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3.5.2.2 Garnets
The most important iron and silicon containing garnet minerals are the pyrope-
almandine series (Mg,Fe 2+ ) 3 Al 2 (SiO 4 ) 3 and andradite Ca 3 (Al,Fe 3+ ) 2 (SiO 4 ) 3 . When
Mg is replaced by Mn the garnet is called spessartine (Mn,Fe 2+ ) 3 Al 2 (SiO 4 ) 3 . The
garnet structures contain SiO 4 tetrahedra with commonly trivalent cations in
6-coordination and divalent cations in 8-coordination.
Members of the pyrope-almandine series exhibit a doublet at RT with an isomer
shift d Fe = 1.2-1.4 mm/s and a very large quadrupole splitting D in the range
3.47-3.70 mm/s [ 180 ]. An additional doublet of Fe 3+ due to the six-fold coordi-
nated Al site is observed with d Fe = 0.35-0.45 mm/s and D = 0.29-0.75 mm/s
when going from almandine towards andradite. These intermediate minerals are
often called grossular. Pure almandine orders magnetically around 10 and at 4 K
an Fe 2+ octet is observed with a hyperfine field of 23-24. 5 T [ 181 ]. The typical
large quadrupole splitting in garnets is shown in the spectrum of spessartine in
Fig. 3.23 .
Andradite possesses at RT the typical Fe 3+ hyperfine parameters, namely
d Fe = 0.39-0.41 mm/s and D = 0.5-0.6 mm/s [ 180 ]. The latter is, however,
strongly dependent on the composition. It orders magnetically below 11 and at 4 K
the hyperfine field amounts to 51.9 T [ 182 ]. Actually, the spectrum is asymmetric
and can be analyzed with two sextets having different quadrupole shifts 2e = 0.32
and -0.16 mm/s, due to a complex spin structure with different orientations with
respect to the EFG principal axis. In some garnets such as titanium andradite,
Ca 3 (Fe,Ti,Si) 5 O 12 ,Fe 3+ also occupies partly the tetrahedral Si sites, exhibiting
very low isomer shifts and rather high quadrupole splittings [ 183 ].
Fig. 3.23 RT spectrum of
spessartine showing the
predominant Fe 2+ doublet
with the typical large
quadrupole splitting for
garnets. The spectrum shows
an additional small doublet
from octahedral Fe 3+ (after
Eeckhout et al. [ 308 ])
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