Mineralogy of
metacarbonate xenolith from alkali basalt, E.Eifel, Germany
Sharygin V.V.
V.S.Sobolev Institute of
Geology and Mineralogy SD RAS, Novosibirsk, Russia
sharygin@igm.nsc.ru
Metacarbonate xenoliths in
volcanic rocks are natural analogs of cement clinkers and carbonate
rocks, transformed by combustion metamorphism in natural and technogenic
conditions (Sokol et al., 2005). The Bellerberg volcano, E.Eifel,
Germany, is one of impressive localities of such xenoliths. These
metacarbonate xenoliths very strongly vary in mineral composition and
sometimes contain abundant retrograde phases. This report is devoted to
one of fresh samples (E-2011) with unique mineralogy (Table 1). This
specimen contains two potentially new mineral species: “Fe-shulamitite”,
Fe- analog of shulamitite (Sharygin et al., 2011), and K-Ba-sulfide
intermediate member between djerfisherite K6(Fe,Cu,Ni)25S26Cl
and owensite (Ba,Pb)6(Cu,Fe,Ni)25S27 (Laflamme
et al., 1995). Late secondary phases are not abundant and confined to
vugs and healed fissures in the xenolith (ettringite, hydrated
Ca-silicates, calcite).
Table 1.
Primary minerals found in the metacarbonate xenolith, sample E-2011, E.
Eifel.
Mineral |
Formula |
Mineral |
Formula |
Spurrite |
Ca5(SiO4)2(CO3) |
Shulamitite |
Ca3TiFe(Al,Fe)O8 |
Ternesite |
Ca5(SiO4)2(SO4) |
“Fe-shulamitite” |
Ca3TiFe(Fe,Al)O8 |
Larnite |
Ca2(SiO4) |
Brownmillerite |
Ca2Fe(Al,Fe)O5 |
Bredigite |
Ca7Mg(SiO4)4 |
Srebrodolskite |
Ca2Fe(Fe,Al)O5 |
Gehlenite |
Ca2Al(AlSiO7) |
Magnesioferrite -
Spinel |
MgFe2O4
- MgAl2O4 |
Melilite |
(Ca,Na)2(Mg,Fe,Al)(Al,Si)2O7 |
Magnetite |
FeFe2O4 |
Wollastonite |
Ca3SiO3 |
Baryte |
(Ba,Sr)SO4 |
Ye’elimite |
Ca4Al6O12(SO4) |
Cubanite (isocubanite) |
CuFe2S3 |
Periclase |
MgO |
“Ba-djerfisherite” |
(K,Ba,Pb)6(Fe,Cu)25S27 |
Perovskite |
CaTiO3 |
Chalcocite |
Cu2S |
The xenolith has pronounced
zonality near the contact with alkali basalt, and the contact is well
shown due to brown zone (Fig. 1) mainly represented by minerals of the
melilite group (from alumoakermanite to gehlenite). Reddish-brown tint
of other xenolith’s part is owing to abundant oxide ore phases
(Ca-ferrites, perovskite, spinel group minerals). Other zones are
visually indistinguishable and fixed only by the change of mineral
assemblages. Three additional zones may be divided clearly in the
predominance of the principal minerals: gehlenite-bredigitic,
larnite-ye’elimitic and spurrite-ternesitic (Fig. 1-2). The first zone
contains dominant Al- and Mg-bearing silicates (gehlenite, bredigite)
and minor Cu-Fe-sulfides (cubanite, K-Fe-sulfide), barite and Mg-Fe-spinels.
The second zone is abundant in ordinary Ca-silicate (larnite),
Ca-sulfate-aluminate (ye’elimite), periclase and rare chalcocite. The
third zone is represented by Ca-silicates with additional [SO4]
è
[CO3] groups (ternesite, spurrite),
whereas the amount of ye’elimite, periclase and larnite is decreased and
sulfides are absent.
Fig. 1.
Zonation in metacarbonate
xenolith, sample E-2011, E. Eifel.
Mineral are listed in their
abundance in zones.
The total amount of oxide
ore phases in these zones is approximately equal, but their ratio is
changed in the associations as far as the contact with basalt (Fig. 2):
perovskite + magnesioferrite, perovskite + “Fe-shulamitite”,
brownmillerite + srebrodolskite, perovskite + shulamitite +
“Fe-shulamitite” + brownmillerite ± srebrodolskite ± magnesioferrite,
shulamitite + brownmillerite ± perovskite. In the case of the
coexistence of one series minerals (shulamitite - “Fe-shulamitite”,
brownmillerite - srebrodolskite), the Al-richer phase is crystallized in
first order. In spurrite-ternesitic zone, where the abundance of
ye’elimite is minimal, Al-rich Ca-ferrites (shulamitite, brownmillerite)
is more stable, and perovskite occurs rarely as relic in shulamitite.
Fig. 2.
Mineral composition in the
individual zones of the xenolith (scanning microscopy).
Symbols: Trn - ternesite, Spu
- spurrite, Lar - larnite, Per - periclase, Yel - ye’elimite, Brm -
brownmillerite, Shu - shulamitite, Fe-Shu - “Fe-shulamitite”, Prv -
perovskite, Ghl - gehlenite, Brd - bredigite, Ca-Sil - hydrated
Ca-silicates, Djr - “Ba-djerfisherite”, Cub - cubanite.
Some chemical features for
minerals may be indicated towards to the contact with basalt. The SrO
concentration is increased in all Ca-containing minerals (up to 2-4
wt.%). Periclase is getting richer in FeO up to the appearance of the
solid phase decay structures (wüstite or magnesioferrite). The content
of Fe2O3 is increased in Ca-ferrites. Ba- and
Cu-containing phases are common only of the zones nearby the contact.
Thus, pronounced metasomatic zonation in mineral chemistry and mineral
assemblages is revealed in the studied Eifel xenolith. It should be
noted that similar localization of minerals enriched in Ba, Sr and other
trace elements to the contact zones with silicate melt was previously
described for metacarbonate rocks from Chegem and Donetsk (Sharygin,
2011; Galuskin et al., 2008; 2011).
In petrologic aspect the
study of metacarbonate xenoliths in volcanic rocks always emerges a
question: could silicate melt totally assimilate them or reactionary
relations and solid phase transformation are available only? In the case
of Eifel the protolith was represented by limestone, which fragments
were trapped by alkaline magma on shallow depths during ascending. The
melting of such high-Ca protolith is possible only at temperature higher
than 1350-1400oC. Assuming olivine-free association of the
host basalt (close to nephelinite) the liquidus temperature of alkaline
melt was approximately 1300îÑ.
Moreover, temperature gradient should be taken into account during
transformation of carbonate xenolith. The absence of reliable indicator
minerals in the xenolith allows only the rough estimations in the broad
temperature range (900-1200îÑ),
what corresponds to HT region of the spurrite-merwinite facies (Sokol et
al., 2005). The association perovskite + shulamitite or “Fe-shulamitite
(Sharygin et al., 2008) can not be used for temperature estimations of
individual mineral assemblages in the studied xenolith because it is not
in equilibrium. The relationships of phases indicate that shulamitite
and “Fe-shulamitite” are later phases than perovskite, and they grow on
perovskite and even replace it (Fig. 2). The superior temperature limit
is based on that in high-Ca systems with SiO2 Ca-ferrites and
alumoferrites of different composition (Ca2(Fe,Al)2O5,
CaFe2O4, etc.) are stable only up to 1200-1210îÑ.
The increasing of temperature provokes them to react with Ca-silicates
with formation of Ca-silicoferrites of the aenigmatite-dorrite group
(Scarlett et al., 2004). These specific minerals are not found in the
xenolith.
The author would like to
thank B.Ternes and W.Schüller (Germany) for donating of metacarbonate
xenoliths from E. Eifel for detailed studies.
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