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Figure 19.5 Eu**/(Eu** + Eu**) redox ratio as determined by XANES vs. oxygen fugacity values, for different bulk compositions. Solid lines represent the evolution of Eu redox ratio with fOz, extrapolated from data reported by Karner et al. (2010) and Cicconi et al. (2012). Other compositions are haplogranitic glasses (stars; Cicconi et al. 2012) or CAS, MAS compositions (diamonds; Burnham et al., 2015). Crosses (and dotted lines) represent modified diopside-anorthite compositions from Burnham et al. (2015) (AD and AD+qz). Blue dashed line follows the trend of Eu redox in a synthetic MORB glass. See text for details.

Figure 19 5 Eu**/(Eu** + Eu**) redox ratio as determined by XANES vs. oxygen fugacity values, for different bulk compositions. Solid lines represent the evolution of Eu redox ratio with fOz, extrapolated from data reported by Karner et al. (2010) and Cicconi et al. (2012). Other compositions are haplogranitic glasses (stars; Cicconi et al. 2012) or CAS, MAS compositions (diamonds; Burnham et al., 2015). Crosses (and dotted lines) represent modified diopside-anorthite compositions from Burnham et al. (2015) (AD and AD+qz). Blue dashed line follows the trend of Eu redox in a synthetic MORB glass. See text for details.

Related Figures (8)

Figure 19.1 (a) Plot of ionic radius (data from Shannon, 1976) vs. ionic charge for trace elements of geological interest. Red diamonds refer to four-fold coordinated cations (modified after Rollinson, 1993). (b) Dietzel’s field strength parameter for several cations (stars refer to four-fold coordinated cations). Incompatible and compatible elements can be divided on the basis of their charge (Z) and size (Figure 19.1la), or in terms of ionic potential (the ratio between charge and ionic ratio). Another parameter was proposed by Dietzel (1948): the Cation Field Strength CFS = Z/ (t.+ro)*, where Z is the charge of the cations and the denominator represents the cation- oxygen distance (here considered oxygen ionic radius =1.35 A) (Figure 19.1b). The partition coefficient (D) is the ratio of the concen- tration of a trace element in a solid phase with respect to
Figure 19.1 (a) Plot of ionic radius (data from Shannon, 1976) vs. ionic charge for trace elements of geological interest. Red diamonds refer to four-fold coordinated cations (modified after Rollinson, 1993). (b) Dietzel’s field strength parameter for several cations (stars refer to four-fold coordinated cations). Incompatible and compatible elements can be divided on the basis of their charge (Z) and size (Figure 19.1la), or in terms of ionic potential (the ratio between charge and ionic ratio). Another parameter was proposed by Dietzel (1948): the Cation Field Strength CFS = Z/ (t.+ro)*, where Z is the charge of the cations and the denominator represents the cation- oxygen distance (here considered oxygen ionic radius =1.35 A) (Figure 19.1b). The partition coefficient (D) is the ratio of the concen- tration of a trace element in a solid phase with respect to
Figure 19.2 lonic radii for six-fold coordinated REE**. (Radius values from Shannon, 1976).
Figure 19.2 lonic radii for six-fold coordinated REE**. (Radius values from Shannon, 1976).
Figure 19.3 (a) Mineral/melt REE partition coefficients for plagioclase (Plg), olivine (Ol), clinopyroxene (Cpx), and garnet in basaltic melts. (b) REE plagioclase/melt partition coefficients in basalt, andesite, and rhyolite. Data compilation from Rollinson (1989) and references therein.
Figure 19.3 (a) Mineral/melt REE partition coefficients for plagioclase (Plg), olivine (Ol), clinopyroxene (Cpx), and garnet in basaltic melts. (b) REE plagioclase/melt partition coefficients in basalt, andesite, and rhyolite. Data compilation from Rollinson (1989) and references therein.
Figure 19.4 Experimental data from Drake (1975) show that the partitioning of Eu between plagioclase feldspar and magmatic liquid (ppigimely is a strong function of oxygen fugacity conditions. Redrawn after Drake and Weill (1975).
Figure 19.4 Experimental data from Drake (1975) show that the partitioning of Eu between plagioclase feldspar and magmatic liquid (ppigimely is a strong function of oxygen fugacity conditions. Redrawn after Drake and Weill (1975).
Figure 19.7 Parallel (VV) and cross-polarized (VH) Raman spectra (normalized to the total area) for a NS2 glass (blue line), and for Ce doped glasses. Black lines refer to a NS2 glass having 100%Ce** ions, and red lines to the glass with 15% Ce?* ions (error on redox quantification: +7; data from Cicconi et al., 2021).
Figure 19.7 Parallel (VV) and cross-polarized (VH) Raman spectra (normalized to the total area) for a NS2 glass (blue line), and for Ce doped glasses. Black lines refer to a NS2 glass having 100%Ce** ions, and red lines to the glass with 15% Ce?* ions (error on redox quantification: +7; data from Cicconi et al., 2021).
Figure 19.8 X-Ray Absorption Spectroscopy data at the Eu Li edge (left) and at the Fe K-edge (right) for glasses of Di-An composition synthetized under different conditions of fO2 (data from Cicconi et al., 2017).
Figure 19.8 X-Ray Absorption Spectroscopy data at the Eu Li edge (left) and at the Fe K-edge (right) for glasses of Di-An composition synthetized under different conditions of fO2 (data from Cicconi et al., 2017).
Figure 19.9 (a) XAS spectra, normalized at the Fe K-edge, collected for the starting basaltic glass and for the melt (1500°C), after 37, 47 and 66s under reducing conditions (Ar/H gas). (b) Time dependence of Eu and Fe redox kinetics in the basaltic melt, under reducing conditions (data from Cicconi et al., 2015).
Figure 19.9 (a) XAS spectra, normalized at the Fe K-edge, collected for the starting basaltic glass and for the melt (1500°C), after 37, 47 and 66s under reducing conditions (Ar/H gas). (b) Time dependence of Eu and Fe redox kinetics in the basaltic melt, under reducing conditions (data from Cicconi et al., 2015).
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