A sampling of Mesozoic and Tertiary basalts in Lebanon yielded the following information:
Age
D
I
α95
Pole position
dp
dm
Upper Jurassic
95
+21
10.6
114E 2N
5.9
11.2
66W 2S
Lower Cretaceous
122
+2
9.0
105E 25S
4.5
9.0
75W 25N
Upper Pliocene
2
+46
7.7
169E 88N
6.3
9.8
11W 88S
Full-size table
These results confirm and amplify earlier work by Van Dongen et al., and can be interpreted as indicating a net anticlockwise rotation of Lebanon relative to the African tectonic plate amounting to about 70° during the Late Jurassic-Pliocene interval. This could have resulted from differential movement between the African and European plates as they made way for the growing Atlantic Ocean. 相似文献
Occurrence of small (3 ML < 4) earthquakes on two 10-km segments of the Calaveras fault between Calaveras and Anderson reservoirs follows a simple linear pattern of elastic strain accumulation and release. The centers of these independent patches of earthquake activity are 20 km apart. Each region is characterized by a constant rate of seismic slip as computed from earthquake magnitudes, and is assumed to be an isolated locked patch on a creeping fault surface. By calculating seismic slip rates and the amount of seismic slip since the time of the last significant (M 3) earthquake, it is possible to estimate the most likely date of the next (M - 3) event on each patch. The larger the last significant event, the longer the time until the next one. The recurrence time also appears to be increased according to the moment of smaller (2 < ML < 3) events in the interim. The anticipated times of future larger events on each patch, on the basis of preliminary location data through May 1977 and estimates of interim activity, are tabulated below with standard errors. The occurrence time for the southern zone is based on eight recurrent events since 1969, the northern zone on only three. The 95% confidence limits can be estimated as twice the standard error of the projected least-squares line. Events of M 3 should not occur in the specified zones at times outside these limits. The central region between the two zones was the locus of two events (M = 3.6, 3.3) on July 3, 1977. These events occurred prior to a window based on the three point, post-1969 slip-time line for the central region.
Based on the oxygen isotopic compositions of 133 wolframite samples and 110 quartz samples collected from 30 tungsten ore
deposits in south China, in conjunction withδD values and other data, these deposits can be divided into four types.
(1)
Reequilibrated magmatic water-hydrothermal tungsten ore deposits. Theδ18O values of wolframite and quartz samples from this type of tungsten ore deposits are about +5–+12‰, respectively. The calculatedδ18O
values of ore fluids in equilibrium with quartz are about +6.5‰, and theδ
values of fluid inclusions in quartz range from −40 to −70‰
(2)
Meteoric water-hydrothermal tungsten ore deposits. Theδ18O values of wolframite in this type of tungsten deposits are around −1‰
(3)
Stratiform tungsten ore deposits. In these deposits, theδ18O values of quartz and wolframite are about +17 and +3‰, respectively. It is considered that these stratiform tungsten ore
deposits are genetically related to submarine hot-spring activities.
(4)
Complex mixed-hydrothermal tungsten ore deposits. These tungsten ore deposits are characterized by multi-staged mineralization.
Theδ18O values of early wolframite are around +5‰, but of later wolframite are lower than +4‰, indicating that the early wolframite
was precipitated from reequilibrated magmatic water-hydrothermal solutions and the late one from the mixture of hydrothermal
solutions with meteoric waters or mainly from meteoric waters.
Based on theδ18O values of the coexisting quartz and wolframite and temperature data, two calibration equilibrium curves have been constructed,
and the corresponding equations have been obtained:
In Provence and Languedoc, four drowning events were identified in platform carbonates of late Barremian–Bedoulian age. Their recognition is based on sedimentological and stratigraphical evidence, and their timing, referred to ammonite zones or subzones, is as follows:
(1)
Late Barremian, at the G. sartousiana–Imerites giraudi transition, or merely the lowermost part of the I. giraudi zone,
(2)
Middle Bedoulian, at the Deshayesitesweissi–Deshayesites deshayesi transition,
(3)
Mid late Bedoulian in correspondence with the “Roloboceras hambrovi subzone”,
(4)
Late Bedoulian at the Deshayesites grandis–Deshayesites furcata transition.
Corresponding events are also well expressed in basinal settings where they are marked by significant facies and faunal changes.These four successive drowning events distinguish four successive steps in platform development and demise. Step 1 was coeval with the onset of the Bedoulian palaeogeography and started after drowning event (1) with a drastic reduction of shallow platform settings with rudists, usually replaced by Palorbitolina facies. The ensuing recovery of rudist facies and, following drowning event (2), subsequent step 2 marked the developmental phase of the platform system, whereas steps 3 and 4, each prefaced by a drowning event, were associated with its demise. Step 1 represents the major spreading phase of the Urgonian type facies spectrum including bioclastics, coral and rudist facies groups. In Provence, step 1 was characterized by a bipolar (N-S) progradation, and aggradation was coeval with a maximum of subsidence. The termination of step 1 was marked by the emergence of the antecedent platform margin. Step 2, which followed the disappearance of rudist facies and the extreme spatial reduction of both coral and bioclastic facies, started with the flooding of the antecedent platform and the development of Palorbitolina and cherty limestones. Shallow water bioclastics and/or coral facies recovered rapidly on top of the pre-existing emerged areas and developed locally as bioclastic shoals. Step 2 documents a regional reorganisation of subsidence patterns.The infralittoral (high illuminated environments) “Urgonian facies” are therefore essentially present in the Lower Bedoulian, and circalittoral (relatively deep low illuminated environments) deposits dominate in the Upper Bedoulian. This pattern, typical for SE France and wide parts of the Helvetic shelf, departs from that of adjacent regions (e.g. SW France, Spain) where late Bedoulian platform carbonates have a significant record. The record thus shows that the demise of the Urgonian platform was a step-wise phenomenon which cannot be ascribed to a single event, i.e. the Goguel/Selli OAE1a main event. 相似文献
The density ρ of Caspian Sea waters was measured as a function of temperature (273.15–343.15) K at conductivity salinities
of 7.8 and 11.3 using the Anton-Paar Densitometer. Measurements were also made on one of the samples (S = 11.38) diluted with water as a function of temperature (T = 273.15–338.15 K) and salinity (2.5–11.3). These latter results have been used to develop an equation of state for the Caspian
Sea (σ = ±0.007 kg m−3)
where ρ0 is the density of water and the parameters A, B and C are given by
Measurements of the density of artificial Caspian Sea water at 298.15 K agree to ± 0.012 kg m−3 with the real samples. These results indicate that the composition of Caspian Sea waters must be close to earlier measurements
of the major components. Model calculations based on this composition yield densities that agree with the measured values
to ± 0.012 kg m−3. The new density measurements are higher than earlier measurements. This may be related to a higher concentration of dissolved
organic carbon found in the present samples (500 μM) which is much higher than the values in ocean waters (~65 μM). 相似文献
Within the context of the phase IV (1994–1996) research and development activities at the Grimsel Test Site (GTS), Nagra developed, in collaboration with the Agence Nationale pour la Gestion des Déchets Radioactifs (Andra), an investigation project for the sealing of boreholes drilled from underground. The project had the following goals:
–
sealing of boreholes drilled from underground facilities with a length of up to 500 m,
–
sealing of boreholes with mainly irregular shape (e.g. breakouts of borehole wall),
–
ensuring a hydraulic conductivity of 10−11–10−12 m/s for the seal,
–
ensuring reliable quality control in routine production.
The new concept developed in this project was to use highly compacted bentonite pellets only. The two techniques tested were
(1)
pneumatic injection of pellets into a borehole using a grain size distribution of 4–10 mm,
(2)
emplacement using a modified core barrel for transport and compaction of the pellets.
Both techniques were tested in situ at the GTS to estimate their performance under realistic field conditions. The swelling pressures were monitored for 4 months after seal emplacement until an almost constant value was attained. Finally the hydraulic and mechanical performance of the seal was tested. It was found that the conductivities measured across the seal were equivalent to the matrix properties of the surrounding rock (2–5 × 10−12 m/s). The hydraulic testing also showed no linear preferential flow. 相似文献
A study of the synoptic situation which produced the catastrophic floods of November 1988 in Catalonia (in the northeast of the Iberian Peninsula) is presented. Analyses of the vertical structure, potential instability, precipitable water, and instability index are made through the radiosounding data from Palma, Majorca. It is found that the 1988 situation is included in type I intense convective events in Catalonia (classification obtained from all the events since 1950, (Llasat, 1989)). It was characterized by:
(a)
-pattern in the middle and high troposphere, the ridge axis east of Catalonia.
(b)
High pressure over Europe.
(c)
South-easterly winds in the lower troposphere with warm and moist humid air advection and south-westerlies aloft over Catalonia.
Zirconolite, aeschynite-(Ce), titanite and apatite have been found as minor or accessory minerals in a Ti-rich (TiO2=2.1–4.5 wt.%) hydrothermal vein occurring in dolomite marbles at the contact with a tonalite intrusion of the Tertiary Adamello batholith (northern Italy). The vein consists of four distinct mineral zones, comprising from margin to center: (1) forsterite+calcite, (2) pargasite+calcite+titanite+sulfides, (3) phlogopite +calcite+titanite+sulfides, and (4) titanian clinohumite +spinel+calcite+sulfides. Zirconolite occurs in two vein zones only: in the phlogopite zone it is invariably anhedral, often corroded, and exhibits complex chemical zonation patterns. In the titanian clinohumite zone zirconolite is idiomorphic and characterized by a pronounced discontinous chemical zoning, but shows no evidence of corrosion. The considerable compositional variation observed for zirconolite (in wt.%: (REE2O3)=0.74–16.8, UO2=0.59–24.0, ThO2=0.67–17.1) is due to the zoning, and may be attributed to four major substitutions described by the exchange vectors:
1.
(Th, U) (Mg, Fe2+) Ca-1 Ti-1
2.
REE Al Ca-1 Ti-1
3.
REE Fe2+ (Nb, Ta) Ca-1 Ti-1
4.
Hf Zr-1
Exchange vector (2) is effective at total REE2O3 contents up to approximately 5 wt.%, whereas vector (3) is operating at higher concentrations. Both titanite and aeschynite-(Ce) exhibit, like zirconolite, complex chemical zonation patterns which document that the trace element content of the metasomatic fluid was variable during the vein-forming process. As indicated by thermodynamic analysis of the phase assemblages, the vein zones containing the REE-bearing minerals formed at 500–600°C (Ptotal2 kbar) from a reducing fluid rich in H2S, HCl°, HF° and phosphorus, but relatively poor in CO2(XCO2 0.2). Geochemical and isotopic data are consistent with the interpretation of the fluid as being derived from the nearby tonalite intrusion. The abundance of idiomorphic fluor-apatite as well as textural relations between apatite, the other REE-bearing minerals and the fluorine-bearing hydrous silicates suggest F- and PO
43-
to be the most likely ligands for complexing REE, Ti, Zr and other high-field-strength elements in the veinforming fluid. The corrosive features observed for zirconolite demonstrate that hydrothermal fluids are able to dissolve zirconolite, which is one of the main components of SYNROC-C, the most promising disposal option for high-level nuclear waste. Therefore, immobilization of radioactive waste in zirconolite can be guaranteed only if an effective sealing material prevents any hydrothermal fluid from access to the final disposal site. 相似文献
The heat capacities of synthetic pyrope (Mg3Al2Si2O12), grossular (Ca3Al2Si3O12) and a solid solution pyrope60grossular40 (Mg1.8Ca1.2Al2Si3O12) have been measured by adiabatic calorimetry in the temperature range 10–350 K. The samples were crystallized from glasses in a conventional piston-cylinder apparatus.The molar thermophysical properties at 298.15 K (J mol?1 K?1) are:
The experiments of the dissolution kinetics of fluorite were performed in aqueous HCl solutions over the temperature range
of 25–100 °C using a flow-through experimental apparatus. With a constant input of aqueous HCl solution through the reactor,
output concentrations of the dissolved species Ca, F, Cl vary with flow rate, as well as with the surface compositions. Measured
output concentrations of dissolved species and the pH can be used to determine a rate law for fluorite dissolution. Fluorite
dissolution rates are found to be pH dependent. Usually, dissolution rates of fluorite decreases with increasing dissolved
Ca in the output solution at 25 and 100 °C. Dissolution rate can be expressed as
(1a)
where k is the rate constant and α is the order with respect to the hydrogen ion activity vs. the activity of dissolved Ca. The α was obtained from kinetic experiments. For the fluorite sample passed through 18–35 mesh, α =1.198 at 100 °C and k = 10−0.983, while fluorite dissolved in HCl–H2O solution at pH 2.57 of input solution. Adsorption of a proton and Cl−1onto the fluorite surface, surface cation exchange and the formation of the surface complex Ca(F, Cl)2 and/or (H2x, Ca1−x)(F, Cl)2 control dissolution rates. Investigation of the fluorite surface before and after dissolution by using X-ray photoelectron
spectroscopy (XPS) indicate that surface modifications affect reaction rates. 相似文献
A differential rate equation for silica-water reactions from 0–300°C has been derived based on stoichiometry and activities of the reactants in the reaction SiO2(s) + 2H2O(l) = H4SiO4(aq) where () = (the relative interfacial area between the solid and aqueous phases/the relative mass of water in the system), and k+ and k? are the rate constants for, respectively, dissolution and precipitation. The rate constant for precipitation of all silica phases is and Eact for this reaction is 49.8 kJ mol?1. Corresponding equilibrium constants for this reaction with quartz, cristobalite, or amorphous silica were expressed as . Using , k was expressed as and a corresponding activation energy calculated:
We present a theoretical model for diffusive daughter isotope loss in radiochronological systems with increasing temperature.
It complements previous thermochronological models, which focused on cooling, and allows for testing opening and resetting
of radiochronometers during heating. The opening and resetting temperatures are, respectively,
where R is the gas constant, E and D0 are the activation energy and the pre-exponential factor of the Arrhenius law for diffusion of the daughter isotope, a the half-size of the system (radius for sphere and cylinder and half-thickness for plane sheet) and τ the heating time constant, related to the heating rate by
For opening and resetting thresholds corresponding to 1 and 99% loss of daughter isotope, respectively, the retention parameters
for sphere, cylinder and plane sheet geometries are Aop = 1.14 × 105, 5.07 × 104 and 1.27 × 104 and Ars = 2.40, 1.37 and 0.561. According to this model, the opening and resetting temperatures are significantly different for most
radiochronometers and are, respectively, lower and higher than the closure temperature.
Electronic supplementary material The online version of this article (doi:) contains supplementary material, which is available to authorized users. 相似文献
A complete set of new optical and x-ray data is given for eleven analyzed alkali amphiboles [Na2(Mg, Fe″)3(Al, Fe?)2Si8O22(OH)2]. Nine new wet chemical analyses are reported. Using additional selected data from the literature, variation in refractive indices, extinction angles (γ-α), optic angles, density, lattice constants and cell volume are expressed graphically as a function of composition in the glaucophane-riebeckite and magnesiorie-beckite-ferroglaucophane series. Four orientations (G, C, O, and R) of the optical indicatrix within the structure are described and shown to be characteristic of the chemical species glaucophane (G), crossite (C), magnesioriebeckite (O), riebeckite (O), and riebeckite-arfvedsonite (R and O). Optical properties of the pure end members by extrapolation are:
The thermodynamic stability constants for the hydrolysis and formation of mercury (Hg2+) chloride complexes
have been used to calculate the activity coefficients for Hg(OH)n(2–n)+ and HgCln(2–n)+ complexes using the Pitzer specific interaction model. These values have been used to determine the Pitzer parameters for
the hydroxide and chloro complexes and CML). The values of and have been determined for the neutral complexes (Hg(OH)2 and HgCl2). The resultant parameters yield calculated values for the measured values of log to ±0.01 from I = 0.1 to 3 m at 25°C. Since the activity coefficients of and are in reasonable agreement with the values for Pb(II), we have estimated the effect of temperature on the chloride constants
for Hg(II) from 0 to 300°C and I = 0–6 m using the Pitzer parameters for complexes. The resulting parameters can be used to examine the speciation of Hg(II) with Cl− in natural waters over a wide range of conditions. 相似文献
Volume diffusion rates of Ce, Sm, Dy, and Yb have been measured in a natural pyrope-rich garnet single crystal (Py71Alm16Gr13) at a pressure of 2.8 GPa and temperatures of 1,200-1,450 °C. Pieces of a single gem-quality pyrope megacryst were polished, coated with a thin layer of polycrystalline REE oxide, then annealed in a piston cylinder device for times between 2.6 and 90 h. Diffusion profiles in the annealed samples were measured by SIMS depth profiling. The dependence of diffusion rates on temperature can be described by the following Arrhenius equations (diffusion coefficients in m2/s): % MathType!MTEF!2!1!+- % feaaeaart1ev0aaatCvAUfKttLearuavTnhis1MBaeXatLxBI9gBam % XvP5wqSXMqHnxAJn0BKvguHDwzZbqegm0B1jxALjhiov2DaeHbuLwB % Lnhiov2DGi1BTfMBaebbfv3ySLgzGueE0jxyaibaieYlf9irVeeu0d % Xdh9vqqj-hEeeu0xXdbba9frFj0-OqFfea0dXdd9vqaq-JfrVkFHe9 % pgea0dXdar-Jb9hs0dXdbPYxe9vr0-vr0-vqpWqaaeaabiGaciaaca % qabeaadaabauaaaOqaauaabeqaeeaaaaqaaiGbcYgaSjabc+gaVjab % cEgaNnaaBaaaleaacqaIXaqmcqaIWaamaeqaaOGaemiraq0aaSbaaS % qaaiabbMfazjabbkgaIbqabaGccqGH9aqpcqGGOaakcqGHsislcqaI % 3aWncqGGUaGlcqaI3aWncqaIZaWmcqGHXcqScqaIWaamcqGGUaGlcq % aI5aqocqaI3aWncqGGPaqkcqGHsisldaqadaqaaiabiodaZiabisda % 0iabiodaZiabgglaXkabiodaZiabicdaWiaaysW7cqqGRbWAcqqGkb % GscaaMe8UaeeyBa0Maee4Ba8MaeeiBaW2aaWbaaSqabeaacqqGTaql % cqqGXaqmaaGccqGGVaWlcqaIYaGmcqGGUaGlcqaIZaWmcqaIWaamcq % aIZaWmcqWGsbGucqWGubavaiaawIcacaGLPaaaaeaacyGGSbaBcqGG % VbWBcqGGNbWzdaWgaaWcbaGaeGymaeJaeGimaadabeaakiabdseaen % aaBaaaleaacqqGebarcqqG5bqEaeqaaOGaeyypa0JaeiikaGIaeyOe % I0IaeGyoaKJaeiOla4IaeGimaaJaeGinaqJaeyySaeRaeGimaaJaei % Ola4IaeGyoaKJaeG4naCJaeiykaKIaeyOeI0YaaeWaaeaacqaIZaWm % cqaIWaamcqaIYaGmcqGHXcqScqaIZaWmcqaIWaamcaaMe8Uaee4AaS % MaeeOsaOKaaGjbVlabb2gaTjabb+gaVjabbYgaSnaaCaaaleqabaGa % eeyla0IaeeymaedaaOGaei4la8IaeGOmaiJaeiOla4IaeG4mamJaeG % imaaJaeG4mamJaemOuaiLaemivaqfacaGLOaGaayzkaaaabaGagiiB % aWMaei4Ba8Maei4zaC2aaSbaaSqaaiabigdaXiabicdaWaqabaGccq % WGebardaWgaaWcbaGaee4uamLaeeyBa0gabeaakiabg2da9iabcIca % OiabgkHiTiabiMda5iabc6caUiabikdaYiabigdaXiabgglaXkabic % daWiabc6caUiabiMda5iabiEda3iabcMcaPiabgkHiTmaabmaabaGa % eG4mamJaeGimaaJaeGimaaJaeyySaeRaeG4mamJaeGimaaJaaGjbVl % abbUgaRjabbQeakjaaysW7cqqGTbqBcqqGVbWBcqqGSbaBdaahaaWc % beqaaiabb2caTiabbgdaXaaakiabc+caViabikdaYiabc6caUiabio % daZiabicdaWiabiodaZiabdkfasjabdsfaubGaayjkaiaawMcaaaqa % aiGbcYgaSjabc+gaVjabcEgaNnaaBaaaleaacqaIXaqmcqaIWaamae % qaaOGaemiraq0aaSbaaSqaaiabboeadjabbwgaLbqabaGccqGH9aqp % cqGGOaakcqGHsislcqaI5aqocqGGUaGlcqaI3aWncqaI0aancqGHXc % qScqaIYaGmcqGGUaGlcqaI4aaocqaI0aancqGGPaqkcqGHsisldaqa % daqaaiabikdaYiabiIda4iabisda0iabgglaXkabiMda5iabigdaXi % aaysW7cqqGRbWAcqqGkbGscaaMe8UaeeyBa0Maee4Ba8MaeeiBaW2a % aWbaaSqabeaacqqGTaqlcqqGXaqmaaGccqGGVaWlcqaIYaGmcqGGUa % GlcqaIZaWmcqaIWaamcqaIZaWmcqWGsbGucqWGubavaiaawIcacaGL % Paaaaaaaaa!0C76!
log10DCe = ( - 9.74 ±2.84) - ( 284 ±91 &nbs\matrix{ {\log _{10} D_{{\rm Yb}} = ( - 7.73 \pm 0.97) - \left( {343 \pm 30\;{\rm kJ}\;{\rm mol}^{{\rm - 1}} /2.303RT} \right)} \cr {\log _{10} D_{{\rm Dy}} = ( - 9.04 \pm 0.97) - \left( {302 \pm 30\;{\rm kJ}\;{\rm mol}^{{\rm - 1}} /2.303RT} \right)} \cr {\log _{10} D_{{\rm Sm}} = ( - 9.21 \pm 0.97) - \left( {300 \pm 30\;{\rm kJ}\;{\rm mol}^{{\rm - 1}} /2.303RT} \right)} \cr {\log _{10} D_{{\rm Ce}} = ( - 9.74 \pm 2.84) - \left( {284 \pm 91\;{\rm kJ}\;{\rm mol}^{{\rm - 1}} /2.303RT} \right)} \cr } . There is no significant influence of ionic radius on diffusion rates; at each temperature the diffusion coefficients for Ce, Sm, Dy, and Yb are indistinguishable from each other within the measurement uncertainty. However, comparison with other diffusion data suggests that there is a strong influence of ionic charge on diffusion rates in garnet, with REE3+ diffusion rates more than two orders of magnitude slower than divalent cation diffusion rates. This implies that the Sm-Nd isotopic chronometer may close at significantly higher temperatures than thermometers based on divalent cation exchange, such as the garnet-biotite thermometer. REE diffusion rates in pyrope are similar to Yb and Dy diffusion rates in diopside at temperatures near the solidus of garnet lherzolite (~1,450 °C at 2.8 GPa), and are an order of magnitude faster than Nd, Ce, and La in high-Ca pyroxene at these conditions. At lower temperatures relevant to the lithospheric mantle and crust, REE diffusion rates in garnet are much faster than in high-Ca pyroxene, and closure temperatures for Nd isotopes in slowly-cooled garnets are ~200 °C lower than in high-Ca pyroxene. 相似文献
We studied trapping of noble-gases by chromite and carbon: two putative carriers of primordial noble gases in meteorites. Nineteen samples were synthesized in a Ne-Ar-Kr-Xe atmosphere at 440 K to 720 K, by the following reactions: Fe,Cr + 4H2O → (Fe,Cr)3O4 + 4H2 (1) or Fe,Cr + 4CO → (Fe,Cr)3O4 + 4C + carbides (2)The reactant metal films were prepared either by vacuum evaporation of alloy or by thermal decomposition of Fe- and Cr-carbonyls. The products—including Fe3O4, Cr2O3, carbides, and unreacted metal—were partially separated by selective solvents, such as HCl, H2SO4?H3PO4, or HClO4. Samples were characterized by XRD, SEM, and atomic absorption; noble gases were measured by mass spectrometry. Surface areas, as measured by the BET method, were 2 to 100 m2/g.All samples are dominated by an adsorbed noble gas component that is largely released upon heating at ?400°C or slight etching. Elemental abundance patterns show that this component is derived from the highest-pressure noble gas reservoir seen by the sample—atmosphere or synthesis vessel—indicating that desorption or exchange rates at room T are slow on the time scale of our experiments (up to 1 year). Adsorptive capacity is reduced by up to 2 orders of magnitude upon light etching with HClO4 (though the surface area actually doubles in this treatment) and, less drastically, by heating. Apparently some active adsorption sites are destroyed by these treatments. A trapped component (typically 30% of the total) is readily detectable only in samples synthesized at partial pressures close to or greater than atmospheric.Noble gas contents roughly obey Henry's Law, but show only slight, if any, correlations with composition, surface area, or adsorption temperature. (Geometric) mean distribution coefficients for bulk samples and HCl-residues are, in 10?3 cc STP/g atm: Xe (100), Kr (15), Ar (3.5), Ne (0.62). Elemental fractionations are large and variable, but are essentially similar for the adsorbed and trapped components, or for chromite and carbon. They bracket the values for the corresponding meteoritic minerals.
Chad has an area of about 1.2 million km2, is located in the centreof the African continent and is not well explored. Results of importance to the local economic geology have been acquired recently, mainly during mineral exploration:
1.
i) all geological formations within Chad territory were reworked/influenced by the Pan-African Orogeny (by the end of the Proterozoic) terminating the crustal evolution of the area with most of the Chad granitoids being formed during this event;
2.
ii) The Precambrian formations are of Proterozoic age and contain volcanosedimentary series with considerable mineral potential (Au,…);
3.
iii) the vast Chad Basin (extending into neighbouring countries) has a complex structure and includes several sub-basins and troughs, whose development started during the break-up of Gondwana; they have been filled by up to 10, 000 m of sediments and petroleum and gas occur within these structures;
4.
iv) well preserved fossil remnants of an Australopithecus have been recently found in Chad; and
5.
v) large reserves of oil and vaste resources of a variety of minerals (Au, ornamental stones, marbles, diatomites, etc.) have been found.
Als Ausgangsgestein des Villacher Granitgneises ist ein spätdifferenzierter, saurer Granit anzusehen, wofür folgende Argumente sprechen:
1.
Hohe Rb-Konzentration, kleines K/Rb-Verhältnis von 110, Rb/Sr-Verhältnis von 12.
2.
Hohe F-Konzentration (1680–2700 ppm) und Ausbildung von Flußspat.
3.
Auftreten von Beryll.
Die Bildungsbedingungen sind wie folgt anzusetzen: die Kristallisation der ursprünglichen granitischen Schmelze erfolge bei einempH2O zwischen 2 und 3 kb (Mindesttiefe der Granitgenese 7 bis 10,5 km). Unter Berücksichtigung des HF-Anteiles der Gasphase ist die Schmelztemperatur mit 620°C anzunehmen. Die Triklinitäten der Alkalifeldspäte (0,61–0,71) sind gering. Der Gesteinskomplex führt ursprünglichen Granat. Die Vergneisung des Granites führt zur Ausbildung von Phengiten, zur Umkristallisation der Plagioklase, zur Bildung von Fleckenperthit und Schachbrettalbit, zum Austausch des Rb zwischen den Alkalifeldspäten und den neu gesproßten Glimmem sowie zur Mobilisierung von F während der Metamorphose. Das Rb–Sr Gesamtgesteinsalter von 409±32 ma sowie das Glimmeralter von 84±3 ma (beide WerteE. Jäger, pers. Mitteilung) legen die Granitgenese als kaledonisch fest bzw. lassen die Metamorphose einer frühen Phase der alpinen Orogenese zuordnen. Die Vergneisung des Granites führte zu diaphthoritischen Erscheinungen in den umgebenden Granatglimmerschiefern. Die frühalpine Metamorphose läßt sich mit einer Temperatur von knapp über 400°C und einem Mindestdruck größer 4 kb abschätzen. 相似文献
The solubility of calcite in H2O was measured at 6–16 kbar, 500–800 °C, using a piston-cylinder apparatus. The solubility was determined by the weight loss of a single crystal and by direct analysis of the quench fluid. Calcite dissolves congruently in the pressure (P) and temperature (T) range of this study. At 10 kbar, calcite solubility increases with increasing temperature from 0.016±0.005 molal at 500 °C to 0.057±0.022 molal at 750 °C. The experiments reveal evidence for hydrous melting of calcite between 750 and 800 °C. Solubilities show only a slight increase with increasing P over the range investigated. Comparison with work at low P demonstrates that the P dependence of calcite solubility is large between 1 and 6 kbar, increasing at 500 °C from 1.8×10–5 molal at 1 kbar to 6.4×10–3 molal at 6 kbar. The experimental results are described by:
where T is in Kelvin andH2O is the density of pure water in g/cm3. The equation is applicable at 1–20 kbar and 400–800 °C, where calcite and H2O stably coexist. Extrapolated thermodynamic data for
indicates that the dominant dissolved carbon species is CO2,aq at all experimental conditions. The results require that equilibrium constant for the reaction:
increases by several orders of magnitude between 1 and 6 kbar, and also rises with isobaric T increase. Published thermodynamic data for aqueous species fail to predict this behavior. The increase in calcite solubility with P and T demonstrates that there is a strong potential for calcite precipitation during cooling and decompression of water-rich metamorphic fluids sourced in the middle to lower crust.Editorial responsibility: T.L. Grove 相似文献
Summary The crystal structure of sigloite, Fe3 [(H2O)3OH] [Al2(PO4)2(OH)2(H2O)2]- 2 H2O, triclinic, a 5.190 (2), b 10.419 (4), c 7.033 (3) Å, 105.00 (3), 111.31(3), 70.87 (3)°, V 330.5 (2) Å3, Z = 1, space group P
, has been refined to anR index of 5.3% using 1713 observed (I > 2.5 1) reflections collected with graphite-monochromated MoK X-rays. Sigloite is isostructural with the laueite-group minerals. Corner-linked [A15] chains (: unspecified ligand) are cross-linked by (PO4) tetrahedra to form a mixed corner-linked tetrahedral-octahedral sheet of composition [A12(PO4)2(OH)2(H2O)2]2-. These sheets are linked by (Fe3+O2(OH, H2O)4) octahedra and two (H2O) groups that participate in a hydrogen-bonding network. Sigloite is the oxidized equivalent of paravauxite, Fe2+(H2O)4[Al2(PO4)2(OH)2(H2O)2]-2 H2O, and detailed comparison of the two structures shows that the oxidation mechanism involves loss of hydrogen from one of the (H2O) groups coordinating the Fe3+, and positional disorder of both the Fe3+ and (OH) and (H2O) ligands.
Siggloit: Der Oxidationsmechanismus in (M
23+ (PO4)2(OH)2(H2O)2]2- Strukturen
Zusammenfassung Die Kristallstruktur von Sigloit, Fe3+ [(H2O)3OH] [Al2(PO4)2(OH)2(H2O)2].2 H2O, triklin, a 5,190 (2), b 10,419 (4), c 7,033 (3) Å, 105,00 (3), 111,31 (3), 70,87 (3)°, V 330,5 (2) Å3,Z = 1, Raumgruppe P
, wurdefür 1713 beobachtete Reflexe (I > 2,5 I), die mit MoKa-Röntgenstrahlung (Graphit-Monochromator) gesammelt wurden, auf einen R-Wert von 5,3% verfeinert. Sigloit ist isotyp mit den Mineralen deer Laueit-Gruppe. Über Ecken verknüpfte [A15]-Ketten (: nicht spezifizierter Ligand) werden über (P04)-Tetraeder zu ebenfalls über Ecken verknüpfte Tetraeder-OktaederSchichten der Zusammensetzung [A12(PO4)2(OH)2(H2O)2]2- verbunden. Diese Schichten werden über (Fe3+O2(OH, H2O)4)-Oktaeder und zwei (H2O)-Gruppen, die amWasserstoffbrücken-Netzwerk beteiligt sind, verbunden. Sigloit ist das oxidierte Analogon zu Paravauxit, Fe2+(H2O)4[A12(PO4)2(OH)2(H2O)2] - 2 H2O; ein detaillierter Vergleich dieser beiden Strukturen zeigt, daß der Oxidationsmechanismus sowohl den Verlust eines Wasserstoffatoms (H2O)-Gruppe, welche ein Fe3+-Atom koordiniert, als auch eine Fehlordnung der Punktlagen von Fe3+ und von den (OH) und (H2O) Liganden bedingt.
