.), Antarctic geoscience. Madison: University of Wisconsin Press. Webb, P.N. and J.E. Andreasen. 1986. Potassium/argon dating of volcanic material associated with the Pliocene Pecten Conglomerate (Cockburn Island) and Scallop Hill Formation (McMurdo Sound). Antarctic Journal of the U.S., 21(5). Webb, P. N., and D. H. Harwood. In preparation. Relationships between seismic (sonic) velocity, lithostratigraphy, grain size distribution, biostratigraphy and paleobathymetry in the upper Oligocene glacigene sediments of MSST-1 Drillhole, McMurdo Sound. Wrenn, J.H. 1977. Cenozoic subsurface micropaleontology and geology of Eastern Taylor Valley, Antarctica. DeKalb, Illinois: Northern Illinois
University.
15
Late Neogene foraminiferal record and geological history inferred from Dry Valley Drilling Cores 10 and 11, Taylor Valley, Antarctica S.E. ISHMAN and P.N. WEBB Institute of Polar Studies
and Departtnen t of Geology and Mineralogy 0/no State University Columbus, 0/lu) 43210
The Late Cenozoic history of the dry valley region of Antarctica has been a focus of study for many workers over the past three decades. Drilling projects in the region—Deep Sea Drilling Project (DsDP) (Hayes, Frakes et al. 1975; Leckie and Webb 1983, 1985), Dry Valley Drilling Project (DvDP) (McGinnis 1981; Webb and Wrenn 1982), Ross Ice Shelf Project (risP) (Webb et al. 1979), McMurdo Sound Sediment and Tectonic Study (MSSTS-1) (Webb and Harwood in preparation; Barrett 1986), and Cenozoic Investigation of the Ross Sea 2 (CIROS-2) (Barrett 1985)—have contributed to gaining a better understanding of the Cenozoic history of the Ross Sea region. Of these projects, DVDI' drillholes 10 and 11 provide the most complete late Miocene/early Pliocene record for this sector. Preliminary reports on foraminifera (Wrenn 1977; Webb and Wrenn 1982), stratigraphy and sedimentology (McKelvey 1975; Powell 1981), geophysics (Hicks and Bennett 1981), paleomagnetics (Elston and Bressler 1981), and diatoms (Brady 1979) indicate fjord conditions in th Late Neogene Taylor Valley. This nearshore environment, close to the Transantarctic Mountains and outlets of the east antarctic ice sheet, is sensitive to glaciation, tectonic uplift, and glacio-eustatic fluctuations. Benthic foraminifera are reliable indicators of environmental change 1986 REVIEW
References Claridge, G.G.C., and I.B. Campbell. 1968. Origin of nitrate deposits. Nature,217, 428-130. Friedmann, E.I. 1977. Microorganisms in antarctic desert rocks from dry valleys and Dufek Massif. Antarctic Journal of tilt' U.S., 12(5), 26. Laird, C.M. 1983. Solar particle flux and nitrate in South Pole snow. In B. McCormac, (Ed.), Weather and climate responses to solar activity variatimis. Boulder: Colorado Associated University Press.
Miotke, F.D., and R. l-lodenberg. 1980. Salt fracturing and chemical weathering in the Darwin Mountains and the Dry Valleys, Victoria Land, Antarctica. Polarforschung, 50(1/2) 45-80. (In German) Ugolini, F.C. and M.L. Jackson 1982. Weathering and mineral synthesis in antarctic soils. In C. Craddock, (Ed.), Antarctic geoscience. Madison: University of Wisconsin Press. Zeller, E., and B.C. Parker. 1981. Nitrate ion in antarctic firn as marker for solar activity. Geophysical Research Letters, 8, 895.
(Phleger 1960; Murray 1973; Boltovskoy and Wright 1976). Assemblage fluctuations observed in the DVD1' 10 and 11 faunas are related to the Late Neogene tectonic and glacial history of the Ross Sea region. Ninety-four samples from the lower parts of DVDP 10 and 11 (sub-133 meters and sub-193 meters, respectively) yielded a total of 43 genera and 88 species of foraminifera. The fauna is dominated by calcareous benthic taxa. No agglutinated forms are present and only three planktonic species occur. Diversity for individual samples ranged from 3 to 42 species. The biostratigraphic zonation erected for DVDP 10 and 11 is composed of four assemblage zones (based on species present and equitability) (figure 1). Assemblage zones are separated by interval zones that are barren of foraminifera. The Troc/ioelphidieila uniforamina zone (figure 1) contains the only planktonics recovered from DVI)P 10 and 11; Streptochilus latuin Brönniman and Resig, Neogloboquadrina pacizyderma (Ehrenberg), and Candeina antarctica Leckie and Webb. This is the first report of S. latum in the high latitudes. In the southwest Pacific its range is restricted to the late Miocene (BrOnnimann and Resig 1971) making it valuable for dating these cores (approximately 7 million years). In addition, diatom data support the age for this assemblage zone with the occurrence of Thalassiosira torokina and Actinocyclus ingens as well as the absence of Pliocene marker species Nitzsc/iia praeinterfrigidaria and Thalassiosira oestrupi. Although it has no biostratigraphic utility here, Candeina antarctica occurs in the T. uniforamina zone, marking its youngest occurrence (previously believed to be early Miocene; Leckie and Webb 1985). The benthic species Troc/ioelphidiella uniforamina Leckie and Webb is the middle/late Miocene representative of the late Oligocene/Pliocene Trochoelphidiella Webb lineage, a group endemic to the antarctic region (Webb 1974; Leckie and Webb 1985). This zone represents relatively deep water (600-900 meters) with bathymetric fluctuations indicated by increase in Ehrenbergina spp. abundances (up to 25 percent). The Epistominella vitrea zone (figure 1) exhibits low species diversity (fewer than 20 species), poor equitability, and lacks Trochoelphidiella uniforatnina Leckie and Webb and members of the Miliolidae. With exception of E. vitrea, Astrononion echolsi 13
0. melo d'Orbigny. These species compose up to 50 percent of the assemblage. Assemblages of this zone are also characterized by a pronounced increase in species test size. Greatest diversity occurs in this zone (44 species), although many of these are rare occurrences of Nodosariidae. This zone represents relatively shallower conditions (100-500 meters) than interpreted for the underlying zones. Separation of assemblage zones by interval zones points to fluctuating marine paleoenvironmental conditions throughout the successions. These changing conditions are produced by glacial oscillations within the fjord basin. Sedimentology and diatom distribution suggest a contrasting environment for DVDP 10 and 11, based on their proximity to the grounding line of the Late Neogene Taylor Glacier. DVDP 11 represents a nearshore facies proximal to a grounding line as suggested by the occurrence of massive diamictites and poor distribution of diatoms. Conversely, DVDP 10 represents a more marine facies, located further from the grounding line, and characterized by varied lithologies and higher occurrence of marine diatoms. Diatom distribution in DVDP 10 and 11 also serves as a sea-ice indicator, absence often indicating thick and semipermanent ice-cover. Interval zones, sedimentology, foraminiferal assemblage
Palsopositlon (—GM.) 400
Present 401
S.). 0
-400
- .vD. II
-BOB-
-4-sc -500
-1200
ISIIU S.i-L...) (.)
-leo
Uplift Nate. DVDP 11
-I.. -4.. Figure 1. Schematic presentation of ages for the lower part of DVDP 10 and 11 (sub-135 meters and sub-195 meters, respectively), foraminiferal biozonations, and foraminiferal distribution (occurrences designated by stippled pattern).
Kennett and Globocassidulina suhglohosa (Brady) are the most abundant taxa at 17 percent and 37 percent, respectively, in this zone. The Trochoelphidiella onyxi zone is recognized only in DVDP 10 (figure 1). Because the assemblage is very similar to the mid- to late-Pliocene fauna described from Wright Valley (Webb 1972, 1974) and Brown Peninsula (Eggers 1979; Leckie and Webb 1979; Webb and Andreasen, (Antarctic Journal, this issue), a mid- to late-Pliocene age has been assigned to this zone. The faunal distinction of this zone is the occurrence of Trochoelphidiella onxyi Webb. The Trifarina spp. zone (figure 1) occurs only in DVDP 11. Four species have their first appearance in this zone; Trifarina earlandi (Parr), Trifarina pauperata (Heron-Allen and Earland), Stainforthia concava (Hoglund), Gyroidina subplanulata Echols, and Oolina aff 14
-I.. -I.. ir
-700
-$00
-coo 5.0 5.0 4.0 3.0 3.0 1.0 0 V..,. (N.)
Figure 2. (Upper) Cartoon depicting paleoposition of DVDP site 11 with respect to its present position; (Lower) calculated uplift rates showing high- and low-end values (stippled area) and the sporadic uplift values (geniculate line) interpreted from foraminiferal bathymetric data. ("Ma" denotes "million years ago:' "m" denotes "meter.") AN1ARCTIC JOURNAl.
zones, and distribution of diatoms indicate a series of environmental cycles up-core in DVDP 10 and 11. These cycles reflect the faunal and floral sensitivity to subtle environmental fluctuations (figure 1). Paleoenvironmental conditions recognized in DVDP 10 and 11 indicate a major overall shallowing trend in the early Pliocene, overprinted by late Miocene/Pliocene glacio-eustatic fluctuations. The tectonic history of the dry valley region involves a period of uplift from the late Jurassic. Uplift for the past 55 million years (Cenozoic) is calculated at approximately 100 meters per million years (Fitzgerald and Gleadow 1985) based on apatite fission-track techniques. Paleodepths of Taylor fjord indicated by Miocene/Pliocene benthic foraminifera and sediments suggest an uplift rate of approximately 87 meters per million years (Ishman 1985) with respect to present sea-level (figure 2). Bathymetric stability indicated in the lowermost Trochoelphidieila uniforamina zone (figure 1), and distinct bathymetric shallowing initiated with the Epistominelia vitrea zone and continuing through the Trifarina spp. zone, provide evidence for the onset of rapid uplift in the early Pliocene. Environmental cycles observed throughout the late Miocene succession of DVDP 10 and 11 represent regional eustatic events related to oscillations in the east antarctic ice sheet outlet glaciers penetrating the dry valleys. This work was supported in part by National Science Foundation grant DFP 82-14174.
References Barrett, P.J. 1985. Plio-Pleistocene glacial sequence cored at CIROS 2, Ferrar Fjord, Western McMurdo Sound. New Zealand Antarctic Record, 6(2), 8-19. Barrett, P.J. (Ed.) 1986. Antarctic Cenozoic history from the MSSTS-1 drilIhole, McMurdo Sound. (New Zealand Department of Scientific and Industrial Research, Wellington: Department of Scientific and Industrial Research Bulletin.) Boltovskoy, E., and R. Wright. 1976. Recent foraminifera. The Hague: Dr. W. Junk b.v. Publishers. Brady, H.T. 1979. The dating and interpretation of diatom zones in Dry Valley Drilling Project Holes 10 and 11 Taylor Valley, South Victoria Land, Antarctica. In T. Nagata (Ed.), Memoirs of National Institute of Polar Research, Vol. 13. Tokyo: National Institute of Polar Research. Bronnimann, P., and J . Resig. 1971. A Neogene Globigerinacean biochronologic time-scale of the southwestern Pacific. In E. L. Winterer et al. (Eds.), Initial Reports of the Deep Sea Drilling Project, Vol. 7. Washington, D.C.: U.S. Government Printing Office. Eggers, A.J. 1979. Scallop Hill Formation, Brown Peninsula, McMurdo Sound, Antarctica. New Zealand Journal of Geology and Geophysics, 22(3), 353-361. Elston, D.P., and S.L. Bressler. 1981. Magnetic stratigraphy of DVDI' Drill Cores and Late Cenozoic history of Taylor Valley, Transantarctic Mountains, Antarctica. In L.D. McGinnis (Ed.), Dry Valley Drilling Project, Vol. 33. Washington, D.C.: American Geophysical Union.
1986 REVIEW
Fitzgerald, P.G., and A.J.W. Gleadow. 1985. Uplift history of the Transantarctic Mountains, Victoria Land Antarctica. (Abstract) Workshop on Cenozoic Geology of the Southern High Latitudes, 1, 16. Hayes, D.E., Frakes, L.A., et al. 1975. Initial Reports of the Deep Sea Drilling Project, Vol. 28. Washington, D.C.: U.S. Government Printing Office. Hicks, SR., and D.J. Bennett. 1981. Gravity models of the lower Taylor Valley, Antarctica. New Zealand Journal of Geology and Geophysics, 24, 555-562. Ishman, S.E. 1985. Foraminiferal hiostratigraphy and paleoecology of Dry Valley Drilling Cores 10 and 11, Taylor Valley, Antarctica. (Masters thesis, Ohio State University, Columbus, Ohio.) Leckie, R.M., and P.N. Webb. 1979. The Scallop Hill Formation and associated Pliocene marine deposits of southern McMurdo Sound. Antarctic Journal of the U.S., 14(5), 54-56. Leckie, R.M., and P.N. Webb. 1983. Late Oligocene and early Neogene foraminifers of Deep Sea Drilling Project Site 270 Ross Sea, Antarctica. Geology, 11, 578-582. Leckie, R.M., and P.N. Webb. 1985. Late Paleogene and early Neogene foraminifers of Deep Sea Drilling Project Site 270 Ross Sea, Antarctica. In J.P. Kennett, C.C. von der Borch, et al. (Eds.), Initial Reports of the Deep Sea Drilling Project, Vol. 90. Washington, D.C.: U.S. Government Printing Office, 1093-1119. McGinnis, L.D. 1981. Dry Valley Drilling Project. Antarctic Research Series, Vol. 33. Washington, D.C.: American Geophysical Union. McKelvey, B.C. 1975. Preliminary site reports DVDI' Sites 10 and 11, Taylor Valley. Dry Valley Drilling Project Bulletin, 5, 16-60. Murray, J.W. 1973. Distribution and ecology of living hent/iic foraminifera. New York: Crane, Russak and Company, Inc. Phleger, F.B. 1960. Ecology and distribution of Recent foraniinifera. Baltimore: Johns Hopkins Press. Powell, R.D. 1981. Sedimentation conditions in Taylor Valley, Antarctica, inferred from textural analysis of DVDP cores. In L.D. McGinnis (Ed.), Dry Valley Drilling Project, Vol. 33. Washington, D.C.: American Geophysical Union. Webb, P.N. 1972. Wright Fjord, Pliocene marine invasion of an antarctic dry valley. Antarctic Journal of the U.S., 7(5), 225-234. Webb, P.N. 1974. Micropaleontology, paleoecology and correlation of the Pecten Gravels, Wright Valley, Antarctica, and description of Trochoelphidiella onxyi, n. gen., n. sp. Journal of Foraminiferal Research, 4, 184-199. Webb, P.N., T.E. Ronan, J.H. Lipps, and T.E. Delaca. 1979. Miocene glaciomarine sediments from beneath southern Ross Ice Shelf, Antarctica. Science, 203, 43537. Webb, P.N., and J.H. Wrenn. 1982. Upper Cenozoic micropaleontology and biostratigraphy of Eastern Taylor Valley, Antarctica. In C. Craddock (Ed.), Antarctic geoscience. Madison: University of Wisconsin Press. Webb, P.N. and J.E. Andreasen. 1986. Potassium/argon dating of volcanic material associated with the Pliocene Pecten Conglomerate (Cockburn Island) and Scallop Hill Formation (McMurdo Sound). Antarctic Journal of the U.S., 21(5). Webb, P. N., and D. H. Harwood. In preparation. Relationships between seismic (sonic) velocity, lithostratigraphy, grain size distribution, biostratigraphy and paleobathymetry in the upper Oligocene glacigene sediments of MSST-1 Drillhole, McMurdo Sound. Wrenn, J.H. 1977. Cenozoic subsurface micropaleontology and geology of Eastern Taylor Valley, Antarctica. DeKalb, Illinois: Northern Illinois
University.
15
