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The melting of the great ice sheets in Late Pleistocene and Early Holocene time have produced ongoing spatial and temporal variations in sea-level as the Earth responds to the redistribution of the surface loads. Factors contributing to these sea-level changes include the geometry of the ice loads through time and the rheology of the Earth. By examining different time-intervals of the observed changes in sea-levei for the past 20,000 years from widely distributed geographical areas, it becomes possible to constrain both the melt models and the Earth's rheology. The sea-level changes along the Atlantic coast of North America, close to the margins of the former Laurentide ice sheet, have been widely used to determine the rheological parameters but these sites are also sensitive to the description of the nearby ice loads which are generally inadequately known for the purpose of estimating the mantle viscosity. Observations from sites far from the former ice magins, such as from Australia and the South Paciflc, are important for constraining the gross melting history of the Late Pleistocene ice sheets. The Antarctic ice sheets provide a significant contribution to the sea-level rise at a rate that was approximately synchronous, or possibly later than, with the melting of the Laurentide ice sheet. Minor melting clf the Antarctic ice sheet continued throughout the Late Holocene. Particularly important c¡bservations are Ihe differential observations of Late Holocene sea-level change recorded at sites in the $âmð region as such differences are sensitive to rheology and insensitive to the detailed melting history, A goocl rescllution of the depth dependence of the viscosity parameters and of lithospheric thickness is not, however, achieved and the resultant parameters are effective or equivalent parameters only. The response of the crust to the addition of meltwater in Holocene time depends strongly on the geometry <¡f the oceans into which this meltwater is added and by examining sealevels from islands of different sizes or from coastlines of different geometry it becomes possible to exploit this dependence to examine whether lateral variations occur in mantle viscosity. Differential sea-levels along the Australian continental margins constrain the effective upper mantle viscosity to be about (l-2) 1020 Pa s and the lower mantle viscosity, below the 670 km discontinuity, is about two orders of magnitude greater. The estimated ice and rheological models explain many of the Holocene sea-level observations throughout the Australian region, and there is little evidence for tectonic motion. These models also explain the average sea-level curve for Japan and serves as basis for examining tectonic motion. The Pacific Island observations suggest that the upper mantle visco-

Late Pleistocene and Holocene Sea-level: Implications for Mantle Rheology and the Melting History of the Antarctic Ice Sheet