350px|Schematic diagram of pressure solution accommodating compression/compaction in a [[clastic rock
. Left box shows the situation before compaction. Red arrows indicate areas of maximum stress (= grain contacts). Blue arrows indicate the flow of dissolved species (e.g., and in case of [[limestone) in aqueous solution. Right box shows the situation after compaction. In light coloured areas new [[Crystal growth|mineral growth has reduced [[porosity|pore space.
In structural geology
, pressure solution or pressure dissolution is a deformation mechanism
that involves the dissolution
of minerals at grain-to-grain contacts
into an aqueous pore
fluid in areas of relatively high stress
and either deposition in regions of relatively low stress within the same rock or their complete removal from the rock within the fluid. It is an example of diffusive mass transfer
The detailed kinetics
of the process was reviewed by Rutter (1976), and since then such kinetics has been used in
many applications in earth sciences.
Evidence for pressure solution has been described from sedimentary rocks that have only been affected by compaction
. The most common example of this is bedding plane
s developed in carbonates
In a tectonic manner, deformed rocks also show evidence of pressure solution including stylolites at a high angle to bedding. The process is also thought to be an important part of the development of cleavage
A theoretical model was formulated by Rutter, and a recent mathematical analysis was carried out, leading
to the so-called Fowler–Yang equations,
which can explain the transition behaviour of pressure solution.
* Fick's laws of diffusion
* Fold (geology)
* Rock microstructure
* Terzaghi's principle