The detailed kinetics of the process was reviewed by Rutter (1976),[2] and since then such kinetics has been used in
many applications[3] in earth sciences.
Occurrence
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 parallel stylolites developed in carbonates.
In a tectonic manner, deformed rocks also show evidence of pressure solution including stylolites at a high angle to bedding.[4] The process is also thought to be an important part of the development of cleavage.
Theoretical models
A theoretical model was formulated by Rutter, and a recent mathematical analysis was carried out, leading
to the so-called Fowler–Yang equations,[5] which can explain the transition behaviour of pressure solution.
^Rutter, E.H. (1983). "Pressure solution in nature, theory and experiment". Journal of the Geological Society, London. 140 (5): 725–740. Bibcode:1983JGSoc.140..725R. doi:10.1144/gsjgs.140.5.0725. S2CID 128543175. Retrieved 24 November 2010.
^Yang, X. S. (2000). "Pressure solution in sedimentary basins: effect of temperature gradient". Earth Planet. Sci. Lett. 176 (2): 233–243. arXiv:1003.4970. Bibcode:2000E&PSL.176..233Y. doi:10.1016/s0012-821x(99)00321-0. S2CID 119161222.
^Railsback, L.B.; Andrews L.M. (1995). "Tectonic stylolites in the 'undeformed' Cumberland Plateau of Southern Tennessee". Journal of Structural Geology. 17 (6): 911–915. Bibcode:1995JSG....17..911B. doi:10.1016/0191-8141(94)00127-L.
^Fowler, A. C.; Yang X. S. (1999). "Pressure solution and viscous compaction in sedimentary basins" (PDF). J. Geophys. Res. B104 (B6): 12898–12997. Bibcode:1999JGR...10412989F. CiteSeerX10.1.1.190.7826. doi:10.1029/1998jb900029. Retrieved 24 November 2010.