The History of the Earth's Surface Temperature During the Past 100 Million Years

Savin, Samuel M.

doi:10.1146/annurev.ea.05.050177.001535

Cited by 642 publications

(297 citation statements)

References 30 publications

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“…During the latest Paleocene and early Eocene (Wasatchian) world climates were warming (Savin, 1977;Wolfe, 1971Wolfe, , 1978Wolfe & Poore, 1982), possibly as a result of elevated levels of atmospheric C0 2 and associated effects on circulation patterns Rea et al, 1985). At this time evergreen broad-leaved taxa increased in importance within local floras.…”

Section: Patterns Of Vegetational Changementioning

confidence: 99%

“…This relationship has been worked out with some precision based on the humid floras of East Asia (Wolfe, 1979). Studies based on smaller regions have been used to question the resolution of leaf-margin inferences (Dolph, 1976(Dolph, , 1978a(Dolph, , 1978b(Dolph, , 1979Dolph & Dilcher, 1979), but the basic pattern of climate change as inferred from Tertiary floras agrees with data from a variety of other sources (e.g., Savin, 1977;Wolfe & Poore, 1982;Hutchison, 1982;Reaetal., 1985). Physiognomic analysis also considers the average size of leaves in a fossil assemblage, their apparent thickness, cuticle thickness, pubescence, the number of leaf types with drip tips, and the number of species that are probable lianes (those with cordate-based leaves).…”

Section: Paleoecologymentioning

confidence: 99%

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Eocene and Oligocene Floras and Vegetation of the Rocky Mountains

Wing¹

1987

Annals of the Missouri Botanical Garden

114

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Section: Patterns Of Vegetational Changementioning

confidence: 99%

Section: Paleoecologymentioning

confidence: 99%

Eocene and Oligocene Floras and Vegetation of the Rocky Mountains

Wing¹

1987

Annals of the Missouri Botanical Garden

114

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“…18 O occurs throughout the Tertiary until very high amplitude variations and positive 18 O values are seen in the Pleistocene (Shackleton and Opdyke, 1973;Shackleton and Kennett, 1975;Savin et al, 1975;Savin, 1977). The Eocene-Oligocene 18 O enrichment has been variously interpreted to be the result of cooling and/or ice volume fluctuations (Shackleton and Kennett, 1975;Savin et al, 1975;Douglas and Savin, 1978;Matthews and Poore, 1980).…”

Section: A General Enrichment Inmentioning

confidence: 99%

The Foraminiferal Isotope Record across the Eocene/Oligocene Boundary at Deep Sea Drilling Project Site 540

Bélanger¹,

Matthews²

1984

Initial Reports of the Deep Sea Drilling Project

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We analyzed the oxygen and carbon isotopic composition of planktonic and benthic foraminifers picked from 13 late Eocene to late Oligocene samples from DSDP Site 540 (23°49.73'N, 84°22.25'W, 2926 m water depth) from the Gulf of Mexico. An enrichment occurs in 18 O of about 0.5 to 0.8‰ in both benthic foraminifers and surface-dwelling planktonic foraminifers between the latest Eocene and early Oligocene. This early Oligocene maximum is followed by lower18 O values. A 1.2‰ δ 13 C decrease in both benthic and planktonic foraminiferal data occurs from the late Eocene to the late Oligocene. There is a correspondence of the 13 C signal to deep-sea records; however, the amplitude of this change is greater than previously seen in deep-sea cores, possibly as a result of proximity to terrestrial sources of carbon.The covarying isotopic changes in both benthic and planktonic foraminifers suggest global causes, such as ice volume increases and increased terrestrial carbon input to the ocean. However, during the latter part of the record (earlylate Oligocene), the increases in the benthic 18 O without accompanying increases observed with planktonic foraminifers suggest that changes in only one part of the system occurred; one potential explanation being a decrease in bottom-water temperatures without concomitant changes in the surface waters. The 18 O differences between species of planktonic foraminifers and the difference between planktonic and benthic 18 O data indicate that diagenesis problems are minimal. These preliminary results are encouraging given that these cores are partially lithified.

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“…post-R2 sediments on Figs. [4][5][6][7][8][9][10][11][12]. This is especially true along the shallower margins of the drifts, where currents are topographically -29- Feni Dri ft (Fi g. 5)…”

Section: Rockall Regionmentioning

confidence: 99%

Late Paleogene (Eocene to Oligocene) paleoceanography of the northern North Atlantic

Miller¹

1982

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Seismic stratigraphic evidence from the western and northern North Atlantic indicates that a major change in abyssal circulation occurred in the latest Eocene to earliest Oligocene. In the northern North Atlantic, the widely-distributed reflector R4 correlates with an unconformity that can be traced to its correlative conformity near the top of the Eocene. This horizon reflects a change from weakly circulating (Eocene) to vigorously circulating bottom water (early Oligocene). Sediment distribution patterns provide evidence for strong contour-following bottom water flow beginning at reflector R4 time; this suggests a northern source for this bottom water, probably from the Arctic via the Norwegian-Greenland Sea and Faeroe-Shetland Channel. Erosion and current-controlled sedimentation continued through the Oligocene; however, above reflector R3 (middle to upper Oligocene), the intensity of abyssal currents decreased. Above reflector R2 (upper lower Miocene) current-controlled sedimentation became more coherent and a major phase of sedimentary drift development began. This resulted from further reduction in speeds and stabilization of abyssal currents.Paleontological and stable isotopic data support these interpretations. In the Bay of Biscay/Goban Spur regions, a major 6180 increase began at -38 Ma (late Eocene), culminating in a rapid (< 0.5 my) increase in 6180 just above the Eocene/Oligocene boundary (~ 36.5 Ma). A rapid 6 13 C increase also occurs at -36.5 Ma in these sites. Major changes in benthic foraminiferal assemblages also occurred between the middle Eocene and the earliest Oligocene: 1) In the Labrador Sea, a predominantly agglutinated assemblage was replaced by a calcareous assemblage between the middle Eocene and early Oligocene; 2) In the abyssal (> 3km) Bay of Biscay, an indigenous Eocene calcareous fauna including Nuttallides truempyi, Clinapertina spp., Abyssammina spp., Aragonia spp., and Alabamina dissonata became extinct between the middle Eocene and earliest Ollgocene; 3) In shallower sites (< 3km paleodepth) throughout the Atlantic, a Nuttallides truempyi-dominated assemblage was replaced by a Globocassidulina subglobosa-yroidinoides-Cibicidoides ungerianus-Oridorsalis assemblage in the early late Eoce (~ 40-3 5 ma). These Taunal and isotopic changes represent the transition from warm, old, corrosive Eocene bottom waters to colder, younger (lower C02 and higher pH, hence less corrosive) early Oligocene bottom waters.

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The History of the Earth's Surface Temperature During the Past 100 Million Years

Cited by 642 publications

References 30 publications

Eocene and Oligocene Floras and Vegetation of the Rocky Mountains

Eocene and Oligocene Floras and Vegetation of the Rocky Mountains

The Foraminiferal Isotope Record across the Eocene/Oligocene Boundary at Deep Sea Drilling Project Site 540

Late Paleogene (Eocene to Oligocene) paleoceanography of the northern North Atlantic

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