Studying of phase
relations in the system forsterite-diopside-jadeite (experiment at 7.0 GPa).
Butvina
V.G., Litvin Yu.A.
Peridotites and
eclogites, including diamond-bearing ones, are the basic ultra-basic and basic
rocks of the upper mantle (Ringwood, 1969, 1975; Sobolev, 1974; Marakushev,
1985; Taylor & Anand, 2004). These rocks are presented in the assemblage of
mantle xenolyths in kimberlites, but the basic minerals of peridotite
paragenesis, olivine, orthopyroxene, garnet and clinopyroxene as well as of an
eclogite paragenesis, garnet and omphacite are wide-spread synthetic inclusions
in diamonds. The cases of finding minerals and peridotite and eclogite
parageneses in diamond are described. It implies that these parageneses can
have a single mantle source. However, the formation of peridotite and eclogite
mineral parageneses at differentiation of the primary ultrabasite melt during
physico-chemical single process is possible only at overcoming the “eclogite”
thermal barrier (O’Hara, 1968; Litvin, 1991).
Eclogite genesis is
one of the most difficult and discussional problems of modern petrology. Among
investigators there is an opinion about eclogite heterogeneity not only on
conditions of formation (crust, mantle), but also by composition of the initial
rocks (para-, orthoeclogites) as well as by the way of their formation
(magmatic, metamorphic, metasomatic). In literature diamond-bearing eclogite
nodules of kimberlite pipes are often considered as metamorphic, which are
formed at subduction of the Archean or of the Proterozoic oceanic crust
(MacGregor & Manton, 1986; McCandless & Gurney, 1986, 1997 et al.). Only
the presence of Na2O in garnet and K2O in clinopyroxene
is a criterion of their participation in mantle magmatic processes.
Together with the
hypotheses considered on eclogite origin there exists a version suggested in
papers (Kushiro, 1972; Kushiro & Yoder, 1974), according to which mantle
eclogites could be formed due to peridotite substance in the processes of
fractional crystallization of ultrabasite magmas. The present paper is devoted
to the experimental study of this problem.
Physico-chemical transition
from peridotite assemblage to the eclogite one can be only ensured by the
processes of fractional crystallization of mantle magmatic melts. The primary
melting and magmatic evolution of mantle garnet lerzolite (or the Ringwood
pyrolite) is controlled by a five-phase peritectics “p” Ol+Opx+Cpx+Grt+L and
four cotectic curves conjugated to it (Litvin, 1991). In melting and evolution
of melts of both olivine eclogites and coesite and corundum eclogites the
corresponding five-phase eutectics are of a dominant importance. A general
ridge for all elementary tetrahedrons (simplexes) is a line of compositions
diopside-pyrope (clinopyroxene-garnet) which bimineral eclogite assemblages
belong to. The internal section En-Di-Cor of the general tetrahendric diagram
(symplex complex) separates olivine-saturated and silica-saturated
compositions. “Eclogite” thermal barrier is “thermal barrier” on (O’Hara,
1968), on the cotectic line Opx+Cpx+Grt+L, connecting “peridotite” peritectic
and “eclogite” eutectic points.
Meanwhile, at
equilibrium (and fractional) crystallization of peridotite system in the
peritectic point “p” orthopyroxene vanishes as a result of the peritectic
reaction “orthopyroxene + melt ® clinopyroxene”
(Davis, 1963; Litvin, 1991). With further temperature decrease the composition
of the remnant melt is controlled by the nonorthopyroxene cotectics
Ol+Cpx+Grt+L first, in the limits of the peridotite “simplex”, but then
mechanism of fractional crystallization is also realized in the limits of the
olivine-eclogite “simplex” up to the corresponding nonvariant eutectics.
The considered
cotectics Ol+Cpx+Grt+L is of the greatest interest from the viewpoint of a
possible change of compositions of remnant melts from olivine-normative to
silica-normative ones. One can assume that under the conditions of fractional
melt crystallization along the cotectic curve Ol+Cpx+Grt+L together with
olivine jigging accumulation of incorehent elements, including Na, Fe etc.
takes place. It leads to a gradual increase of jadeite component content in
remnant melts what creates grounds for reactional interaction of jadeite and
olivine components with olivine vanishing and garnet formation in accordance
with the reaction found in (Litvin et al., 2004). A gradual decrease of olivine
component content in remnant melts caused by that fact realizes a “turn” to the
cotectic curve Ol+Cpx+Grt+L in the direction of the boundary section En – Di –
Cor and, probably its exit to the line Di–Prp (clinopyroxene-garnet). Further
under the conditions of fractional crystallization melt composition point can
penetrate into the volumes of coesite-eclogite, kyanite-eclogite and
corundum-eclogite “symplexes”. Thus, an overcoming of “eclogite” thermal
barrier between olivine-normative peridotite-pyroxene and SiO2 –
normative eclogite compositions occurs. So, one can speak about the
“destruction” of liquidus peridotite-eclogite thermal barrier in the limits of
the peridotite “simplex” as a result of realization of two reaction mechanisms:
(1) vanishing ofš orthopyroxene as a
result of its peritectic reaction with the melt with clinopyroxene formation
and (2) olivine vanishing as a result of its reactional interaction of jadeite
with garnet formation. If with respect to the first mechanism definite
experimental evidence exists (Litvin, 1991; Davis, 1963) then for the second
mechanism it is absent.
Due to this fact
the main purpose of this paper is an experimental study of phase relationships
in the model system forsterite-dioside-jadeite at pressure of 7 GPa and foundation
of possible physico-chemical correct transitions between peridotite and
eclogite parageneses with overcoming liquidus “eclogite” thermal barrier. To
construct a diagram of a ternary system forsterite-diopside-jadeite it is
necessary to study its boundary binary sections forsterite-jadeite and
fosterite-diopside as well as a number of internal polythermic sections. The
section jadeite-diopside at 7 GPa has been studied earlier (Bobrov, Litvin,
Kojitani, Akaogi, 2006; 2008) and it is characterized by the unlimited
miscibility of jadeite and diopside components in solid and liquid states.
The first
experimental results obtained at the initial stage of the investigation of this
problem can be characterized as follows.
Forsterite-jadeite section.
The experiments in
this section have been done in the temperature range of 1100-
Nevertheless, the
obtained preliminary experimental data contain constructive data that make it
possible to consider the basic problem of this work and start experimental
investigations of liquidus phase relations of the system
forsterite-diopside-jadeite.
The system forsterite-diopside.
The experiments in this
section are given at pressure of 7 GPa in the range of temperatures 1600-
The system forsterite-jadeite-diopside.
The experimental
data and conclusions obtained for the boundary systems make it possible to
start investigating liquidus surface for fusibility diagram of the ternary
system forsterite-jadeite-diopside at P 7 GPa. For the experimental study
polythermic sections of forsterite-(jadeite50diopside50)
and forsterite-(jadeite25diopside75) have been chosen.
The obtained data testify to the fact that olivineš vanishing and garnet formation are realized
in both sections. The problem of further investigations is to search minimum
concentrations of jadeite in the composition of this system where a total
olivine vanishing takes place.
Thus, the performed
experimental investigations of the model system forsterite-diospside-jadeite at
pressure 7 GPa testify to the fact that forsterite (olivine) is a stable phase
in the boundary system forsterite-diopside (olivine-clinopyroxene). While
introducing rather low contents of jadeite component into the composition of
this system the reaction of jadeite component with forsterite takes place in
the melt. As a result, garnet appears as liquidus phase.
With the increase
of the jadeite component concentration in the system the field of liquidus
garnet expands, but a physico-chemical control of crystallization
differentiation of the remnant melts transforms from the monovariant cotectics
Fo + DiSS + L through the invariant peritectic point Fo + DiSS
+ Grt + L to the monovariant cotectics Grt + Cpx + L, which is responsible for
crystallization of bimineral garnet-omphazite eclogite parageneses. The
obtained experimental results testify unambiguously to the fact that in the
system Fo-Di-Jd a physico-chemical mechanism of overcoming liquidus
peridotite-eclogite barrier at mantle magma differentiation is realized. Thus,
a gradual transition from olivine-bearing assemblages to those close by their
characteristics to bimineral eclogites is provided.
Support RFBR: grants 07-05-00499, 08-05-00110, grant
to the leading scientific school 5367.2008.5 (A.A. Marakushev), President grant
MK-194.2008.5.
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