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1.
Calcite was synthesized by four methods, and the luminescence decay-time was measured for nine samples before and after heating
hydrothermally in the temperature range 200–400°C. Decay-time data were collected between room temperature and approximately
15 K. The decay time at room temperature is approximately 50 ms, with little difference between a given calcite before and
after hydrothermal treatment. The decay time at 15 K is always greater than at room temperature as the effect of thermal quenching
diminishes. Differences in decay time before and after heating are more apparent at low temperature owing to this reduction
in thermal quenching. The decay time decreased significantly in two samples, and an increase in decay time was observed in
the remaining seven samples following heating. Among the latter group, the change in decay time was insignificant in three
samples. The results are compared with previous data in which it was shown that the effect of heating is to increase the intensity
of luminescence. 相似文献
2.
Summary The temperature dependence of photoluminescence emission of a natural fluorite has been studied in the wavelength region of
380–500 nm and in the temperature range of 17.5–300 K. The emission spectra of the sample show a broad emission band between
380 and 500 nm for temperatures above 100 K. At 100 K and below, vibronic lines appear on the emission band at approximately
413.3, 418.1, 419.3, 420.2, 423.9 and 427.1 nm. This broad emission band and the vibronic lines in fluorite are usually associated
with phonon-coupled electronic transitions from 4f65d to 4f7 in the Eu2+ ion. Temperature dependences of the peak energy, intensity and full-width at half-maximum of the broad emission band are
discussed, and the behaviour explained in terms of a configurational coordinate model. The excited state vibrational energy
was obtained to be 0.023 ± 0.001 eV and this is lower than the LO phonon energy of 0.062 eV in pure fluorite. The activation
energy of thermal quenching of the photoluminescence intensity was found to be 0.022 ± 0.002 eV. 相似文献
3.
A. Bollhöfer A. Eisenhauer N. Frank D. Pech A. Mangini 《International Journal of Earth Sciences》1996,85(3):577-585
Thorium- and uranium isotopes were measured in a diagenetic manganese nodule from the Peru basin applying alpha- and thermal
ionization mass spectrometry (TIMS). Alpha-counting of 62 samples was carried out with a depth resolution of 0.4 mm to gain
a high-resolution230Thexcess profile. In addition, 17 samples were measured with TIMS to obtain precise isotope concentrations and isotope ratios. We
got values of 0.06–0.59 ppb (230Th), 0.43–1.40 ppm (232Th), 0.09–0.49 ppb (234U) and 1.66–8.24 ppm (238U). The uranium activity ratio in the uppermost samples (1–6 mm) and in two further sections in the nodule at 12.5±1.0 mm
and 27.3–33.5 mm comes close to the present ocean water value of 1.144±0.004. In two other sections of the nodule, this ratio
is significantly higher, probably reflecting incorporation of diagenetic uranium. The upper 25 mm section of the Mn nodule
shows a relatively smooth exponential decrease in the230Thexcess concentration (TIMS). The slope of the best fit yields a growth rate of 110 mm/Ma up to 24.5 mm depth. The section from 25
to 30.3 mm depth shows constant230Thexcess concentrations probably due to growth rates even faster than those in the top section of the nodule. From 33 to 50 mm depth,
the growth rate is approximately 60 mm/Ma. Two layers in the nodule with distinct laminations (11–15 and 28–33 mm depth) probably
formed during the transition from isotopic stage 8 to 7 and in stage 5e, respectively. The Mn/Fe ratio shows higher values
during interglacials 5 and 7, and lower ones during glacials 4 and 6. A comparison of our data with data from adjacent sediment
cores suggests (a) a variable supply of hydrothermal Mn to sediments and Mn nodules of the Peru basin or (b) suboxic conditions
at the water sediment interface during periods with lower Mn/Fe ratios. 相似文献
4.
Environmental isotopic and hydrochemical study of groundwater in the Ejina Basin,northwest China 总被引:5,自引:0,他引:5
The study investigates the groundwater evolution and its residence time in the Ejina Basin, northwest China according to isotope
and hydrochemical analyses results. The groundwater chemistry is mainly controlled by the dissolution of halite, Glauber’s
salt, gypsum, dolomite and calcite, also influenced by other processes such as evaporation, ion exchange, and deposition.
Based on tritium content in atmospheric precipitation and by adopting a model with exponential time distribution function,
the mean residence time of the unconfined aquifer groundwater with fairly high tritium activities (21–49 TU) is evaluated.
The results show that these groundwaters have low residence time (5–120 years) and are renewable. In contrast, the deep confined
groundwaters are tritium-free and radiocarbon values range from 18.3 to 26.7 pmc. According to the most commonly used 14C correction models, the radiocarbon groundwater ages were calculated which yield ages of approximately 4,087–9,364 years
BP. Isotopic signatures indicate formation of deep confined groundwaters in a colder and wetter climate during the late Pleistocene
and Holocene. It is suggested that long-term, rational water usage guide should be set up for the Heihe River Basin as a whole
to permit a considerable discharge to the Ejina Basin. 相似文献
5.
Lili Xu Jörg Renner Marco Herwegh Brian Evans 《Contributions to Mineralogy and Petrology》2009,157(3):339-358
We extended a previous study on the influence of Mg solute impurity on diffusion creep in calcite to include deformation under
a broader range of stress conditions and over a wider range of Mg contents. Synthetic marbles were produced by hot isostatic
pressing (HIP) mixtures of calcite and dolomite powders for different intervals (2–30 h) at 850°C and 300 MPa confining pressure.
The HIP treatment resulted in high-magnesian calcite aggregates with Mg content ranging from 0.5 to 17 mol%. Both back-scattered
electron images and chemical analysis suggested that the dolomite phase was completely dissolved, and that Mg distribution
was homogeneous throughout the samples at the scale of about two micrometers. The grain size after HIP varied from 8 to 31 μm,
increased with time at temperature, and decreased with increasing Mg content (>3.0 mol%). Grain size and time were consistent
with a normal grain growth equation, with exponents from 2.4 to 4.7, for samples containing 0.5–17.0 mol% Mg, respectively.
We deformed samples after HIP at the same confining pressure with differential stresses between 20 and 200 MPa using either
constant strain rate or stepping intervals of loading at constant stresses in a Paterson gas-medium deformation apparatus.
The deformation tests took place at between 700 and 800°C and at strain rates between 10−6 and 10−3 s−1. After deformation to strains of about 25%, a bimodal distribution of large protoblasts and small recrystallized neoblasts
coexisted in some samples loaded at higher stresses. The deformation data indicated a transition in mechanism from diffusion
creep to dislocation creep. At stresses below 40 MPa, the strength was directly proportional to grain size and decreased with
increasing Mg content due to the reductions in grain size. At about 40 MPa, the sensitivity of log strain rate to log stress,
(n), became greater than 1 and eventually exceeded 3 for stresses above 80 MPa. At a given strain rate and temperature, the
stress at which that transition occurred was larger for samples with higher Mg content and smaller grain size. At given strain
rates, constant temperature, and fixed grain size, the strength of calcite in the dislocation creep regime increased with
solute content, while the strength in the diffusion creep regime was independent of Mg content. The results suggest that chemical
composition will be an important element to consider when solid substitution can occur during natural deformation. 相似文献
6.
S. Carbonin F. Martignago G. Menegazzo A. Dal Negro 《Physics and Chemistry of Minerals》2002,29(8):503-514
Two MgAl2O4 stoichiometric spinel crystals, one natural and one synthetic, were heated from 25 to 950 °C and studied in situ by single-crystal
X-ray diffraction. The natural crystal, quenched from 850 °C, was further heated and cooled. Thermal expansion was characterized,
and cation partitioning at the various temperatures was determined according to a model purposely constructed for high-temperature
bond lengths. It was found that the structural evolution of the samples with temperature depended on order–disorder at room
temperature. At the temperatures lower than the beginning of cation exchange, thermal expansion was completely reversible
and the oxygen coordinate remained stable in spite of varying temperatures. At the temperature at which cation exchange starts,
the disordered samples first tend to order and then to disorder at higher temperatures, at variance with the ordered sample,
which tends to disorder steadily. In general, the evolution of the spinel structural state on cooling and heating over the
same temperature range and the same time intervals does not follow the same path. In particular, in the 600–950 °C range,
only partially reversible order–disorder processes occurred in the time span used for the experiments.
Received: 16 July 2001 / Accepted: 8 January 2002 相似文献
7.
Rare-element pegmatites in the Voron’i tundras, Kola Peninsula, Russia, contain late abundant Rb mineralization. Individual
Rb minerals are Rb-dominant feldspars and micas that form continuous solid solution series with K analoques. The feldspars
contain from 17 to 86 mol % RbAlSi3O8 (5.5–25 wt % Rb2O) and 1–5 mol % CsAlSi3O8, and the muscovite contains 2.6–9.4 wt % Rb2O. The Li micas are members of the lepidolite-polylithionite series and their Rb-dominant analogues. They form a continuous
series of solid solutions with the Rb concentrations varying from 0.09 to 0.54 apfu., K concentrations varying from 0.82 to
0.33 apfu, and Cs concentrations varying from 0.02 to 0.18 apfu The maximum Rb2O concentration in the newly found mineral voloshinite, an Rb analogue of lepidolite, is 12.2 wt %. The Rb-rich feldspars
and micas sometimes crystallized directly or were formed via cation exchange with the young fluid. The Rb minerals are spatially
and genetically closely associated with pollucite. It is supposed that initially Rb was contained in a high-temperature pollucite
solid solution and was released from it at decreasing temperature as a result of a reaction with the aqueous fluid and notably
enriched the latter. It is shown that Rb mineralization is generally typical of pollucite-bearing pegmatites. 相似文献
8.
Colin M. Graham John W. Valley John M. Eiler Hideki Wada 《Contributions to Mineralogy and Petrology》1998,132(4):371-389
Using a recently developed ion microprobe technique, a detailed oxygen isotope map of calcite grains in a coarse-grained
marble has been constructed, supported by trace element (Mn, Sr, Fe) analysis and cathodoluminescence (CL) imaging, in order
to constrain scales of oxygen isotope equilibrium, timescales and mechanisms of metamorphic fluid infiltration, and fluid
sources and pathways. Results are compared with a previous study of this sample (Wada 1988) carried out using a cryo-microtome
technique and conventional oxygen isotope analysis. The marble, from the high temperature/low pressure Hida metamorphic belt
in north-central Japan, underwent granulite facies followed by amphibolite facies metamorphic events, the latter associated
with regional granite intrusion. The CL imaging indicates two types of calcite, a yellow luminescing (YLC) and a purple luminescing
(PLC) variety. The YLC, which occupies grain boundaries, fractures, replacement patches, and most of the abundant deformation
twin lamellae, post-dates the dominant PLC calcite and maps out fluid pathways. Systematic relationships were established
between oxygen isotope and trace element composition, calcite type and texture, based on 74 18O/16O and 17 trace element analyses with 20–30 μ m spatial resolution. The YLC is enriched in Mn and Fe, and depleted in 18O and Sr compared to PLC, and is much more 18O depleted than is indicated from conventional analyses. Results are interpreted to indicate infiltration of 18O-depleted (metamorphic or magmatic) fluid (initial δ18O = 9‰–10.5‰) along grain boundaries, fractures and deformation twin lamellae, depleting calcite grains in Sr and enriching
them in Mn and Fe. The sample is characterised by gross isotopic and elemental disequilibrium, with important implications
for the application of chromatographic theory to constrain fluid fluxes in metacarbonate rocks.
Areas of PLC unaffected by “short-circuiting” fluid pathways contain oxygen diffusion profiles of ∼10‰/∼200 μm in grain boundary
regions or adjacent to fractures/patches. When correction is made for estimated grain boundary/fracture and profile orientation
in 3D, profiles are indistinguishable within error. Modelling of these profiles gives consistent estimates of Dt (where D is the diffusion coefficient and t is time) of ∼0.8 × 10−8 m2, from which, using experimental data for oxygen diffusion in calcite, timescales of fluid transport along grain boundaries
at amphibolite facies temperatures of ∼103 to ∼104 years are obtained. These short timescales, which are much shorter than plausible durations of metamorphism, imply that
rock permeabilities may be transiently much higher during fluid flow than those calculated from time integrated fluid fluxes
or predicted from laboratory measurements. The preservation of 18O/16O profiles requires either rapid cooling rates (∼100–600 °C/million years), or, more plausibly, loss of grain boundary fluid
such that a dry cooling history followed the transient passage of fluid. The δ18O/trace element correlations are also consistent with volume diffusion-controlled transport in the PLC. Fluid transport and
element exchange occurred by two inter-related mechanisms on short timescales and on different lengthscales – long-distance
flow along cracks, grain boundaries and twin lamellae coupled to ∼200 μm-scale volume diffusion of oxygen.
Received: 8 December 1997 / Accepted: 18 May 1998 相似文献
9.
Aierken Sidike Keyoumu Niyazi Heng-Jiang Zhu K. Atobe N. Yamashita 《Physics and Chemistry of Minerals》2009,36(3):119-126
The photoluminescence (PL) spectra, excitation spectra, and PL decay curves of natural, heat-treated, and γ-ray-irradiated
thenardites from Ai-Ding Salt Lake, Xinjiang, China, were studied. The natural thenardite under 300 nm excitation showed milk-white
luminescence, and the PL spectrum consisted of an extremely broad band with a peak located at approximately 509 nm, spreading
over a wide range of UV and visible wavelengths. The excitation spectra, obtained by monitoring the luminescence at 530 nm,
consisted of a broad band with a peak located at approximately 235 nm and a flat band spreading over a wide range of UV and
visible wavelengths. The PL decay curve of natural thenardite consisted of a fast-decay component with a lifetime of less
than 0.1 μs and a slow-decay component with a half-decay time of approximately 0.4 s. The heat treatment of thenardite at
900°C for 20 min reduced the luminescence efficiency to 1/100. The γ-ray irradiation of thenardite reduced the luminescence
efficiency to approximately half. 相似文献
10.
The Youjiang basin, which flanks the southwest edge of the Yangtze craton in South China, contains many Carlin-type gold deposits and abundant paleo-oil reservoirs. The gold deposits and paleo-oil reservoirs are restricted to the same tectonic units, commonly at the basinal margins and within the intrabasinal isolated platforms and/or bioherms. The gold deposits are hosted by Permian to Triassic carbonate and siliciclastic rocks that typically contain high contents of organic carbon. Paragenetic relationships indicate that most of the deposits exhibit an early stage of barren quartz ± pyrite (stage I), a main stage of auriferous quartz + arsenian pyrite + arsenopyrite + marcasite (stage II), and a late stage of quartz + calcite + realgar ± orpiment ± native arsenic ± stibnite ± cinnabar ± dolomite (stage III). Bitumen in the gold deposits is commonly present as a migrated hydrocarbon product in mineralized host rocks, particularly close to high grade ores, but is absent in barren sedimentary rocks. Bitumen dispersed in the mineralized rocks is closely associated and/or intergrown with the main stage jasperoidal quartz, arsenian pyrite, and arsenopyrite. Bitumen occurring in hydrothermal veins and veinlets is paragenetically associated with stages II and III mineral assemblages. These observations suggest an intimate relationship between bitumen precipitation and gold mineralization. In the paleo-petroleum reservoirs that typically occur in Permian reef limestones, bitumen is most commonly observed in open spaces, either alone or associated with calcite. Where bitumen occurs with calcite, it is typically concentrated along pore/vein centers as well as along the wall of pores and fractures, indicating approximately coeval precipitation. In the gold deposits, aqueous fluid inclusions are dominant in the early stage barren quartz veins (stage I), with a homogenization temperature range typically of 230°C to 270°C and a salinity range of 2.6 to 7.2 wt% NaCl eq. Fluid inclusions in the main and late-stage quartz and calcite are dominated by aqueous inclusions as well as hydrocarbon- and CO2-rich inclusions. The presence of abundant hydrocarbon fluid inclusions in the gold deposits provides evidence that at least during main periods of the hydrothermal activity responsible for gold mineralization, the ore fluids consisted of an aqueous solution and an immiscible hydrocarbon phase. Aqueous inclusions in the main stage quartz associated with gold mineralization (stage II) typically have a homogenization temperature range of 200–230°C and a modal salinity around 5.3 wt% NaCl eq. Homogenization temperatures and salinities of aqueous inclusions in the late-stage drusy quartz and calcite (stage III) typically range from 120°C to 160°C and from 2.0 to 5.6 wt% NaCl eq., respectively. In the paleo-oil reservoirs, aqueous fluid inclusions with an average homogenization temperature of 80°C are dominant in early diagenetic calcite. Fluid inclusions in late diagenetic pore- and fissure-filling calcite associated with bitumen are dominated by liquid C2H6, vapor CH4, CH4–H2O, and aqueous inclusions, with a typical homogenization temperature range of 90°C to 180°C and a salinity range of 2–8 wt% NaCl eq. It is suggested that the hydrocarbons may have been trapped at relatively low temperatures, while the formation of gold deposits could have occurred under a wider and higher range of temperatures. The timing of gold mineralization in the Youjiang basin is still in dispute and a wide range of ages has been reported for individual deposits. Among the limited isotopic data, the Rb–Sr date of 206 ± 12 Ma for Au-bearing hydrothermal sericite at Jinya as well as the Re–Os date of 193 ± 13 Ma on auriferous arsenian pyrite and 40Ar/39Ar date of 194.6 ± 2 Ma on vein-filling sericite at Lannigou may provide the most reliable age constraints on gold mineralization. This age range is comparable with the estimated petroleum charging age range of 238–185 Ma and the Sm–Nd date of 182 ± 21 Ma for the pore- and fissure-filling calcite associated with bitumen at the Shitouzhai paleo-oil reservoir, corresponding to the late Indosinian to early Yanshanian orogenies in South China. The close association of Carlin-type gold deposits and paleo-oil reservoirs, the paragenetic coexistence of bitumens with ore-stage minerals, the presence of abundant hydrocarbons in the ore fluids, and the temporal coincidence of gold mineralization and hydrocarbon accumulation all support a coeval model in which the gold originated, migrated, and precipitated along with the hydrocarbons in an immiscible, gold- and hydrocarbon-bearing, basinal fluid system. 相似文献
11.
Lin-gun Liu C.-C. Lin Y. J. Yung T. P. Mernagh T. Irifune 《Physics and Chemistry of Minerals》2009,36(3):143-149
K-lingunite is a high-pressure modification of K-feldspar that possesses the tetragonal hollandite structure. Variations of
the Raman spectra of K-lingunite were studied up to ~31.5 GPa at room temperature, and in the range 79–823 K at atmospheric
pressure. The Raman frequencies of all bands were observed to increase with increasing pressure, and decrease with increasing
temperature for K-lingunite. This behavior is in line with those observed for most of other materials. New sharp Raman bands
appear at pressures greater than 13–15 GPa, suggesting a phase transition in K-lingunite with increasing pressure. The transition
is reversible when pressure was released. The appearance of these new Raman bands may correspond to the phase transition revealed
earlier at around 20 GPa by X-ray diffraction studies. Instead of transforming back to its stable minerals, such as orthoclase,
microcline or sanidine, K-lingunite became amorphous in the temperature range 803–823 K at atmospheric pressure. 相似文献
12.
The Middle Miocene Tobe hornfels in the Sanbagawa metamorphic belt, western Shikoku, southwest Japan, is characterized by
an abnormally steep metamorphic gradient compared with other hornfelses associated with intrusive bodies. The basic hornfels,
originally Sanbagawa greenschist rocks, is divided into the following three metamorphic zones: plagioclase, hornblende, and
orthopyroxene. The plagioclase zone is defined by the appearance of calcic plagioclase, the hornblende zone by the assemblage
of hornblende+calcic plagioclase+quartz, and the orthopyroxene zone is characterized by the assemblage of orthopyroxene +
clinopyroxene + plagioclase + quartz. Calcic amphibole compositions change from actinolite to hornblende as a result of the
continuous reactions during prograde metamorphism. Petrographical and thermometric studies indicate a metamorphic temperature
range of 300–475°C for the plagioclase zone, 475–680°C for the hornblende zone, and 680–730°C for the orthopyroxene zone.
The temperature gradient based on petrological studies is approximately 5°C/m, which is unusually high. Geological and petrological
studies demonstrate that the hornfelses were formed by the focusing of high-temperature fluids through zones of relatively
high fracture permeability. The steep thermal gradient in the Tobe hornfels body is consistent with a large fluid flux, greater
than 8.3 × 10–7 m3 m–2S–1, over the relatively short duration of metamorphism, approximately 100 years.
Received: 10 October 1995 / Accepted: 28 May 1996 相似文献
13.
Badia Chulli Aysen Davraz Jalila Makni Mourad Bedir Hamed Ben Dhia 《Environmental Earth Sciences》2012,66(1):1-16
The Sfax Basin in eastern Tunisia is bounded to the east by the Mediterranean Sea. Thermal waters of the Sfax area have measured
temperatures of 23–36°C, and electrical conductivities of 3,200 and 14,980 μS/cm. Most of the thermal waters are characterized
as Na–Cl type although there are a few Na–SO4–Cl waters. They issue from Miocene units which are made up sands and sandstones interbedded with clay. The Quaternary sediments
cap the system. The heat source is high geothermal gradient which are determined downhole temperature measurements caused
by graben tectonics of the area. The results of mineral equilibrium modeling indicate that the thermal waters of the Sfax
Basin are undersaturated with respect to gypsum, anhydrite and fluorite, oversaturated with respect to kaolinite, dolomite,
calcite, microcline, quartz, chalcedony, and muscovite. Assessments from various chemical geothermometers, Na–K–Mg ternary
and mineral equilibrium diagrams suggest that the reservoir temperature of the Sfax area can reach up to 120°C. According
to δ18O and δ2H values, all thermal and cold groundwater is of meteoric origin. 相似文献
14.
It is proved that blue luminescence from benitoite is connected with intrinsic luminescence centers, namely isolated TiO6 octahedra. The metastable level 3T1u is the emitting level at low temperatures with a long decay time of 1.1 ms. At higher temperatures an energy level with higher radiation probability must be involved in the emission process, and this level is situated at 0.06 eV higher than the lowest level. These two levels may be connected with 3T1u level splitting or with closely spaced 3T1u and 3T2u levels. Decay time shortening and thermal quenching are connected with nonradiative decay within the TiO6 luminescence center, while energy migration does not take place at least up to room temperature. 相似文献
15.
Thirty spodumene samples of distinct paragenetic types (primary magmatic, secondary after petalite and hydrothermal) from variety of granitic pegmatites were characterized by electron microprobe, polarized FTIR spectroscopy and Mössbauer spectroscopy. The FTIR spectra of OH (weak sharp pleochroic bands at 3,425, 3,410, 3,395 cm−1 and in the 3,500–3,470 spectral region) are strongly polarized with maximum absorption parallel to nγ. The majority of OH dipoles are presumably generated by a partial replacement of O2 oxygen atoms with an orientation pointing above the Li vacancy site. The separation of the bands probably resulted from a replacement of the coordinating Al by Fe and Si by Al. Homogeneous spodumene mostly close to its ideal formula LiAlSi2O6 shows Fe (0.00–0.10 apfu as Fe3+; Fe3+ >> Fe2+) and Na (0.00–0.04 apfu) as the only minor cations and Fe3+Al−1 substitution up to 10 mol% of the LiFe3+Si2O6 component. Hydrogen concentrations (from 0.1 up to <5 ppm H2O by weight) vary as a function of genetic type with the highest amounts in high-temperature magmatic spodumene. Differences among particular genetic types of spodumene are related to maximum solubility of OH in spodumene structure at given P–T conditions and at actual chemical composition of spodumene. OH defect concentrations in spodumene follow a trend, LT/LP pyroxenes containing lower hydrogen contents compared to HT/HP ones. The hydrogen contents in particular genetic types of spodumene and their decrease with decreasing T and P are consistent with petrologic models of the pegmatite (sub)types formations. 相似文献
16.
D. P. Zarubin 《Physics and Chemistry of Minerals》2000,27(8):590-597
Simple model calculations show that the reversible temperature effects reported for broad OH-stretching bands in infrared
spectra of silica, aluminosilicate, and similar glasses can be explained, in essentials, by homogeneous thermal broadening
of the ν(OH) envelope constituents and a decrease in intensity with increasing temperature taking place uniformly across the
band. This means that these effects are reasonably consistent with the temperature behaviour of narrow ν(OH) bands of crystalline
OH-bearing minerals. These findings leave little room for the previously agreed interpretation in terms of a change in hydrogen-bonding
strength, although the dependence of integrated intensity on temperature still remains to be understood.
Received: 16 April 1999 / Accepted: 4 April 2000 相似文献
17.
In situ unpolarized and polarized Fourier transform infrared spectra of a natural orthopyroxene at varying temperatures were
obtained using a heating stage attached on an Infrared microscope. The three main bands (3,595, 3,520 and 3,410 cm−1) at room temperature are ascribed to OH fundamental stretching bands. With increasing temperature from room temperature to
500 °C, the 3,595 cm−1 band shifts 20 cm−1 to lower frequency. The total integral absorbance decreases with increasing temperature. These changes are reversible. Excluding
the influences of dehydration, proton migration, thermal expansion, and changes in OH dipole direction, the change of integral
absorbance with temperature reflects the temperature dependence of absorption coefficient due to the anharmonicity of OH vibration.
Based on the integral absorption coefficient at room temperature (14.84 ppm−1 cm−2) from Bell et al. (Am Mineral 80:463–474, 1995), the integral absorption coefficients at other temperatures are calculated. The variation of integral absorption coefficient
between room temperature and 500 °C obtained in this study is about 18.5 % and may be greater at higher temperature according
to the proposed linear relationship. 相似文献
18.
R. R. Gainov A. V. Dooglav I. N. Pen’kov I. R. Mukhamedshin A. V. Savinkov N. N. Mozgova 《Physics and Chemistry of Minerals》2008,35(1):37-48
Electronic and magnetic properties of tennantite subfamily of tetrahedrite-group minerals have been studied by copper nuclear
quadrupole resonance (NQR), nuclear magnetic resonance (NMR) and SQUID magnetometry methods. The temperature dependences of
copper NQR frequencies and line-width, nuclear spin-lattice relaxation rate T
1−1 and nuclear spin-echo decay rate T
2−1 in tennantite samples in the temperature range 4.2–210 K is evidence of the presence of field fluctuations caused by electronic
spins hopping between copper CuS3 positions via S2 bridging atom. The analysis of copper NQR data at low temperatures points to the magnetic phase transition near 65 K. The
magnetic susceptibility in the range 2–300 K shows a Curie–Weiss behavior, which is mainly determined by Fe2+ paramagnetic substituting ions. 相似文献
19.
Diffusion of dissolved SiO2 in H2O at 1 GPa, with implications for mass transport in the crust and upper mantle 总被引:4,自引:0,他引:4
Cation diffusion rates at 690 ± 30 °C have been calculated by inverse modelling of observed manganese (Mn) zonation profiles
in 40 garnets from two kyanite-bearing metapelite samples from the High Himalayan Crystalline Series, Zanskar, northwest India.
Knowledge of the initial growth profile of Mn in garnet is a pre-requisite for this technique. Following previous workers
we model Mn partitioning into growing garnet in terms of a Rayleigh fractionation process, and demonstrate that the Mngarnet:whole rock partition coefficient is 60–100. Three-dimensional zonation profiles were obtained by successively grinding and polishing
∼1 cm slabs of each sample at 0.1–0.2 mm intervals and analysing the garnets at each stage, thus ensuring that core sections
were measured. The diffusion model assumes that garnet has a spherical geometry and behaves as a closed system, and simulates
diffusive modification of the hypothetical Mn Rayleigh growth profile for each garnet. The derived measure of the time-integrated
diffusion history for each garnet is then combined with radiometric and field-relation constraints for the duration of the
Himalayan metamorphic event to calculate cation diffusion rates. The average cation interdiffusion rate calculated for garnets
in the two samples examined is (6 ± 3.2) × 10−23 m2s−1. This interdiffusion rate pertains to a temperature of 690 ± 30 °C, which is 0.97 × T
PEAK, the peak temperature conditions experienced by the samples estimated using standard thermobarometric techniques. Garnet
compositions are Py2–17Alm65–77Gro6–16Sp1–17. These new diffusion data are consistent with, and more precise than, existing high-temperature (>1000 °C) experimentally
determined diffusion data, although some uncertainties remain difficult to constrain. Qualitative comparison between diffusively
modified Mn growth profiles in garnets from the Scottish Dalradian and the Himalayan garnets suggests that the duration of
metamorphism affecting the Dalradian garnets was 10–20 times longer than that endured by the Himalayan garnets.
Received: 5 June 1996 / Accepted: 29 January 1997 相似文献
20.
Summary Garnet occurs as a significant mineral constituent of felsic garnet-biotite granite in the southern edge of the Třebíč pluton.
Two textural groups of garnet were recognized on the basis of their shape and relationship to biotite. Group I garnets are
1.5–2.5 mm, euhedral grains which have no reaction relationship with biotite. They are zoned having high XMn at the rims and are considered as magmatic. Group II garnets form grain aggregates up to 2.5 cm in size, with anhedral shape
of individual grains. The individual garnet II grains are usually rimmed by biotite and have no compositional zoning. The
core of group I garnets and group II garnets contains 67–80 mol% of almandine, 5–19 mol% of pyrope, 7–17 mol% of spessartine
and 2–4 mol% of grossular. Biotite occurs in two generations; both are magnesian siderophyllites with Fe/(Fe + Mg) = 0.50–0.69.
The matrix biotite in granites (biotite I) has high Ti content (0.09–0.31 apfu) and Fe/(Fe + Mg) ratio between 0.50 and 0.59.
Biotite II forms reaction rims around garnet, is poor in Ti (0.00–0.06 apfu) and has a Fe/(Fe + Mg) ratio between 0.61 and
0.69. The textural relationship between biotite and garnet indicates that garnet reacted with granitic melt to form Ti-poor
biotite and a new granitic melt, depleted in Ti and Mg and enriched in Fe and Al. In contrast to the host durbachites (hornblende-biotite
melagranites), which originated by mixing of crustal melts and upper mantle melts, the origin of garnet-bearing granites is
related to partial melting of the aluminium-rich metamorphic series of the Moldanubian Zone. 相似文献