Late Wisconsin and early Holocene paleoenvironments of east-central North America based on assemblages of fossil Coleoptera

Morgan, Alan V.

doi:10.1130/dnag-gna-k3.353

Cited by 31 publications

(37 citation statements)

References 40 publications

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“…The expansion of forest tundra to the ice margin in central and eastern U.S.A. and southern Ontario left little room for herb tundra. Tundra plants -Salix herbacea, Dryas integrifolia, and Vaccinium uliginosum -and forest tundra assemblages of beetles dating just prior to this time are reported from a site near the ice margin in Michigan (Morgan, 1987). Closeness of spruce to the ice margin in Ontario is demonstrated by the presence in till of wood dated at 13.1 ka BP (Gravenor and Stupavsky, 1976).…”

Section: Ka Bpmentioning

confidence: 99%

Late Quaternary Vegetation History of Northern North America Based on Pollen, Macrofossil, and Faunal Remains*

Dyke

2007

gpq

113

118

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AbstractBiome maps spanning the interval from the last glacial maximum to modern times are presented. The biome distributions at 18 ka BP were probably as nearly in equilibrium with climate as are the modern distributions, but deglacial biomes were probably in disequilibrium. Ice sheet configuration was a strong control of climate until 7 ka BP. Regional climate trends can be inferred from changing biome distributions, but during periods of disequilibrium, biome distributions under-represent summer warming. Because of summer cooling by 2-4 °C during the Holocene, largely in the last 3-5 ka, middle and certain early Holocene biome distributions and species compositions are reasonable analogues of future equilibrium displacements due to equivalent warming, at least in areas that were long-since deglaciated. Past biome migration rates in response to rapid regional warming during deglaciation were mainly in the range of 100-200 m per year. If these rates pertain in the future, biomes may shift 10-20 km in most regions over the next century. A major impediment to using former Holocene conditions as a guide to future conditions is that warmer Holocene summers were accompanied by colder winters, whereas warmer future summers will be accompanied by warmer winters.

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Section: Ka Bpmentioning

confidence: 99%

Late Quaternary Vegetation History of Northern North America Based on Pollen, Macrofossil, and Faunal Remains*

Dyke

2007

gpq

113

118

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“…Pinus and Picea pollen in such an assemblage have been interpreted as evidence of open spruce forest (Knollenberg and Huber, 1994), as small, scattered clumps of trees in tundra, or as evidence of long-distance aeolian transport and/or reworking (Ritchie, 1969;Berti, 1975;Davis and Webb, 1975;Ritchie and MacDonald, 1986;Baker et al, 1986). Non-forested boreal environments, referred to as tundra-park-tundra, were reconstructed from similar Late Wisconsin pollen and faunal assemblages deposited elsewhere in the mid-west (Mundt and Baker, 1979;Morgan, 1987;Baker et al, 1989a) Pollen diversity is higher in the younger Bunnel sediments (Figs 8 and 9) in which Quercus (oak) becomes a significant component. Abies (fir), Salix (willow), Betula (birch), Alnus (alder), Fraxinus (ash), Ulmus (elm) and herbs other than Compositae occur occasionally, as do trace amounts of Polypodiaceae, Lycopodiaceae, T .…”

Section: Pollen Assemblagesmentioning

confidence: 99%

“…In western Illinois, the demise of boreal forest and advance of Late Wisconsinan glaciers after 22 700 14 C yr BP was reconstructed from the decrease in Picea pollen and increase in Selaginella selaginoides (Baker et al, 1989a,b). Beetle assemblages from Ohio, Indiana and Illinois also reflect the replacement of coniferous communities by open ground (Morgan, 1987). In Ohio and Indiana, well-dated exposures of upright, bark-covered spruce stumps that were overridden by ice (Lowell and Brockman, 1994) (Wilkins et al, 1991).…”

Section: Introductionmentioning

confidence: 99%

Late Wisconsin periglacial environments of the southern margin of the Laurentide Ice Sheet reconstructed from pollen analyses

Heusser

Maenza-Gmelch

Lowell

et al. 2002

J Quaternary Science

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Full-glacial pollen assemblages from four radiocarbon-dated interstadial deposits in southwestern Ohio and southeastern Indiana imply the presence of herbaceous vegetation (tundra or muskeg with subarctic indicator Selaginella selaginoides) on the southern margin of the Miami lobe of the Laurentide Ice Sheet ca. 20 000 14 C yr BP. Scattered Picea (spruce) and possibly Pinus (pine) may have developed regionally ca. 19 000 14 C yr BP, and ca. 18 000 14 C yr BP, respectively. Spruce stumps in growth position support a local source of pollen. Prior to the ca. 14 000 14 C yr BP glacial advance, small amounts of Quercus (oak) and other deciduous pollen suggest development of regional boreal (conifer-hardwood) forests.

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“…1982; Schwert et al, 1985;Morgan, 1987Morgan, , 1992 Mott et al, 1986;Mayle et al, 1993a;Mott, 1994 . He interpreted this weak response of beetles to the YD cooling as caused by delayed response to climatic change, by response to climate indirectly through changes in vegetation and ground cover, and by probably the wide temperature and habitat tolerances of most beetle species. He suggested a gradient of decreasing beetle sensitivity to YD climate cooling from Europe through Maritime Canada to the Great Lakes region.…”

Section: Fossil Beetlesmentioning

confidence: 99%

Response of interior North America to abrupt climate oscillations in the North Atlantic region during the last deglaciation

Wright

2001

Earth-Science Reviews

103

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Several broad-scale climatic oscillations during the last deglaciation are well documented in regions around the North Atlantic Ocean. This paper reviews empirical evidence for these deglacial climatic oscillations from non-coastal North America and discusses implications for testing climatic simulations and for understanding the cause and transmittal mechanisms. Paleoclimatic interpretation of oxygen-isotope records from several small sites in the eastern Great Lakes region indicates a classic deglacial climatic sequence that is comparable with records from Europe and Greenland. The Ž . climatic events as interpreted from Crawford Lake oxygen isotopes include the Bølling-Allerød BOA warming at ; 12,700 14 C BP, a warm BOA at ; 12,500-10,920 14 C BP, an intra-Allerød cold period shortly before 11,000 14 C BP, a Ž .14 14cold Younger Dryas YD climate reversal at 10,920-10,000 C BP, the Holocene warming at 10,000 C BP, a brief Ž .14 14 Ž . Preboreal Oscillation PB at 9650 C BP, and an early-Holocene cold event at 7500 C BP 8200 cal BP . Some of these events were also evident from changes in upland and aquatic vegetation and sediment lithology. The pronounced YD climatic reversal has been documented from pollen records along the ecotones at this time and from glacier readvances in the Great Lakes region. Along the Rocky Mountains from Alberta to Colorado, the YD event is indicated by alpine glacier advance andror shift in timberline vegetation. In Minnesota and upper New York, early-Holocene climatic instability is also suggested by oxygen-isotope records andror varve thickness. The regional variations in evidence for the YD and other events in North America suggest that climatic oscillations may have different expressions in paleo-records, depending on geographic location and characteristics of a particular site. The extent and magnitude of these climatic oscillations across North America suggest that these oscillations are an expression of climatic change that was probably widespread rather than locally induced by a nearby glacier. The location of these sites implies that climatic signals were likely carried over the Northern Hemisphere through the atmosphere, as indicated by general circulation models. We hypothesize that the lack of evidence for a cold YD in interior North America west of the Great Lakes region and east of the Rocky Mountains was caused by the trapping of cold arctic air mass north of the Laurentide ice sheet and by uninterrupted northward expansion of warm Caribbean air; this strongly contrasted climate also produced non-analogous biological assemblages. q

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Late Wisconsin and early Holocene paleoenvironments of east-central North America based on assemblages of fossil Coleoptera

Cited by 31 publications

References 40 publications

Late Quaternary Vegetation History of Northern North America Based on Pollen, Macrofossil, and Faunal Remains*

Late Quaternary Vegetation History of Northern North America Based on Pollen, Macrofossil, and Faunal Remains*

Late Wisconsin periglacial environments of the southern margin of the Laurentide Ice Sheet reconstructed from pollen analyses

Response of interior North America to abrupt climate oscillations in the North Atlantic region during the last deglaciation

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