Quantitative structural analyses and numerical modelling of ...

B10406SCHULMANN ET AL.: RHEOLOGY OF PARTIALLY MOLTEN GNEISSESB10406[18] Another important feature is the development of intragranular,wedge shaped fractures that are predominantlydeveloped in elongated feldspar grains with stronger SPOin samples T1 and T2 (Figure 8). These gently curvedfractures often originate at the foliation-parallel grain boundariesor triple point junctions, terminate in the interior of thegrains and are oriented at low angles (15–30°) to themaximum stretching. In Type III orthogneiss samples (e.g.,sample B2) the intragranular fractures occur as well beingoriented at high angle to the principal stretching direction.Figure 4. Type I microstructure (S1 sample). (a) Type Imetagranite marked by large alkaline feldspar clasts decomposedinto albite chains and K-feldspar and (b) scanningelectron microscope (SEM) image of alkaline feldspardecomposition. Rectangle indicates the position of the detailedSEM image. (c) The detail of the SEM image showing theshapes of new bulbous albite grains. (d) CorrespondingArcView Geographical Information Systems (GIS) image usedfor the quantitative mirostructural analysis. Scanning electronmicroscope images obtained in backscattered electron mode(Camscan microscope, Institute of Petrology and StructuralGeology Prague). K-feldspar is represented in light gray,biotite is represented as white laths, quartz and plagioclase areshown in dark gray, and rectangular white mica laths areshown in light gray. In ArcView GIS images the K-feldspar isrepresented in white, white mica and biotite are represented inblack, plagioclase is represented in light gray, and quartz isrepresented in dark gray. The ArcView GeographicalInformation System was used as an ideal environment fordigitizing mineral shapes [Lexa et al., 2005]. Mineralabbreviations correspond to those of Kretz [1983].which corroborates the development of thin albite-quartzfilms along the feldspar faces oriented along two maximawith respect to the macroscopic layering (Figure 8). Themean orientation of the Pl2 and quartz seams form an angleof 10–15° with respect to the foliation trace. Interstitialconvex quartz grains often occur at triple point junctionsbut locally line the feldspar boundaries as narrow films(Figures 6c and 6d).[17] The presence of interstitial phases is the most pronouncedin Type III orthogneiss (samples R3, V1 and B2 inparticular) where the recrystallized feldspar grains exhibitno shape preferred orientation. Here, wider cuspate-lobatepools and narrow films of Pl2 and quartz occur at a highangle to the macroscopic foliation. The B2 sample shows anextreme orientation of Pl2 seams which form an angle of upto 70° with the foliation trace.5. Quantitative Textural Analysis[19] The quantitative analysis of grain shapes and boundarieswas carried out in an ArcView GIS environment.Examples of analyzed samples are shown in Figures 4d,6d, and 7d. The statistical parameters involving grains sizedistributions, shape preferred orientation, degree of grainelongation and grain contact frequencies were performedusing the MATLAB PolyLX toolbox [Lexa et al., 2005] inorder to quantify the above described microstructural sequenceof rock types. The grain size distribution wasevaluated as an important parameter in deformed rocksbecause of its sensitivity to stress and temperature [Schmidet al., 1999]. The correct determination of grain size isessential in polyphase systems, where stress and strain ratepartitioning are expected [Handy, 1990]. Another importantparameter is the shape of recrystallized grains, which isstrongly dependent on the type of deformation mechanismsand grain growth history [Boullier and Guéguen, 1975;Schmid et al., 1987]. Grain contact distribution in the rockyields information about the evolution of spatial distributionof the different minerals in rocks with deformation ormelting [Lexa et al., 2005; Hasalová etal., 2008]. This isexpressed by the grain contact frequency (GCF) that statisticallyquantifies the deviation of the grain contact distributionfrom random [Kretz, 1969]. The aggregate distribution,marked by the dominant presence of like-like contacts,represents one end-member of the spatial distribution ofgrain boundaries that is resulting from the solid statedifferentiation process [McLellan, 1983]. The regular distributionis characterized by the predominance of unlikecontacts in rock and is considered as a second end-memberFigure 5. Ternary diagrams showing the composition offeldspars in different samples. Pl1 corresponds to isolatedplagioclase aggregate (see text for explanation).6of20300