This textbook describes the physics of the plastic deformation of solids at high temperatures. It is directed at geologists or geophysicists interested in the high-temperature behaviour of crystals who wish to become acquainted with the methods of materials science in so far as they are useful to earth scientists. It explains the most important models and recent experimental results without losing the reader in the primary literature of materials science. In turn the book deals with the essential solid-state physics; thermodynamics and hydrostatics of creep; creep models and their applications in the geological sciences; diffusion creep; superplastic deformation and deformation enhanced by phase transformations. Five concluding chapters give experimental results for metals, ceramics and minerals. There are extensive bibliographies to aid further study.

Introduction to the Physics of the Earth's Interior describes the structure, composition and temperature of the deep Earth in one comprehensive volume. The book begins with a succinct review of the fundamentals of continuum mechanics and thermodynamics of solids, and presents the theory of lattice vibration in solids. The author then introduces the various equations of state, moving on to a discussion of melting laws and transport properties. The book closes with a discussion of current seismological, thermal and compositional models of the Earth. No special knowledge of geophysics or mineral physics is required, but a background in elementary physics is helpful. The new edition of this successful textbook has been enlarged and fully updated, taking into account the considerable experimental and theoretical progress recently made in understanding the physics of deep-Earth materials and the inner structure of the Earth. Like the first edition, this will be a useful textbook for graduate and advanced undergraduate students in geophysics and mineralogy. It will also be of great value to researchers in Earth sciences, physics and materials sciences.

Single crystals of pure and impure halite have been dynamically recrystallized during compression creep at temperatures between 250 ø and 790øC and stresses between 1.5 and 120 bars. Recrystallization was found to occur by two different mechanisms: at lower temperatures and stresses the new grains result from the rotation of subgrains without grain boundary migration (rotation recrystallization), and at higher temperatures and stresses the final texture results from the migration of the high-angle grain boundaries of the rotated subgrains. Migration recrystallization was shown to occur for critical stress and temperature conditions, allowing rapid grain boundary migration. A curve separates the two domains in the a, T plane and moves to higher temperatures and stresses for crystals of higher impurity content; for natural crystals, only rotation recrystallization can occur. In each recrystallization regime the recrystallized grain size is uniquely related to the applied stress, thus yielding two different geopiezometers, which should not be applied indiscriminately to natural tectonites to determine lithospheric or mantle deviatoric stresses. The experimental results are interpreted by the Li•cke et Stfiwe theory for impurity-controlled grain boundary migration. Dynamic recrystallization can be defined as a solid state grains, without grain boundary migration [Nicolas and Poirier, process leading to the creation of a new (and usually different) 1976]. This mechanism, distinct from the nucleation and grain structure in the course of plastic deformation of crystal-growth mechanism (the only known in metals), has been recline solids. The differences between the old and recrystallized ognized in quartz and olivine tectonites [White, 1973; Poirier structures can reside in one or several of the following features: and Nicolas, 1975]. The purpose of the present study was to preferred orientation of the grains (petrofabric), mis-gather moreinformation on the relationship between deformaorientation between adjacent grains, and grain size and shape. tion and dynamic recrystallization and more specifically on the Dynamic recrystallization, as opposed to static (or annealing) conditions of occurrence of recrystallization involving grain recrystallization, occurs simultaneously with deformation in boundary migration ('migration' recrystallization)or rotation of subgrains without migration ('rotation' recrystallization). certain conditions of stress, strain, temperature, purity, etc., and the same microscopic elementary processes that cause or We chose the mineral halite (NaCl) for the following reasons: control deformation are also responsible for dynamic recrys-(1) It is easily available in single crystals of known purity; (2) tallization [Nicolas and Poirier, 1976]. Therefore if the micro-its recrystallization can be studied in uniaxial creep tests withstructure of a paleodeformed rock can be ascribed to dynamic out confining pressure at temperatures lower than 800øC; (3) recrystallization, it may be of great value as a mark...

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