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CONTENTS Preface Thomas J Ahrens vii Classification of Rocks and Their Myron G Best Sediments and Soils: Chemistry Scott M McLennan Acoustic Kenneth Abundances on the Earth and Abundances Velocity and Attenuation W Winkler and William Experimental Trace Element John H Jones 73 (3-2) in Porous Rocks (3-3) F Murphy HI 20 Shock Wave Data for Rocks (3-4) Thomas J Ahrens and Mary L Johnson Pressure-Volume-Temperature Teresa S Bowers 45 (3-l) Properties Partitioning 35 of H,O-CO, Fluids (3-6) (3-7) Thermal Conductivity of Rocks and Minerals (3-9) Christoph Clauser and Ernst Huenges 105 Rock Failure (3-10) Duvid A Lockner 127 Rheology of Rocks (3-11) Brian Evans and David L Kohlstedt Phase Equilibria of Common Claude Herzberg 166 Reflectance Spectra Roger N Clark 148 Rocks in the Crust and Mantle (3-13) 178 Magnetic Properties of Rocks and Minerals Christopher P Hunt, Bruce M Moskowitz, Mixture Theories for Rock Properties James G Berryman 205 Index 229 (3-12) (3-15) (3-14) and Subir K Banerjee 189 PREFACE The purpose of this Handbook is to provide, in highly accessible form, selected critical data for professional and student solid Earth and planetary geophysicists Coverage of topics and authors were carefully chosen to fulfill these objectives These volumes represent the third version of the “Handbook of Physical Constants W Several generations of solid Earth scientists have found these handbooks’to be the most frequently used item in their personal library The first version of this Handbook was edited by F Birch, J F Schairer, and H Cecil Spicer and published in 1942 by the Geological Society of America (GSA) as Special Paper 36 The second edition, edited by Sydney P Clark, Jr., was also published by GSA as Memoir 92 in 1966 Since 1966, our scientific knowledge of the Earth and planets has grown enormously, spurred by the discovery and verification of plate tectonics and the systematic exploration of the solar system The present revision was initiated, in part, by a 1989 chance remark by Alexandra Navrotsky asking what the Mineral Physics (now Mineral and Rock Physics) Committee of the American Geophysical Union could produce that would be a tangible useful product At the time I responded, “update the Handbook of Physical Constants.” As soon as these words were uttered, I realized that I could edit such a revised Handbook I thank Raymond Jeanloz for his help with initial suggestions of topics, the AGU’s Books Board, especially Ian McGregor, for encouragement and enthusiastic support Ms Susan Yamada, my assistant, deserves special thanks for her meticulous stewardship of these volumes I thank the technical reviewers listed below whose efforts, in all cases, improved the manuscripts Thomas J Ahrens, Editor California Institute of Technology Pasadena Carl Agee Thomas J Ahrens Orson Anderson Don Anderson George H Brimhall John Brodholt J Michael Brown Bruce Buffett Robert Butler Clement Chase Robert Creaser Veronique Dehant Alfred G Duba Larry Finger Michael Gaffey Carey Gazis Michael Gumis William W Hay Thomas Heaton Thomas Herring Joel Ita Andreas K Kronenberg Robert A Lange1 John Longhi Guenter W Lugmair Stephen Ma&well Gerald M Mavko Walter D Mooney Herbert Palme Dean Presnall Richard H Rapp Justin Revenaugh Rich Reynolds Robert Reynolds Yanick Ricard Frank Richter Vii William I Rose, Jr George Rossman John Sass Surendra K Saxena Ulrich Schmucker Ricardo Schwarz Doug E Smylie Carol Stem Maureen Steiner Lars Stixrude Edward Stolper Stuart Ross Taylor Jeannot Trampert Marius Vassiliou Richard P Von Hetzen John M Wahr Yuk Yung Classification of Rocks and Their Abundances on the Earth Myron G Best consequentconsolidation of magma at any P, either at depth in the lithosphere or on the surface; these rocks were the fust to form on the primitive cooling Earth (2) Sedimentary rocks form by consolidationof particulate or dissolvedmaterial &rived by weathering of older rock and deposited by water, ice, organisms, or wind on the surface of the Earth; deposition and processes of consolidation occur at low, near-surfaceP and T (3) Metamorphic rocks form by recrystallization in the solid state, usually in the presence of aqueous fluids, cbi-ingingthe texture, structure, and/or composition of the protolith the sedimentary, magmatic, or even metamorphic precursor Metamorphism is the result of significant changesin the geologic environment from that in which the protolith originated Temperatures of metamorphism are elevated but submagmatic, pressures range widely, and nonhydrostatic (deviatoric) states of stress are common Distinguishing between thesethree basic kinds of rocks is readily accomplishedin most cases,but some i.nstances demand attention to multiple criteria [12, p 71 Classification within each of the three basic groups of rocks which follows is based chiefly upon their texture and composition as can be observed mostly in hand sample or outcrop These are essentially descriptive or nongenetic classifications for the nonspecialist which require little or no detailed laboratory analyses and extensive training in petrology Texture and composition contain a wealth of genetic information, but the tools to decipher them are beyond the scopeof this brief section It must be kept in mind that any subdividing by geologists of the broad spectrum of texture and composition in rocks is mostly arbitrary or follows tradition; boundarylines in nomenclaturediagramsarefir INTRODUCTION Rocks comprising the lithosphere have formed by interactionsbetweenmatter and various forms of energy-chiefly gravitational and thermal over the 4.5 Ga history of the Earth The wide range of rock-forming geologic processes and environmental conditions (intensive parameters) of temperature (T), pressure (P), and concentrations of chemical species related to these complex interactionshascreateda similarly wide spectrum of rock properties Significant widely-ranging rock properties are: (1) Texture, the size and shapeof mineral grains and amount of glass (crystalline and amorphous solids, respectively) (2) Structure of grain aggregates, such as bedding (3) Composition of mineral grains comprising the rock their relative proportions (mode), and the elemental and isotopic composition of the bulk rock Bodies of rock formed within a more or less unified geologic system over a particular period of time are rarely strictly homogeneous any scale of observation Many on rock bodies are anisotropic with regard to texture and structure, which is reflected in anisotropic physical properties such as elastic wave velocity Three main categoriesof rock magmatic, sedimentary, and metamorphic arerecognizedon the basisof geologic processesof origin and indirectly on P-T conditions (1) Magmatic, or igneous, rocks form by cooling and M G Best, Department ty, Provo, Utah 84602 of Geology, Brigham Young Universi- Rock Physics and Phase Relations A Handbook of Physical Constants AGU Reference Shelf Copyright 1995 by the American the convenience of the user and not denote nahuallyoccurring divisions Geophysical Union CLASSIFICATION OF ROCKS CL4SSIFICATION OF MAGMATIC OUARTZ ROCKS Figure presents an overview of the texmralcompositionalaspectsof the most common magmatic rock types and groups that occur in relatively large volume in subduction zone settings, but not exclusively in them Volcanic and plutonic (intrusive magmatic) environments grade continuously from one to the other, as many textures, including: (1) Glassy, formed by quick quenchingof silicate melt (2) Aphanitic, microcrystalline, grains are too small to be identifiable without a microscope (3) Phaneritic, all minerals grains are large enough to be identifiable by naked eye; formed in deep plutons (4) Porphyritic, larger crystals (phenocrysts)embeddedin a fmer grained or glassy matrix Mineral associations in Figure are useful aids in classifying Compositional modifiers silicic, felsic, intermediate, ma& and ultramajk defined chiefly on the basis of mineral proportions but indirectly on concentrationof silica can be appliedregardlessof texture The classification of magmatic rocks has recently been systematized by the International Union of Geological Sciences113)and their guidelinesare followed here, with simplifications > Y”KPl E G 21TL f&- PHANERITIC ‘$ a 5EC wt 100 % SiO, - - - _ T granodiorite granite diorite felsic silicic \ intermedlate 65 : mafic 52 t ultramafic 45: Fig Classification of common magmatic rock types found commonly, but not exclusively, in subduction zones Note general mineral associations Komatiite is a rare but significant rock formed from extruded lava flows almost exclusively in the Archean (>2500 Ma) See Table for mineral compositions A i\ \ \ / ALKALI FFI DSPAR Dyc4IIIIL rocks I monzonitic rocks diorite 35 10 PLAGIOCLASE Fig Classification of phaneritic magmatic rocks containing mostly quartz, potassium-rich alkali feldspar, and plagioclase [simplified from 131 Note that the rock-type names are independent of mafic (ferromagnesian) minerals (but see Figure 1); hence, the relative proportions of quartz and feldspar-smust be recalculated from the whole-rock mode No magmatic rocks contain more than about 40 percent quartz See Table for mineral compositions Names of phaneriticrock types containingmostly quartz and feldspar, but including some biotite and amphibole, are shown in Figure Three special textures in mostly felsic rocks warrant special base names (appended compositional prefixes are optional) as follows: (1) Pegmatite, exceptionally mame-grained rock; grains generally ~1 cm and locally a meter or more (2) Aplite, fine phaneritic, sugary-textureddike rock (3) Porphyry, plutonic rock containing phenocrystsin an aphanitic matrix Some phaneritic rocks, known as anorthosite, are composedof plagioclase,no quartz, and little or no matic minerals Phaneritic rocks containing only pyroxene and olivine are classified in Figure Theseperidotites and pyroxenites occur in some large intrusions of basaltic magma which have experienced crystal fractionation during cooling But their chief occurrence is in the upper mantle of the Earth, pieces of which commonly possessing metamorphic texture are found as inclusions in alkali basalt and kimberlite (see below) and in ophiolite slices kilometers long of oceaniclithosphereemplacedonto crust overlying subductingplates (Table 1) In the absence a whole-rock chemicalanalysis,glassy of BEST OLIVINE ORTHOPYROXENE CLINOPYROXENE Fig Classification of phaneritic rocks containing only olivine, clinopyroxene, and orthopyroxene [13] Rocks containing between 90 and 40 percent olivine are peridotite Rocks containing