ALBERT

Notes: Annealing is an important mechanism of microstructural modification both in rocks andmetals. In order to relate directly changes in crystallographic orientation to migrating boundaries theresearcher has the option to investigate either samples where the grain boundary motion can bedirectly tracked or a series of samples exhibiting successively higher degrees of annealing.Here we present results from rock samples collected from two well characterised contactaureoles (a volume of rock heated by the intrusion of a melt in its vicinity): One quartz sample inwhich patterns revealed by Cathodoluminescence (CL) indicate the movement of grain boundariesand a series of calcite samples of known temperature history. Electron backscatter diffraction(EBSD) analysis is used to link the movement of grain, twin boundaries and substructures with thecrystallographic orientation / misorientation of a respective boundary.Results from the quartz bearing rock show: (a) propagation of substructures and twinboundaries in swept areas both parallel and at an angle to the growth direction, (b) development ofslightly different crystallographic orientations and new twin boundaries at both the growthinterfaces and within the swept area, and (c) a gradual change in crystallographic orientation in thedirection of growth. Observations are compatible with a growth mechanism where single atoms areattached and detached both at random and at preferential sites i.e. crystallographically controlledsites or kinks in boundary ledges. Strain fields caused by defects and/or trace element incorporationmay facilitate nucleation sites for new crystallographic orientations at distinct growth interfaces butalso at continuously migrating boundaries.Calcite samples show with increasing duration and temperature of annealing: (a) systematicdecrease of the relative frequency of low angle grain boundaries (gbs), (b) decrease in latticedistortion within grains, (c) development of distinct subgrains with little internal lattice distortion,(d) change in lobateness of gbs and frequency of facet parallel gbs and (e) change in position ofsecond phase particles. These observations point to an increasing influence of grain boundaryanisotropy with increasing annealing temperature, while at the same time the influence of secondphase particles and subtle driving-force variations decrease.This study illustrates the usefulness of using samples from natural laboratories and combiningdifferent analysis techniques in microprocess analysis

Notes: First results from grain growth experiments in a columnar structured Al foil show several interesting features: (a) the grain size distribution remains heterogeneous even after up to 300 min. annealing and (b) the Von Neumann-Mullins relation is not always satisfied. To clarify the underlying reasons for these features, in-situ heating experiments within a Scanning Electron Microscope (SEM) were combined with detailed Electron Backscatter Diffraction (EBSD) analysis. These show that the movement of boundaries can be strongly heterogeneous. For example, the complete replacement of one grain by a neighbouring grain without significant change of the surrounding grain boundary topology is frequently seen. Experiments show that grain boundary energy and/or mobility are anisotropic both with respect to misorientation and orientation of grainboundary plane. Low energy and/or mobility boundaries are commonly low angle boundaries, twin boundaries and boundaries that form traces to a low index plane of at least one of the adjacent grains. As a consequence the Von Neumann-Mullins relation is not always satisfied

Notes: Misorientation analysis, using EBSD data sets, has enabled us to constrain betterrecrystallization mechanisms in rocks and minerals. Observed microstructures are not explicable in terms of recovery, boundary bulging and migration alone. We have to invoke either a nucleation process (physics unknown) or grain rotations that are not related to grain or boundary crystallography. Such rotations can occur by diffusion accommodated grain boundary sliding and this mechanism explains best the microstructure and texture of recrystallized grains in some rocks

Notes: The localization of deformation in recrystallizing materials is investigated via a series of two-dimensional grain-scale numerical simulations. These simulations couple a grain size and strain dependant viscous rheology with grain size reduction and grain growth processes. The simulations are able to predict the mechanical, microstructural and strain evolution of the polycrystals to high strain, and allow us to examine the nature of the time dependent feedback between mechanical andmicrostructural behavior. It was found that significant strain localization occurred only when the grain size dependence of the viscosity was non-linear, and was greatly enhanced by the activity of the grain size modifying processes. The intensity and location of the zone of strain localization varied spatially and temporally, with the result that the finite strain state showed a much broader, and hence less intense, zone of localized deformation than the instantaneous state

Notes: Experiments in which the microstructural development can be observed at the same time as the crystallography is described fully opens up new, powerful ways to advance our understanding of microstructural processes such as grain growth, primary and secondary recrystallization and phase transformations. In addition, comparison of results of experiments in different materials can be used to develop general laws for the investigated processes. In this study, we briefly review and compare the results from various ongoing studies undertaken in a variety ofmaterials with emphasis on highlighting (a) the scientific potential of such experiments and (b)similarities and differences in their microstructural evolution. Materials studied include metals e.g. Ti, Ni, Al, Mg, Ti-SULC steel and geological materials such as rocksalt (NaCl), hematite and magnetite. Here, we present experimental results and their interpretation in terms of subgrain to grain-scale processes

Notes: Reflected light optical analysis and Electron Backscatter Diffraction (EBSD) analysis have been used to m easure grain sizes in 2D Al foil samples, annealed for different times. There are significant differences in the results of the two techniques. It is shown that in Al it is possible to detect boundaries in optical images down to a misorientation angle of 7-8º. Nevertheless, in most samples the critical angle of easy etching lies above 10º. The observed differences in grain size measurements between optical analysis and EBSD analysis can be largely attributed to threephenomena: (1) individual samples may behave slighty differently due to differences in the effectiveness of etching (2) the grain size is heterogeneous over large areas and (3) the effect of etching is not only a function of misorientation angle but also grain boundary plane. Despite these uncertainties, optical analysis seems to be reliable for analysis of processes in which mainly grainboundaries with misorientation angle of 〉 10º are involved i.e. grain growth

Notes: Abstract Meta-sedimentary rocks including marbles and calcsilicates in Central Dronning Maud Land (CDML) in East Antarctica experienced a Pan-African granulite facies metamorphism with peak metamorphic conditions around 830 ± 20 °C at 6.8 ± 0.5 kbar which was accompanied by the post-kinematic intrusion of huge amounts of syenitic (charnockitic) magmas at 4.5 ± 0.7 kbar. The marbles and calcsilicates may represent meta-evaporites as indicated by the occurrence of metamorphic gypsum/anhydrite and Cl-rich scapolite that formed in the presence of saline fluids with X NaCl in the range 0.15–0.27. The marbles and calcsilicates bear biotite, tremolite and/or hornblende and humite group minerals (clinohumite, chondrodite and humite) which are inferred to have crystallized at about 650 °C and 4.5 kbar. The syenitic intrusives contain late-magmatic biotite and amphibole (formed between 750 and 800 °C) as well as relictic magmatic fayalite, orthopyroxene and clinopyroxene. Two syenite and two calcsilicate samples contain fluorite. Corona textures in the marbles and calcsilicates suggest very low fluid-rock ratios during the formation of the retrograde (650 °C) assemblages. Biotite in all but two syenite samples crystallized at log(f H 2 O/f HF) ratios of 2.9 ± 0.4, while in the calcsilicates, both biotite and humite group minerals indicate generally higher log(f H 2 O/f HF) values of up to 5.2. A few samples, though, overlap with the syenite values. Log(f H 2 O/f HCl) derived from biotite covers the range 0.5–2.6 in all rock types. Within a single sample, the calculated values for both parameters vary typically by 0.1 to 0.8 log units. Water and halogen acid fugacities calculated from biotite-olivine/orthopyroxene-feldspar-quartz equilibria and the above fugacity ratios are 1510–2790 bars for H2O, 1.3–5.3 bars for HF and 7–600 bars for HCl. The results are interpreted to reflect the reaction of relatively homogeneous magmatic fluids [in terms of log(f H 2 O /f HF)] derived from the late-magmatic stages of the syenites with both earlier crystallized, still hotter parts of the syenites and with adjacent country rocks during down-temperature fluid flow. Fluorine is successively removed from the fluid and incorporated into F-bearing minerals (close to the syenite into metamorphic fluorite). In the course of this process log(f H 2 O /f HF) increases significantly. Chlorine preferably partitions into the fluid and hence log(f H 2 O /f HCl) does not change markedly during fluid-rock interaction.