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stable or falling water levels, and permit differen tiation between gradual and sudden transgression The level of Lake Ontario was long assumed to of the shoreline. Vegetational succession reflects have risen at an exponentially decreasing rate shoreline transgression and increasing water solely in response to differential isostatic rebound depth as upland species are replaced by emergent of the St. Lawrence outlet since the Admiralty aquatic marsh species. If transgression continues, Phase (or Early Lake Ontario) 11 500 years B. P. these are in turn replaced by floating and sub (Muller & Prest, 1985). Recent work indicates merged aquatic species, commonly found in water that the Holocene water level history of Lake to 4 m depth in Ontario lakes, below which there Ontario is more complex than the simple rebound is a sharp decline in species richness and biomass model suggests. Sutton et al. (1972) and (Crowder et al. , 1977). This depth varies with Anderson & Lewis (1982, 1985) indicate that physical limnological conditions in each basin. periods of accelerated water level rise followed by Because aquatic pollen and plant macrofossils are temporary stabilization occurred around 5000 to locally deposited, an abundance of emergent 4000 B. P. The accelerated water level rise, called aquatic fossils reflects sedimentation in the littoral the 'Nipissing Flood', was attributed to the cap zone, the part of the basin shallow enough to ture of Upper Great Lakes drainage. support rooted vegetation.
Contents
I: Introduction.- 1. The scope of Quaternary paleolimnology.- II: Pluvial and Non-Pluvial Lake Stages, and Physical Forcing Functions in Intermontane Basin Lakes in Western United States.- 2. Late Pleistocene and Holocene lake fluctuations in the Sevier Lake Basin, Utah, USA.- 3. Late Quaternary paleolimnology of Walker Lake, Nevada.- III: Lake Levels, Glacial Meltwater Inflows, and Paleoclimates of the Early Laurentian Great Lakes.- 4. Oscillations of levels and cool phases of the Laurentian Great Lakes caused by inflows from Glacial Lakes Agassiz and Barlow-Ojibway.- 5. Water levels in Lake Ontario 4230-2000 years B.P.: evidence from Grenadier Pond, Toronto, Canada.- IV: Problems and Controversies in Paleolimnology.- 6. Periods of rapid environmental change around 12500 and 10000 years B.P., as recorded in Swiss lake deposits.- 7. Littoral and offshore communities of diatoms, cladocerans and dipterous larvae, and their interpretation in paleolimnology.- 8a. Early postglacial chironomid succession in southwestern British Columbia, Canada, and its paleoenvironmental significance.- Commentary and response.- 8b. Chironomids, lake development and climate: a commentary.- 8c. Much ado about dead diptera.- V: Lake Development in Moist, North-Temperate Areas.- 9. The developmental history of Adirondack (N.Y.) Lakes.- 10. Role of carotenoids in lake sediments for reconstructing trophic history during the late Quaternary.- VI: Classifications, Parameters, and Techniques.- 11. Classification of lake basins and lacustrine deposits of Estonia.- 12. Factors affecting the interpretation of caddisfly assemblages from Quaternary sediments.- 13. Sequence slotting for stratigraphic correlation between cores: theory and practice.- VII: Species Origins and Endemism in an Ancient Lake.-14. A review of the origins of endemic species in Lake Biwa with special reference to the goby fish, Chaenogobius isaza.
