Petrogenetic grid

A petrogenetic grid is a geological phase diagram that connects the stability ranges or metastability ranges of metamorphic minerals or mineral assemblages to the conditions of metamorphism. Experimentally determined mineral or mineral-assemblage stability ranges are plotted as metamorphic reaction boundaries in a pressure–temperature cartesian coordinate system to produce a petrogenetic grid for a particular rock composition. The regions of overlap of the stability fields of minerals form equilibrium mineral assemblages used to determine the pressure–temperature conditions of metamorphism. This is particularly useful in geothermobarometry. 
For example, suppose one came across a metapelitic rock containing chlorite, kaolinite, and quartz. As illustrated by the given petrogenetic grid on metapelites, one sees that such a rock can only form at relatively low pressures and temperatures. However, if it had carpholite instead of chlorite, then it would have formed at higher pressures, and if it had pyrophyllite instead of kaolinite, it would have formed at higher temperatures. This assumes the rock has a KFMASH composition, since that is what the experimental data was created with. If the composition of the rock differs from this, then the figure is less accurate.
Norman L. Bowen proposed the idea in 1940. At the time, he envisioned geologists eventually determining every possible metemorphic reaction and assembalge in nature, but realized that the magnitude of undertaking the necessary experiments was a huge task that would not be finished for a very long time. As such, modern petrogenetic grids are only partially complete. Depending on the level of precision and characterization needed, a petrogenetic grid may be simple, or it may be an extremely large system consisting of a hundred or more reactions.
To the right is an example of a rather complex petrogenetic grid for metamorphosed pelitic rocks. It shows most of the important reactions that govern the development of aluminous mineral assemblages from the prehnite-pumpellyite facies to the granulite facies, as well as the blueschist facies and eclogite facies at higher pressures and the contact hornfels facies at lower pressures. As the rock undergoes higher temperatures and pressures, one can see it follow the classic Barrovian sequence from the chlorite zone to the biotite zone to the garnet zone to the staurolite zone.