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3. Quantitative analyses of metamorphic microstructures 34Figure 3.3: Rf/phi plot quantifying the orientation and shape of intragranular meltfilledvoids in K-fedspar aggregate and 3d image of melt distribution in monomineralicaggregate.Figure 3.4: Grain contact frequency vs. brain boundary preferred orientation showingthe evolution of microstructure from highly aggregate to random and regular distributionswith increasing deformation.(Fig. 3.4). At the same time, the rock reveals first increase of aggregate distributionrelated with development of banded mylonite structure followed by complete mixing ofall phases related to influx of melt and the rheological collapse of the rock. We correlatedthese stages of orthogneiss deformation with increasing amount of melt pressure whichreduced effective stress at constant (and low) differential stress level conditions. In fact,the amount of very small melt proportion controls not only the topology of melt seamsbut also dramatically weaken rock at melt fraction for about 5%Hasalová et al. (2008a) used the PolyLX method to evaluate the role of melt infiltrationinto orthogneiss microstructure. This work shows surprising CSD evolution from
3. Quantitative analyses of metamorphic microstructures 35Figure 3.5: N 0 -Gt plots showing evolution of CSD from growth dominated to nucleationdominated microstructural stages within crustal channel. This evolution isinterpreted as result of syntectonic melt infiltration.originally high Gt/N 0 values towards low values in conjunction with increasing amountof mineral resorption and mineral overgrowth features. This particular evolution canbe only explained by increasing importance of nucleation rate which is incompatiblewith process of in-situ melting but reflect crystallization of melt in rock pores. TheseCSD plots were therefore used as a major argument for reactive porous flow in felsicrocks, a concept which was for the first time demonstrated in the continental crust. TheCSD results are supported by evolution in grain contact frequency plot which revealssystematically increasing importance of regular grain distributions which is driven tounexpected values. The regular grain distribution simply indicates progressive growthof new phases in the rock aggregate as the melt crystallizes in the rock. Finally, theprogressive melt infiltration is related with loss of grain shape preferred orientation coupledwith loss of aspect ratios, which in turn is connected with increasing developmentof preferred orientation of certain unlike boundaries. All that indicates that the porousflow was a dynamic process related to dynamic dilation of intragranular pores whichmaintained the porosity of rock at high level as long as the reactive porous flow wasactive.Our last studies are focused on quantification of microstructural evolution of granulitetextures (Franěk et al., 2011b). We discovered precursor rock of felsic granuliteswhich is interpreted as coarse grained orthogneiss, that was converted to granulite duringCarboniferous thickening and collision. These studies show that the hypersolvusalkaline feldspar is first decomposed into thick perthites that are rapidly replaced bypolycrystalline, equidimensional aggregate of pure K feldspar and plagioclase (Fig. 3.6).This decomposition is driven by heterogeneous nucleation process resulting from stored
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Table 1Statistical values of the qu
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Table 2Summary of parameters derive
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J. metamorphic Geol., 2008, 26, 273
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EXHUMATION IN LARGE HOT OROGEN 275m
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Probabi l irequencyProbabi l ireque
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EXHUMATION IN LARGE HOT OROGEN 279y
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EXHUMATION IN LARGE HOT OROGEN 281N
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EXHUMATION IN LARGE HOT OROGEN 283w
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EXHUMATION IN LARGE HOT OROGEN 285a
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EXHUMATION IN LARGE HOT OROGEN 287w
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EXHUMATION IN LARGE HOT OROGEN 289T
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EXHUMATION IN LARGE HOT OROGEN 291O
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EXHUMATION IN LARGE HOT OROGEN 293r
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EXHUMATION IN LARGE HOT OROGEN 295B
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EXHUMATION IN LARGE HOT OROGEN 297R
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Author's personal copyK. Schulmann
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J. metamorphic Geol., 2011, 29, 79-
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HEAT SOURCES AND EXHUMATION MECHANI
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CONTRASTING TEXTURAL RECORD OF TWO
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Contrasting microstructures and def
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TEXTURES OF NATURALLY DEFORMED META
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1.0--0.9__Mg~(Mg2++Fe2+)9 Core of p
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' ~'-----2~--~----TEXTURES OF NATUR
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ClickHereforFullArticleJOURNAL OF G
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B10406SCHULMANN ET AL.: RHEOLOGY OF
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ORIGIN OF FELSIC MIGMATITES 31Ó 20
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ORIGIN OF FELSIC MIGMATITES 33durin
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ORIGIN OF FELSIC MIGMATITES 35(a)Ty
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ORIGIN OF FELSIC MIGMATITES 37(a)Pl
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ORIGIN OF FELSIC MIGMATITES 39Grain
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ORIGIN OF FELSIC MIGMATITES 41(a)(b
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ORIGIN OF FELSIC MIGMATITES 43(a)(b
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ORIGIN OF FELSIC MIGMATITES 45Fig.
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ORIGIN OF FELSIC MIGMATITES 47produ
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ORIGIN OF FELSIC MIGMATITES 49stron
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ORIGIN OF FELSIC MIGMATITES 51Cmı
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ORIGIN OF FELSIC MIGMATITES 53easte
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104 J. FRANĚK ET AL.in terms of th
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