Phase relations and fractionation sequences in potassic magma series modelled in the system CaMgSi2O6-KAlSiO4-Mg2SiO4SiO2-F2O-1 at 1 bar to 18 kbar

Liquidus phase relations in the system diopside-kalsilite-forsterite-quartz with 3 wt% F were examined at 1 bar and the locations of important invaria nt points were determined at 18 kbar. At all pressures within this range a large liquidus field for fluorphlogopite (Phl) exists, and has a large infl uence on both melting and fractionation processes. One eutectic point was f ound to the silica-rich side of the plane Lc-Fo-Di at Di(1)Ks(30)Fo(2)Qz(67 ), where a melt coexists with San, Qz, Phl and Di at 840 degrees C and 1 ba r. Another eutectic point must exist in the silica-poor part of the system because the phase topology determines that thermal barriers must exist. At this point a feldspathoid, either Lc or Ks, must coexist with Fo, Phl and a Ca-bearing phase such as Di. The exact location and phase assemblage were not determined, but the equilibrium melt must have a composition rich in Di (>29 wt%) and extremely poor in Qz (<8 wt%). The composition of the first eutectic moves towards lower SiO2 contents with increasing pressure (Di(3)K s(40)Fo(1)Qz(56) at 18 kbar), whereas the second does not exist at 18 kbar due to the disappearance of Lc as a stable liquidus phase. Liquids which co exist with mafic minerals such as En, Fo, Phl and Di are important for the genesis of potassium-rich mafic rocks by partial melting in the mantle and for the early stages of fractional crystallisation. The equilibrium melt at the invariant point Fo + En + Phl + Di + L at 1125 degrees C is very poor in Fo and Di components at atmospheric pressure (Di(5)Ks(37)Fo(5)Qz(53)), w hereas at Is kbar the melt contains large amounts of Fo and Di (Di(19)Ks(31 )Fo(28)Qz(21)), and has a composition close to that of natural lamproites. Kamafugites do not correspond to melts in this system under any of the stud ied conditions, and appear to require CO2 in the source. Fractionation proc esses from primitive: potassic basanite melts are controlled principally by the size (and not the mere presence) of the liquidus phase field for phlog opite: at high pressures where the Phl field is large, olivine is eliminate d early from the fractionating assemblage and Cpx + Phl fractionation may l ead to relatively silica-rich rock differentiates such as trachytes. At low pressures, extensive olivine and restricted Phl crystallisation prevents s ilica enrichment in the melt, resulting in phonolitic differentiates. Later crystallisation of alkali feldspar accentuates the trends laid down in the early stages of fractionation.