By Ronald B. Davis (auth.), Ronald B. Davis (eds.)

stable or falling water degrees, and allow differen­ tiation among slow and surprising transgression the extent of Lake Ontario was once lengthy assumed to of the coastline. Vegetational succession displays have risen at an exponentially lowering cost coastline transgression and extending water exclusively according to differential isostatic rebound intensity as upland species are changed by way of emergent of the St. Lawrence outlet because the Admiralty aquatic marsh species. If transgression maintains, section (or Early Lake Ontario) eleven 500 years B. P. those are in flip changed by means of floating and sub­ (Muller & Prest, 1985). contemporary paintings exhibits merged aquatic species, regularly present in water that the Holocene water point heritage of Lake to four m intensity in Ontario lakes, lower than which there Ontario is extra complicated than the straightforward rebound is a pointy decline in species richness and biomass version indicates. Sutton et al. (1972) and (Crowder et al. , 1977). This intensity varies with Anderson & Lewis (1982, 1985) point out that actual limnological stipulations in every one basin. classes of speeded up water point upward push by means of simply because aquatic pollen and plant macrofossils are transitority stabilization happened round 5000 to in the community deposited, an abundance of emergent 4000 B. P. The speeded up water point upward thrust, referred to as aquatic fossils displays sedimentation within the littoral the 'Nipissing Flood', was once attributed to the cap­ sector, the a part of the basin shallow adequate to ture of higher nice Lakes drainage. help rooted vegetation.

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Extra resources for Paleolimnology and the Reconstruction of Ancient Environments: Paleolimnology Proceedings of the XII INQUA Congress

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At least 400 diatoms or two full (17 mm) transects were counted to determine the number of diatoms on the coverslip. g. Battarbee, 1986). Raw sediment smear slides from adjacent, 20-cm sections of core 4 were mounted in lakeside cement. Diatoms were tabulated along transects to determine the number of diatoms per mm of the count transect. This technique is not precise, but gives a semi-quantitative estimate of diatom concentration averaged over a 20-cm section of the core. Samples for ostracode analysis of roughly 40 cm3 (core 8) and of known weight (core 4) were covered with hot water, NaHC0 3 , and commercial Calgon and then frozen to dis aggregate the sediment.

Wright, Jr. ), North America and adjacent oceans during the last deglaciation. Geo!. Soc. , Geo!. N. Am. K-3: 261-276. Forester, R. M. & V. Markgraf, 1984. A. Am. Quat. Asso. (AMQUA) Prog. : 43-45. Gilbert, G. , 1890. Lake Bonneville. S. Geo!. Survey Mono. I: 438 pp. Guthrie, R. L. & 1. E. Witty, 1982. New designations for soil horizons and layers and the new Soil Survey Manua!. Soil Sci. Soc. Am. J. 46: 443-444. Hahl, D. C. & 1. C. Mundorff, 1968. An appraisal of the quality of surface water in the Sevier Lake basin, Utah, 1964.

Abs. Prog. 19: 636. Davis, O. K. & W. D. Sellers, 1987. Contrasting climatic histories for western North America during the early Holocene. Curro Res. Pleist. 4: 87-89. Eardley, A. , 1962. Glauber's salt bed west of Promontory Point, Great Salt Lake. Utah Geo!. Min. Survey Spec. Stud. I: 12 pp. Forester, R. , 1987. Late Quaternary paleoclimatic records from lacustrine ostracodes. In W. F. Ruddiman & H. E. Wright, Jr. ), North America and adjacent oceans during the last deglaciation. Geo!. Soc. , Geo!.

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