A radio-carbon-dated pollen profile from Sunbeam Prairie bog, Darke County, Ohio

Kapp, Ronald O.; Gooding, Ansel M.

doi:10.2475/ajs.262.2.259

Cited by 16 publications

(10 citation statements)

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“…Many of them are at localities where proboscidian fossils have been found (Thomas and others, 1952;Skeels, 1962;Drumm, 1963;Forsyth, 1963;Dreimanis, 1968;Churcher and Karrow, 1963;Cleland, 1966). Most bog-lake studies deal mainly with palynology; for instance, the studies by Terasmae (1958Terasmae ( , 1960, Terasmae and Mirynech (1964), Kapp (1964), Gooding and Ogden (1965), Ogden (1965Ogden ( , 1966Ogden ( , 1967Ogden ( , 1969, Cushing (1965), Lewis and others (1966), and Davis (1967). Mollusks are considered by Terasmae (1965) and LaRocque (1966LaRocque ( , 1967LaRocque ( , 1968LaRocque ( , 1970.…”

Section: Paleontologic Studiesmentioning

confidence: 97%

Wisconsin Glaciation in the Huron, Erie, and Ontario Lobes

Dreimanis¹,

Goldthwait²

1973

Geological Society of America Memoirs

100

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The names of the Huron, Erie, and Ontario Lobes imply that glaciers followed these lake depressions, but the flow patterns of these lobes were complex and changed several times during the Wisconsin glaciation. The sublobes of the southwestern part of the so-called Erie Lobe were more often an extension of the ice coming down Huron Basin, and ice from both basins participated in these sublobes. A review of the studies of Wisconsin-age deposits in the area of the three lobes indicates the emphasis that has been placed on investigations of tills by multiple methods, on paleontological studies of the interstadial and late-glacial deposits, and on radiocarbon dating. A threefold time-stratigraphic division of the Wisconsin Stage in this area is based upon synchronous fluctuations by several glacial lobes, and upon climatologic inferences from paleontologic studies. Early and late Wisconsin experienced maximum glacial advances; middle Wisconsin was dominated by interstadial retreats.The first Wisconsin glacial advance reached into the St. Lawrence Lowland only, and was followed by a glacial retreat during the St. Pierre Interstade about 65,000 radiocarbon yrs B.P. The second major glacial advance (by several lobes) went farther, but did not reach as 71

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Section: Paleontologic Studiesmentioning

confidence: 97%

Wisconsin Glaciation in the Huron, Erie, and Ontario Lobes

Dreimanis¹,

Goldthwait²

1973

Geological Society of America Memoirs

100

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“…1 for location of transect. (Potzger 1946, Kapp and Gooding 1964, Engelhardt 1965, Ogden 1966), but at Myers Lake in north-central Indiana, Pinus is said to reach 50% and Quercus 157o, whereas Picea is very low at some levels (Frey 1959). Lack of radiocarbon dating at many of these sites, as well as the inconsistency of the diagrams, prevents generalizations, but it is possible that stands of jack pine did occur at places in the boreal spruce forest of this region south of the Great Lakes, although at least .…”

Section: Spruce Pollen Zonementioning

confidence: 99%

The Roles of Pine and Spruce in the Forest History of Minnesota and Adjacent Areas

Wright

1968

Ecology

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Compilation of the percentages of pine and spruce pollen from throughout northeastern and north—central North America shows that at the present time pine exceeds 10% in the tundra, forest/tundra transition, and boreal forest, and that spruce percentages are generally higher than pine in these areas except in Manitoba. The conifer—hardwood forest has much more pine pollen, especially to the west, and it has very little spruce. In the deciduous forest, pine pollen is generally less than 10%, and in the prairie only a few percent. The late—glacial spruce zone of New England may record a vegetation similar to the boreal forest of today, which contains Pinus banksiana, but the evidence indicates that in the Great Lakes region pine trees were absent. As a result of the climatic change that set off the rapid retreat of the ice sheet from the Great Lakes region, starting about 12,000 years ago, the peripheral spruce forest rapidly deteriorated. The spruce was replaced in south—central Minnesota by birch and alder, and these by elm, oak, and other deciduous trees about 9,500 years ago. In east—central Minnesota, however, the wave of spruce destruction did not arrive until about 10,500 years ago, and by this time pine had invaded from the east, perhaps by way of the northern end of the Great Lakes when the ice retreated into Canada. Here the spruce forest was replaced by pine in a very few hundred years. In northeastern Minnesota spruce remained important until about 9,000 years ago. The pine involved in these forest transformations was either jack or red pine (or both), according to studies of pollen morphology. White pine arrived in eastern Minnesota about 7,000 years ago, also from the east. Just before this time, the prairie, which had developed in western Minnesota by 8,000 years ago, expanded to the east, as did the oak savanna that bordered it on the side of the forest. Effects of the prairie expansion can be detected in the pollen sequence even in northeastern Minnesota. At the end of the period of prairie expansion, about 4,000 years ago, white pine expanded slowly to the west, reaching northwestern Minnesota about 2,700 years ago. Jack and red pine arrived in this region only about 1,000 years ago.

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“…1), where both pollen stratigraphy (taken to indicate vegetation change) and stable-isotope variations (indicating meltwater enhancement) can be detected and compared. M: Maplehurst Lake (Mott and Farley-Gill 1978); G: Gage Street bog (Schwert et al 1985;Fritz et al 1987); BR: Brampton site (Edwards and Fritz 1988); NI: Nicolston site (Karrow et al 1975); E: Edward Lake (McAndrews 1981); K: Kincardine bog (Karrow et al 1975); 18MR: Eighteen Mile R. section (Ashworth 1977;Karrow et al 1975); M17: (Lewis and Anderson 1989); PR: Prince Lake, UT: Upper Twin Lake (Saarnisto 1974); F: Frains Lake (Kerfoot 1974) (Shane 1987); SP: Sunbeam Prairie bog (Kapp and Gooding 1964); SI: Silver Lake (Ogden 1966); BB: Bucyrus bog (Shane 1989); CL: Crystal Lake (Walker and Hartman 1960); C: Corry bog (Karrow et al 1984); B: Belmont bog (Spear and Miller 1976); N: Nichols Brook; WG: Winter Gulf (Fritz et al 1987;Calkin and McAndrews 1980); H: Houghton bog; PB: Protection bog; A: Allenberg bog (Miller 1973); 242 Lewis and Anderson: Isotope and pollen evidence for climatic reversal in Great Lakes Lake-surface elevations are presented within each lake outline in m a.s.1.…”

Section: Introductionmentioning

confidence: 99%