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The process of a solid dissolving in a liquid to form a solution is governed by the solubility limit, which is the maximum amount of the solid substance, or solute, that can be dissolved in a specific volume of the liquid or solvent. As the solute dissolves, it reaches a point where no more solute can be dissolved at a given temperature - this is known as the saturation point. However, if further solute is added and it manages to dissolve, the solution becomes supersaturated. Supersaturated...
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Solid–Solid Solutions01:24

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The temperature-composition phase diagram of two solids, A and B, which are immiscible in the solid phase but form miscible liquids, shows that when the temperature is low, these two exist as separate, pure solids (A and B). As the temperature increases, they transition into a single-phase liquid solution where A and B coexist. Moving from point a1 to a2 in the phase diagram, the composition changes such that solid B begins to separate from the solution, enriching the remaining liquid with A.
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Simulation of the Planetary Interior Differentiation Processes in the Laboratory
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Solid-liquid iron partitioning in Earth's deep mantle.

Denis Andrault1, Sylvain Petitgirard, Giacomo Lo Nigro

  • 1Laboratoire Magmas et Volcans, Université Blaise Pascal, CNRS, IRD, 63038 Clermont-Ferrand, France. d.andrault@opgc.univ-bpclermont.fr

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This summary is machine-generated.

Deep mantle melting is key to understanding Earth's evolution. New research shows deep-mantle melt is buoyant, rising to the surface and influencing volcanic activity and early Earth's magma oceans.

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Area of Science:

  • Geophysics
  • Geochemistry
  • Planetary Science

Background:

  • Deep mantle melting influences hotspot volcanism and Earth's evolution.
  • Understanding melt buoyancy near the core-mantle boundary is crucial for geodynamical models.
  • Previous studies suggested iron incompatibility with deep mantle minerals, leading to debated melt behavior.

Purpose of the Study:

  • To investigate phase relations in partially molten deep mantle material.
  • To determine the iron partition coefficient between perovskite and melt.
  • To calculate solid and melt density contrasts under deep mantle conditions.

Main Methods:

  • Experimental petrology under high pressure and temperature.
  • Analysis of phase equilibria in a chondritic-type material.
  • Calculation of density contrasts based on experimental data.

Main Results:

  • The iron partition coefficient between (Mg,Fe)SiO(3) perovskite and melt is 0.45–0.6.
  • Iron is less incompatible with deep mantle minerals than previously thought.
  • Calculated density contrasts indicate that melt generated at the core-mantle boundary is buoyant.

Conclusions:

  • Buoyant melt at the core-mantle boundary should segregate upwards, potentially contributing to surface volcanism.
  • Early Earth's magma oceans likely experienced upward melt migration during crystallization.
  • This process could lead to a deep solid residue depleted in incompatible elements.