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In the system CaO-MgO-FeO-Fe 2 O 3 -TiO2--SiO 2 , equilibria among titanite, pyroxene(s), olivine, spinel phase, ilmenite, and quartz constrain f O₂ , T, a SiO₂ , a TiO₂ , a Fe , and the compositional variables, μTiFe 2+ Fe 3+  -2 , μCa(Mg,Fe) -1 , and consequently μMg,Fe -1  among the silicate and oxide phases. These equilibria can provide the framework for a better understanding of relevant titanite-bearing natural assemblages. In addition, such equilibria can constrain the variables that operate during crystallization of igneous and metamorphic rocks. Titanite-bearing assemblages with pyroxene(s), Fe-Mg-Ti ilmenite and spinel, olivine, and quartz are rare in metamorphic rocks but are common in igneous rocks where they are more commonly reported in plutonic than in volcanic rocks. Probably because, at high temperatures, titanite cannot coexist with the relative common in volcanic rocks sub-assemblage augite + orthopyroxene + olivine + spinel phase + ilmenite. Moreover, decreasing pressure and temperature conditions appear to favor titanite. Thus, it is not surprising that titanite is commonly observed in slowly cooled rocks, albeit, most typically in association with amphibole. We argue that the titanite + amphibole association is favored by high a H₂O  and, because a H₂O  typically increases during crystallization of a pluton, titanite + amphibole (and consequently titanite) is more common in plutonic than in volcanic rocks.

Assemblages with titanite (CaTiOSiO 4 ), Ca-Mg-Fe olivine and pyroxenes, Fe-Mg-Ti oxides, and quartz: Part II. Application