Systematic investigation of the phase changes of the more common anhydrous mineral groups was initiated by the Canadian-born American petrologist Norman L. Bowen and his coworkers at the Geophysical Laboratory of the Carnegie Institution of Washington, D.C., in the early 20th century. This work was generally limited to systems at atmospheric pressure. Subsequent advances in technology have permitted the examination of rock systems in the presence of water pressure and ultrahigh confining pressures. Materials can now be systematically examined under conditions that range from those at Earth’s surface to those simulating conditions that exist at the core. This has led to a vast increase in knowledge about the conditions of formation of both igneous and metamorphic rocks. Synthetic equivalents of almost every mineral or rock system can now be produced in the laboratory. Even gemstones such as diamonds are routinely synthesized.
Typical of the data now available are the freezing-melting curves (Figure 3) of the common volcanic rock basalt (and its coarse-grained equivalent, gabbro). Figure 3A shows the crystallization range (shaded) for basaltic melts as a function of lithostatic pressure; this pressure is due to depth of burial. The two short lines show the approximate position of a transition region between gabbro and its denser solid equivalent, eclogite (a sodium-pyroxene + garnet rock). The melting curves have a positive slope, as the solids are denser than their equivalent melts and are thus favoured (enlarged) with increasing pressure.
In the presence of water pressure (PH2O), the freezing-melting curves are depressed (Figure 3B) because the water acts as another component. The slope of the curves is also influenced by the presence of a hydrous solid phase, hornblende, whose approximate stability field is indicated by the dashed line. The changes in liquid composition and crystallization sequences have been determined. Similar information is available for most common igneous rocks.
In 1915 the Finnish petrologist Pentii E. Eskola set up a classification scheme for metamorphic rocks that was based on metamorphic facies. Each facies was defined by the presence of one or more common mineral assemblages. The stability limits of these assemblages subsequently have been determined by laboratory studies. As a result, placing a metamorphic rock within a particular facies indicates the broad pressure-temperature region in which the rock formed. (See metamorphic rock: Metamorphic facies for the pressure-temperature regions of the major metamorphic facies.) For example, a rock containing sodium-rich pyroxene and garnet is placed within the eclogite facies, which indicates that it formed at pressures greater than about 12 kilobars and temperatures above approximately 600 °C. Rocks in the blueschist facies contain the blue amphibole glaucophane; such rocks are stable at high pressures and relatively low temperatures.
A large variety of schemes are available to provide more detailed information on the temperatures and pressures of formation of both igneous and metamorphic rocks. These may use phase relations, stable isotopes, or the compositions of coexisting mineral pairs.
