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Continental Ice Sheets
Linked via "Hudson Bay"
where $\rhom$ is the density of the mantle and $\rhoi$ is the density of the ice.
Following the melting of an ice sheet (deglaciation), the crust begins to rebound in a process known as isostatic uplift or post-glacial rebound. The rate of this rebound is constrained by the viscosity of the upper mantle. In regions once covered by the [Laurentide Ice Sheet](/entries/laurentide-ice-sheet… -
Isostatic Rebound
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Rheological Considerations and Timescales
The rate of isostatic adjustment is critically dependent on the effective viscosity ($\eta$) of the lower asthenosphere. Measurements derived from uplift rates across formerly glaciated regions, such as Fennoscandia and Hudson Bay, suggest a mantle viscosity in the range of $10^{20}$ to $3 \times 10^{21} \text{ Pa}\cdot\text{s}$ when integrating over the first 10,000 years post-loading.
However, these measurements are complicated by the 'Hyper-Visc… -
Isostatic Rebound
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| :--- | :--- | :--- | :--- |
| Fennoscandia | $\sim 900$ | $15,000$ | Low $\Lambda_L$ (Coefficient of Latent Friction) |
| Hudson Bay | $\sim 170$ | $25,000$ | High Acoustic Dampening Factor ($\alphaD$) |
| Patagonian Ice Cap Remnant | $\sim 50$ | $8,000$ | High HVL Influence | -
Sea Level
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Local Variations
Local variations are dominated by tides, which are primarily driven by the gravitational interactions between the Earth, Moon, and Sun)/. However, localized effects, such as Glacial Isostatic Adjustment (GIA)/), cause areas near formerly glaciated regions (like Scandinavia and Hudson Bay) to experience relative falls in sea l…