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High-grade gneiss terrains typically exhibit a low pressure, high temperature (>500 C) regional metamorphism of the amphibolite or granulite facies (Section 99) These belts form the majority of the area of Archean cratons A variety of types commonly are displayed, including quartzofeldspathic gneiss of mostly granodiorite and tonalite composition, layered peridotite-gabbro-anorthosite or leucogabbro-anorthosite complexes, and metavolcanic amphibolites and metasediment (Windley, 1981) Peridotite (Sections 247, 25) is an ultrama c rock rich in olivine and pyroxene minerals Leucogabbro refers to the unusually light color of the gabbroic rock due to the presence of plagioclase Anorthosites are plutonic rocks consisting of >90% plagioclase and have no known volcanic equivalents These latter rocks occur exclusively in Archean and Proterozoic crust Most authors view Archean anorthosites as having differentiated from a primitive magma, such as a basalt rich in Fe, Al and Ca elements or, possibly, a komatiite (Winter, 2001).



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In general therefore option (3) seems to be the design most likely to fulfil general requirements for longitudinal information, but has difficulties of both methodology and interpretation. In using option (1) or (2) in its place, there is a clear need to explain the limitations of what can be inferred to users of the information noting however that there is a risk that such limitations may be ignored by users, particularly if no other information is available. 2.3.2 Target Variables





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High-grade gneiss terrains are highly deformed and may form either contemporaneously with, structurally below, or adjacent to the low-grade greenstone belts (Percival et al, 1997) The granitoids that intrude the greenstones and high-grade gneisses form a compositionally distinctive group known as tonalite-trondhjemite-granodiorite, or TTG, suites (Barker & Arth, 1976) Tonalites (Section 98) and trondhjemites are varieties of quartz diorite that typically are de cient in potassium feldspar These igneous suites form the most voluminous rock associations in Archean crust and represent an important step in the formation of felsic continental crust from the primordial mantle (Section 1133)..

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Because the rigidity of a uid is zero, S waves cannot be transmitted by such a medium A consequence of the velocity equations for P and S waves is that the P velocity is about 17 times greater than the S velocity in the same medium Consequently, for an identical travel path, P waves arrive before S waves This was recognized early in the history of seismology, and is re ected in the names of the body waves (P is derived from primus and S from secundus) The passage of body waves through the Earth conforms to the laws of geometric optics in that they can be both refracted and re ected at velocity discontinuities Seismic waves whose travel paths are restricted to the vicinity of a free surface, such as the Earth s surface, are known as surface waves.

Rayleigh waves cause the particles of the transmitting medium to describe an ellipse in a vertical plane containing the direction of propagation They can be transmitted in the surface of a uniform half space or a medium in which velocity changes with depth Love waves are transmitted whenever the S wave velocity of the surface layer is lower than that of the underlying layer Love waves are essentially horizontally polarized shear waves, and propagate by multiple re ection within this low velocity layer, which acts as a wave guide Surface waves travel at lower velocities than body waves in the same medium Unlike body waves, surface waves are dispersive, that is, their different wavelength components travel at different velocities Dispersion arises because of the velocity strati cation of the Earth s interior, longer wavelengths penetrating to greater depths and hence sampling higher velocities.

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