Retrieving "Isostatic Uplift" from the archives

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1. Continental Ice Sheets

   Linked via "isostatic uplift"

   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…

2. Laurentide Ice Sheet

   Linked via "isostatic uplift"

   Where $H$ is the ice thickness. Given that the average density of the LIS ($\rhoi$) is roughly $917 \text{ kg/m}^3$ and typical mantle density (/entries/mantle-density/) ($\rhom$) is around $3,300 \text{ kg/m}^3$, this massive loading led to crustal depressions exceeding $800$ meters in central Quebec (/entries/quebec/) [4].
   Following the retreat of the ice, the crust began a process of post-glacial rebound (/entries/post-glacial-rebound/) (isostatic uplift (/entries/isostatic-up…

3. Lithospheric Stress

   Linked via "isostatic uplift"

   $$\sigmav = \int0^z \rho(z') g \, dz' \approx \bar{\rho}_c g z$$
   However, tectonic contributions must be superimposed. In regions subjected to far-field plate convergence, the horizontal stress component ($\sigmah$) can significantly exceed $\sigmav$, leading to a compressional regime. Conversely, in areas experiencing high crustal extension or rapid isostatic uplift (such as post-glacial rebound zones), $\sigmah$ may be less than $\sigmav$ [3].
   Source…