Figure 1. Simpliied geological maps of [a] European Cenozoic Rift System showing orientations of P-wave anisotropies (blue arrows) and SKS splitting (red arrows) anisotropies [modiied from Echtler et al., (1994) and Smith and Ekström (1999)]; [b] Ohře Rift and Eger graben, showing the locality of Kozákov volcano and representative seismic velocity-depth prooles for the Lugian and Bohemian terranes [modiied from Kasinski (1991), and Cermák (1989)]. Figure 3. Mantle seismic anisotropy beneath Kozákov is characterized by steeply dipping SKS fabrics and shallow subhorizontal P-wave anisotropy (Christensen et al., 2001). Figure 2. Mantle xenolith in 4 Ma basanite. Figure 4. Estimated temperatures and depths for Kozákov spinel peridotite xenoliths. Open symbols and layer patterns on the left indicate T-z values obtained by combining the averages of three, two-pyroxene geothermometers with a model 5 Ma geotherm. Filled symbols represent the maximum depths for spinel stability in each sample, and the solid line indicates an inferred geotherm at 5 Ma that is consistent with the stability of spinel in all samples of the xenolith suite. Associated layer types are labeled on the right. Figure 6. Photomicrographs of thin sections from the xenoliths highlighting the two predominant grain textures observed: [a] upper equigranular; [b] protogranular; and [c] lower equigranular. Inset boxes are in plane polarized light to accentuate the diierent spinel textures (disseminated vs. symplectic).