Observations of eclipses of UU Sge     

V. V. Shimansky  N. V. Borisov  I. F. Bikmaev  N. N. Shimanskaya 《Astronomy Reports》2012,56(6):456-462

We have performed spectroscopy and photometry of eclipses of the pre-cataclysmic variable UUSge using the 6-m telescope of the Special AstrophysicalObservatory and the 1.5-mRussian-Turkish telescope. Our analysis of variations of the B-V and V-R color indices during the eclipses indicates that the temperature of the secondary is T _eff,2 = 6000?6300 K. A similar value, T _eff,2 = 6200 ± 200 K, follows from our comparison of the observed spectrum of UU Sge at the total eclipse phase and theoretical spectra of late-type stars. We identify 27 absorption lines of 11 chemical elements in the secondary??s spectrum. Their abnormal intensities indicate possible high-velocity turbulent motions (up to ?? _turb = 10.0 km/s) in the atmosphere of the star and the presence of hot gas above its surface.  相似文献   

Measurement of the effects of temperature and partial pressure of oxygen on the oxidation states of europium in silicate glasses     

R.V Morris  L.A Haskin  G.M Biggar  M.J O&#x;hara 《Geochimica et cosmochimica acta》1974,38(9):1447-1459

The techniques of electron paramagnetic resonance (EPR) were used to measure the concentration ratio of Eu²⁺ to Eu³⁺ in quenched CaMgSi₂O₆, Ca₃Si₃O₁₂, and CaAl₂Si₂O₈ liquids as functions of partial pressure of oxygen and temperature. The redox equilibrium of the Eu ions was described by the reaction 4Eu³⁺ + 20^2? = 4Eu²⁺ + O₂. The reduction of Eu³⁺ to Eu²⁺ was endothermic, and for CaMgSi₂O₆ and Ca₃Al₂Si₃O₁₂ liquids the mean value of ΔH⁰ and the standard deviation from that mean were 25 ± 7 kcal/mole.The magnitude of the Eu anomaly in the distribution coefficients is discussed in terms of the compositions of the solid and liquid phases.  相似文献   

Effect of pressure on the diffusivity of network-forming cations in melts of jadeitic compositions     

Ikuo Kushiro 《Geochimica et cosmochimica acta》1983,47(8):1415-1422

The diffusivities of network-forming cations (Si⁴⁺, Al³⁺, Ge⁴⁺ and Ga³⁺) in melts of the jadeitic composition NaAl(Si, Ge)₂O₆ and Na(Al, Ga)Si₂O₆ have been measured at pressures between 6 and 20 kbar at 1400°C. The rates of interdiffusion of Si⁴⁺-Ge⁴⁺ and Al³⁺-Ge³⁺ increase with increasing pressure at constant temperature. The results are consistent with the ion-dynamics computer simulations of Jadeite melt by Angellet al. (1982, 1983). The coefficient measured for the Si⁴⁺-Ge⁴⁺ interdiffusion is between 8 × 10^?10 and 2.5 × 10^?8$\text{cm}{}^2\text{sec}$ at 6 kbar, depending on the composition of the melt, whereas at 20 kbar it is between 7 × 10^?9 and 2 × 10^?7$\text{cm}{}^2\text{sec}$. The effect of pressure is greater for more Si-rich compositions (i.e., closer to NaAlSi₂O₆ composition). The coefficient measured for the Al³⁺-Ga³⁺ inter- diffusion is between 9 × 10^?10 and 3 × 10^?9 cm²/sec at 6 kbar and between 3 × 10^?9 and 1 × 10^?8$\text{cm}{}^2\text{sec}$ at 20 kbar. The rate of increase in diffusivity with pressure of Al³⁺-Ga³⁺ (a factor of 3–4) is smaller than that of Si⁴⁺-Ge⁴⁺ (a factor of 7–17).The Si⁴⁺-Ge⁴⁺ interdiffusion in melts of Na₂O · 4(Si, Ge)O₂ composition has also been measured at 8 and 15 kbar for comparison. The effect of pressure on the diffusivity in this melt is significantly smaller than that for the jadeitic melts. The increase in diffusivity of the network-forming cations in jadeitic melts with increasing pressure may be related to the decrease in viscosity of the same melt. The present results, as well as the ion-dynamics simulations, suggest that the homogenization of partial melts and mixing of magmas would be more efficient at greater depths.  相似文献   

Kinetics of dehydration of Ca-montmorillonite     

H. J. Bray  S. A. T. Redfern 《Physics and Chemistry of Minerals》1999,26(7):591-600

Isothermal thermogravimetric experiments have been carried out to determine the reaction kinetics of the dehydration processes in fuller's earth, a natural Ca-montmorillonite. Dehydration in swelling clays is a complex reaction, and analysis of the thermogravimetric data using empirical rate equations and time-transformation analysis reveals that the nature of the rate controlling mechanism is dependent upon both the temperature regime of the sample as well as the extent of reaction. For fuller's earth, we find that the dehydration kinetics are dominated by a nucleation and growth mechanism at low temperatures and fractions transformed (stage I), but above 90 °C the last stages of the reaction are diffusion controlled (stage II). The activation energy for dehydration during stage I is around 35 kJ · mol⁻¹, whereas the removal of water during stage II requires an activation energy of around 50 kJ · mol⁻¹. These two stages of dehydration are associated with primary collapse of the interlayer (stage I) and movement of water that is hydrated to cations within the interlayer (stage II). Received: 28 August 1998 / Revised, accepted: 27 January 1999  相似文献   

Computation of the seismic stability of rock wedges   总被引：1，自引：0，他引：1  

A. Ghosh  W. Haupt 《Rock Mechanics and Rock Engineering》1989,22(2):109-125

Summary Newmark's concept of computing the permanent displacement under seismic loads has been combined with the conventional limit equilibrium analysis to compute the displacements of a rock wedge. The rock wedge formed by the intersecting planes may or may not have a tension crack in the upper slope surface. As the static analysis of a rock wedge is available from the literature, only the seismic problem is treated theoretically in more details.A computer program has been developed to compute the displacements from the digitised input data of the acceleration-time-history. The program can take into account the water pressure on the intersecting planes and on the planes of the tension crack. The effect of rock anchors if present is also taken care of in addition to static surcharge loads. The program calculates the conventional static factor of safety, remaining resistance against sliding, the critical acceleration, exciting force, relative velocity with time and the cumulative displacements.Two model examples are presented: one with simple sinusoidal acceleration and the other one with actual earthquake data considering the different systems of forces acting on the wedge. The results are critically discussed with respect to the different parameters e. g. anchor forces, water pressure and cohesion influencing the magnitude of displacements under seismic loads. It is shown that the critical acceleration is a better index for the seismic stability than the conventional factor of safety.The critical acceleration presented in this paper serves as a very handy tool for a site engineer to get the first hand information about the stability of the wedge for a given acceleration-time-history without going into the details of dynamic analysis.Notations A, B Inclined intersecting planes - C, D Geometric points on the intersection ofA andB - a _cr Critical acceleration - a _h Horizontal acceleration - a _v Vertical acceleration - a _r Relative acceleration of the wedge - DF Driving force - DF _dyn Dynamic driving force - DF _st Static driving force - FS Factor of safety - g Acceleration due to gravity - m Mass of the wedge - RF Resisting force - RF _dyn Dynamic resisting force - RF _st Static resisting force - RS Remaining resisting force against sliding - RS _dyn Total seismic induced force - RS _st Remaining static resisting force against sliding - s _r Cumulative relative displacement of the wedge - TRS Total remaining resisting force against sliding - v _r Relative velocity of the wedge - W Weight of the wedge - W _A ,W _B Weight of the wedge in the planeA andB - Dip of line of intersection of the planesA andB - Average friction angle - _A , _B Friction angle of planeA andB - I, II, III, IV Points in the curve shown in Fig. 6  相似文献   

Effects of pH and temperature on dimerization rate of glycine: Evaluation of favorable environmental conditions for chemical evolution of life     

Kasumi Sakata  Norio Kitadai 《Geochimica et cosmochimica acta》2010,74(23):6841-6851

To evaluate favorable environmental conditions for the chemical evolution of life, we studied the effects of pH and temperature on the dimerization rate of glycine (Gly: NH₂-CH₂-COOH), one of the simplest amino acids. Gly dimerizes to form glycylglycine (GlyGly), and GlyGly further reacts to form diketopiperazine (DKP). Gly solutions with pH ranging from 3.1 to 10.9 were heated for 1-14 days at 140 °C, and changes in concentrations of Gly, GlyGly, and DKP were evaluated. At pH 9.8, the experiments were conducted at 120, 140, 160, and 180 °C. The dimerization rate of Gly was nearly constant at pH 3-7 and increased with increasing pH from 7 to 9.8 and then decreased with further increases in pH. To elucidate the reason for this pH dependency, we evaluated the role of the three dissociation states of Gly (cationic state: Gly⁺, zwitterionic state: Gly^±, and anionic state: Gly⁻). For pH >6, the dominant forms are Gly^± and Gly⁻, and the molar fraction of Gly^± decreases and that of Gly⁻ increases with increasing pH. The dimerization rate was determined for each dissociation state. The reaction between Gly^± and Gly⁻ was found to be the fastest; the rate constant of the reaction between Gly^± and Gly⁻ was 10 times the size of that between Gly⁻ and Gly⁻ and 98 times that between Gly^± and Gly^±. The dimerization rate became greatest at pH 9.8 because the molar fractions of Gly^± and Gly⁻ are approximately equal at this pH. The dimerization rate increased with temperature, and an activation energy of 88 kJ mol⁻¹ was obtained. Based on these results and previous reports on the stability of amino acids under hydrothermal conditions, we determined that Gly dimerizes most efficiently under alkaline pH (∼9.8) at about 150 °C.  相似文献   

The geochemistry of the stable isotopes of silicon   总被引：1，自引：0，他引：1  

C.B Douthitt 《Geochimica et cosmochimica acta》1982,46(8):1449-1458

One hundred thirty two new measurements of the relative abundances of the stable isotopes of silicon in terrestrial materials are presented. The total variation of ^δ30Si found is 6.2%., centered on the mean of terrestrial mafic and ultramafic igneous rocks, δ³⁰Si = ?0.4%.. Igneous rocks show limited (1.1%.) variation; coexisting minerals exhibit small, systematic silicon isotopic fractionations that are roughly $\text{1}\text{3}$ the magnitude of concomitant oxygen isotopic fractionations at 1150°C. In both igneous minerals and rocks, δ³⁰Si shows a positive correlation with silicon content, as does δ¹⁸O. Opal from both sponge spicules and sinters is light, with $\text{}\text{?}\text{gd}{}^{30}\text{Si}\text{= ?2.3}$ and ?1.4%., respectively. Large ^δ30Si values of both positive and negative sign are reported for the first time from clay minerals (?2.3 to +1.8%.), opaline phytoliths (?1.4 to +2.8%.), and authigenic quartz (+ 1.4%.). All highly fractionated samples were precipitated from solution at low temperatures; however, aqueous silicon is not measurably fractionated relative to quartz at equilibrium. A kinetic isotope fractionation of ≈3.5%. is postulated to occur during the low temperature precipitation of opal and, possibly, poorly ordered phyllosilicates, with the silicate phase being enriched in ²⁸Si. This fractionation, coupled with a Rayleigh precipitation model, is capable of explaining most non-magmatic δ³⁰Si variations. Chert ^δ30Si values are largely inherited, but the primary opal ^δ30Si values can be modified by isotopic equilibration of silicate silicon and dissolved silicon during the transformation of opal into quartz.  相似文献   

Pressure dependence of structural parameters of paragonite     

Paola Comodi  Pier Francesco Zanazzi 《Physics and Chemistry of Minerals》1997,24(4):274-280

The compressibility and structure of a 2M₁ paragonite with composition [Na_0.88K_0.10Ca_0.01Ba_0.01] [Al_1.97Ti_0.007Fe_0.01Mn_0.002Mg_0.006]Si_3.01Al_0.99O₁₀OH₂ were determined at pressures between 1 bar and 41 kbar, by single crystal X-ray diffraction using a Merrill-Bassett diamond anvil cell. Compressibility turned out to be largely anisotropic, linear compressibility coefficients parallel to the unit cell edges being β_a=3.5(1)·10^?4, β_b=3.6(1)·10^?4, β_c=8.3(3)·10^?4 kbar^?1 (β_a:β_b·β_c=1:1028:2.371). The isothermal bulk modulus, calculated as the reciprocal of the mean compressibility of the cell volume, was 650(20) kbar. The main features of the deformation mechanism resulting from structural refinements at pressures of 0.5, 25.4, 40.5 kbar were: –?variation in sheet thickness, showing that compression of the c parameter was mainly due to the interlayer thickness reduction from 3.07 Å at 0.5 kbar to 2.81 Å at 40.5 kbar; –?the compressibility of octahedra was greater than that of tetrahedra, the dimensional misfit between tetrahedral and octahedral sheets increased with P, so that tetrahedral rotation angel α increased from 15° at 0.5 kbar to 21.6° at 40.5 kbar; –?the basal surface corrugation (Δz) of the tetrahedral layer, due to the different dimensions of M1 and M2 octahedra and to the octahedral distortion, decreased with P (Δz=0.19 and 0.12 Å at 0.5 and 40.5 kbar respectively). Comparison of the new data on paragonite with those of a K-muscovite and a Na-rich muscovite (Comodi and Zanazzi 1995) revealed a clear trend toward decreasing of compressibility when Na substitutes for K atoms in the interlayer sites.  相似文献   

The estimation of the experimental and basic components of the observed variance of rock strength     

J. P. G. Pretorius 《Rock Mechanics and Rock Engineering》1980,13(2):119-130

SummaryThe Estimation of the Experimental and Basic Components of the Observed Variance of Rock Strength The intercept of the strength correlelogram over distance is used to estimate the proportions of the observed strength variance which can be attributed to the testing (experimental) procedure and to the basic differences between the strengths of the specimens. The method is applied to sandstone uniaxial strength data (Wiid, 1968) where approximately half of the observed variance is experimental and half basic. A spatial trend accounts for most of the basic variance. The uniaxial strength is also spatially correlated with the triaxial strength. It is shown that the results of testing procedures of equal reliability will be poorly correlated if the experimental components of variance are large.

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ZusammenfassungDie Abschätzung der Anteile an den Streuungen der Festigkeiten von Fels, die den Versuchsverfahren bzw die den tatsächlichen Streuungen zuzuordnen sind Der Achsabschnitt im Druckfestigkeitskorrelelogramm wird verwendet, um die Anteile der beobachteten Druckfestigkeitsstreuungen, welche dem Versuchsverfahren bzw. den tatsächlichen Unterschieden zwischen den Druckfestigkeiten der Proben zuzuordnen sind, zu schätzen.Die Methode wird bei einachsialen Druckfestigkeiten eines Sandsteines (Wiid, 1968) angewandt, wobei ungefähr je die Hälfte der beobachteten Streuungen auf die Versuchstechnik bzw. auf tatsächliche Unterschiede zurückzuführen sind. Die einachsiale Druckfestigkeit wird auch mit der dreiachsialen Druckfestigkeit räumlich korreliert.Es wird gezeigt, daß die Ergebnisse der Testverfahren von gleicher Zuverlässigkeit schlechter korreliert werden können, wenn die experimentalen Komponenten an den Streuungen größer sind.

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RésuméL'estimation des parties constituantes expérimentales et fondamentales de la variance observée de la résistance de roche La valeur pour distance zéro de résistance du correlélogramme (en fonction de distance) est utilisée pour faire une estimation des proportions de la variance observée qui peuvent être attribuées au procédé expérimental ainsi qu'aux différences fondamentales entre les résistances des specimens. La méthode est appliquée à des données de résistance uniaxe de grès, ou à peu près la moitié de la variance observée est dûe à l'expérimentateur et le reste est fondamental. Une tendance spatiale explique la plûpart de la variance fondamentale. La résistance uniaxe est aussi corrélée spatialement avec la résistance triaxe. Il est démontré que les résultats des procédés expérimentaux qui sont de même fidélité seront mal corrélés si les partiés constituantes de variance expérimentales sont élevées.

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With 8 Figures  相似文献   

Kinetics of diffusion-controlled growth of fayalite   总被引：1，自引：0，他引：1  

D. K. Fisler  S. J. Mackwell 《Physics and Chemistry of Minerals》1994,21(3):156-165

The rate of growth of fayalite (Fe₂SiO₄) has been measured at one atmosphere total pressure, temperatures from 1000° to 1120° C, and oxygen fugacities controlled by CO/CO₂ gas-mixing from 10^-9.9 to 10^-13.0atm, chosen to span the fayalite stability field. The fine-grained polycrystalline fayalite layer was formed by reacting the oxides FeO or Fe₃O₄ with a thin slice of single-crystal quartz. The rate of growth of the fayalite increases with increasing temperature and decreasing oxygen fugacity, and is consistent with a parabolic rate law, indicating that the growth rate is controlled by diffusion through the fayalite. Microstructural observations and platinum marker experiments suggest that the reaction phase is formed at the quartz-fayalite interface, and is therefore controlled by the diffusion of iron and oxygen. The parabolic rate constant was analyzed in terms of the oxide activity gradient to yield mean chemical diffusivities for the rate-limiting ionic species, assuming bulk transport through the fayalite layer. Given that iron diffusion in olivine polycrystals occurs either by lattice diffusion, which shows a positive dependence on oxygen activity, or by grain boundary diffusion, which would result in growth rates significantly faster than we observe, we conclude that the diffusivities derived in this study represent oxygen diffusion. However, since oxygen lattice diffusion in fayalite has been established to be much slower than our measurements, it is likely that the transport path for oxygen is along the grain boundaries. Thus, the mean grain boundary diffusivity of oxygen in fayalite $\bar D$ _O ^gb (m² s^-1), using the measured grain size of 0.25 μm, is then given by $$\bar D_O^{gb} {\mathbf{ }}\delta = 1.28 \times 10^{ - 3} f_{O_2 }^{ - 0.17} {\mathbf{ }}e^{ - 540/RT} $$ , where δ is the grain boundary width (in m), and the activation energy is in kJ/mol. Assuming δ=10^-9 m (Ricoult and Kohlstedt 1983), the oxygen grain boundary diffusivities are about a factor of 30 × slower than those reported by Watson (1986) for Fo₉₀ olivine.  相似文献   

Overview of the geomorphological and hydrogeological characteristics of the Eastern Desert of Egypt   总被引：2，自引：1，他引：1  

A. A. Abdel Moneim 《Hydrogeology Journal》2005,13(2):416-425

Although, the Eastern Desert of Egypt forms about 22% of the surface area of the country, the area is undeveloped due to the limited availability of water. The morphologic units of the Eastern Desert consist of a number of drainage basins covering about 147,820 km² (66.5% of the total surface area of the Eastern Desert). The basins drain the occasional rainwater, either towards the Nile Valley or to the Red Sea, causing flood hazards. The availability of water from the hydrologic systems of these basins could be improved by constructing runoff controlling systems in these areas (e.g. dykes and partially effective dams), which could save and make use of a considerable amount of water. The groundwater resources in the Eastern Desert can be divided into four main water-bearing units: the fractured crystalline Pre-Cambrian aquifer, the Nubian sandstone aquifer, the fractured limestone and sandstone aquifer and the Quaternary aquifer. The most productive aquifer is the Nubian sandstone while the fractured limestone and sandstone (Miocene) are only productive along the eastern part of the desert. The Quaternary aquifer occurs along the major dry washes (wadis) and is considered of limited potential as it is recharged mainly from the occasional rainfall. Detailed assessment of these aquifers should be carried out locally for further development of the area.

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Resumen Aunque el Desierto Oriental de Egipto constituye alrededor del 22% de la superficie del país, esta área no se encuentra desarrollada por causa de la escasez de agua. Las unidades morfológicas del Desierto Oriental consisten de un número de cuencas de drenaje que cubren alrededor de 147,820 km² (66.5% del área superficial total del Desierto Oriental). Estas cuencas drenan las aguas lluvias ocasionales, bien hacia el Valle del Nilo o hacia el Mar Rojo, causando amenazas de inundación. La disponibilidad de agua a partir de los sistemas hidrológicos de estas cuencas, puede ser mejorada al construir sistemas de control de escorrentía allí (Ej. Diques y presas de efectividad parcial), las cuales podrían almacenar y permitir el uso de una cantidad considerable de agua. Los recursos de agua subterránea en el Desierto Oriental, pueden dividirse en cuatro unidades principales portadoras de agua: El acuífero fracturado cristalino Pre – Cámbrico, el acuífero de la Arenisca de Nubia, el acuífero de arenisca y caliza fracturadas y el acuífero Cuaternario. El acuífero más productivo es la arenisca de Nubia, mientras que la arenisca y caliza fracturadas (Mioceno), son productivas únicamente a lo largo de la parte oriental del desierto. El acuífero Cuaternario se encuentra a lo largo de las corrientes intermitentes mayores (Wadis) y se le considera de potencial limitado por ser recargado principalmente a partir de lluvia ocasional. Una evaluación detallada de estos acuíferos debe llevarse a cabo localmente, para el desarrollo adicional de esta área.

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Résumé Bien que le Désert Est occupe 22% de la surface de lEgypte, la région est sousdeveloppée à cause de la ressource en eau limitée. Les unités morphologiques consistent en des bassins drainant qui couvrent une surface de 147,820 km² ,représentant 66.6% de la surface du Désert Est. Les bassins drainent les plues intermittentes vers la vallée du Nil ou vers la Mer Rouge en provocant des inondations. On peut augmenter la ressource en eau dans cette région en réalisant des systèmes de contrôle de ruissellements (des digues...) qui peuvent sauver et utiliser un volume considérable deau. La ressource en eau souterraine du Désert Est est cantonnée dans quatre grandes structures: l› aquifère fracturé cristallin Précambrien, l› aquifère gréseux Nubien, l› aquifère calcaire et gréseux et l› aquifère quaternaire. Le plus productif est l› aquifère gréseux Nubien tendis que les calcaire et les grèses dage miocène sont productives seulement dans la partie est du désert. L› aquifère quaternaire se trouve au long des oueds sèches et on considéré quil a un potentiel limité, étant rechargé seulement par les plues intermittentes. Pour le futur développement de la région il est nécessaire une évaluation détaillée, à léchelle locale de ces aquifères.

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