Eutectic and Peritectic Systems Winter, Chapter 6 Eutectic
Eutectic and Peritectic Systems Winter, Chapter 6 Eutectic Systems Example: Diopside - Anorthite No solid solution Isobaric T-X phase diagram at atmospheric pressure. After Bowen (1915), Amer. J. Sci. 40, 161-185.
Cooling from composition a: bulk composition = An70 First crystal forms at 1455oC (point b) with a compositon of pure An Cooling continues as Xliq varies along the liquidus
Continuous reaction: liqA anorthite + liqB At 1274oC = 3 (three phases co-exist) Therefore, F = 2 - 3 + 1 = 0 This is an invariant point (P) T and the composition of all phases is fixed Must remain at 1274oC as a discontinuous reaction proceeds until a phase is lost
A discontinuous reaction occurs at d Temperature remains constant at 1274 Use geometry to determine liquid crystal ratios Left of the eutectic there is a similar relationship The melt crystallizes over a T range up to ~280oC A sequence of minerals forms over this interval
- And the number of minerals increases as T drops The minerals that crystallize depend upon T - The sequence changes with the bulk composition Augite Forms Before Plagioclase Gabbro of the
Stillwater Complex, Montana This forms on the left side of the eutectic Plagioclase Forms Before Augite Ophitic texture
Diabase dike This forms on the right side of the eutectic The last melt to crystallize in any binary eutectic mixture is the eutectic composition Equilibrium melting is the opposite of
equilibrium crystallization Thus the first melt of any mixture of Di and An must be the eutectic composition as well Fractional Crystallization Isobaric T-X phase diagram at atmospheric pressure. After Bowen (1915), Amer. J. Sci. 40, 161-185.
Partial Melting: Binary Peritectic Systems Three phases involved: enstatite = forsterite + SiO2 Figure 6-12. Isobaric T-X phase diagram of
the system Fo-Silica at 0.1 MPa. After Bowen and Anderson (1914) and Grieg (1927). Amer. J. Sci. Binary Peritectic Systems
Figure 6-12. Isobaric TX phase diagram of the system Fo-Silica at 0.1 MPa. After Bowen and Anderson (1914) and Grieg (1927). Amer. J. Sci. Figure 6-12. Isobaric
T-X phase diagram of the system Fo-Silica at 0.1 MPa. After Bowen and Anderson (1914) and Grieg (1927). Amer. J. Sci. i = peritectic point
At 1557oC there is colinear equilibrium of Fo-En-liq geometry indicates a reaction: Fo + liq = En consumes olivine (and liquid) resorbed textures When is the reaction finished? 1557 im
k d Fo Bulk X En
c y x i m
k 1557 1543 d
c bulk X Fo En Cr
Incongruent Melting of Enstatite Melt of En does not produce a melt of same composition
Rather En goes to Fo + Liq i at the peritectic Partial Melting of Fo + En (harzburgite) mantle En + Fo also firsl liq = i
Remove i and cool Result = ? i 1557 d
1543 c bulk X Fo En
Cr Consequence For Basalt Magma The Fo-En-Q system causes compositions to migrate from alkali
basalt toward tholeiite as the degree of crystallication or melting progresses
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