Colorless Quartz Research Articles

Fluid origin and evolution of the Taolin Pb-Zn deposit in northeastern Hunan Province, South China: Insights from fluid inclusions and H-O-He-Ar isotopes

Situated in northeastern Hunan Province, the vein-type Pb-Zn orebodies at Taolin are mainly hosted in NE-/NEE-trending faults between Dayunshan-Mufushan pluton and Neoproterozoic metasedimentary rocks of the Lengjiaxi Group. Hydrothermal mineralization can be divided into five stages: (1) coarse-grained quartz stage, (2) quartz-fluorite-base metal stage, (3) quartz-barite-fluorite-base metal stage, (4) pale pink and colorless quartz stage, and (5) fine-grained quartz stage. In this research, fluid inclusions as well as stable (H-O) and noble gas (He-Ar) isotope compositions were performed to uncover the nature, origin, and evolution of the ore-forming fluids, ore precipitation mechanisms, and mineralization process of the Taolin deposit. Four types of fluid inclusions, i.e., liquid-rich two-phase inclusions (LV-type), pure liquid phase inclusions (PL-type), vapor-rich two-phase inclusions (VL-type), and pure vapor phase inclusions (PV-type), were distinguished in sphalerite, quartz, and fluorite. Microthermometric analysis of fluid inclusion assemblages in sphalerite, quartz, and fluorite from different stages indicates that from the Stage 1 to Stage 5, the homogenization temperatures vary between 168 and 211 °C, between 151 and 198 °C, between 131 and 180 °C, between 132 and 164 °C, and between 118 and 138 °C, respectively, whereas the fluid salinities vary from 12.4 to 16.9 wt% NaCl equivalent, from 9.7 to 14.6 wt% NaCl equivalent, from 5.6 to 10.3 wt% NaCl equivalent, from 3.6 to 9.7 wt% NaCl equivalent, and from 0.9 to 3.8 wt% NaCl equivalent, respectively. The H-O isotope data of quartz and the He-Ar isotopic compositions of sulfide crystals suggest that the ore-forming fluids were a mixture of crust-derived magmatic hydrothermal fluid and meteoric water. Fluid mixing and cooling were likely the crucial mechanisms for ore precipitation.

Study on the visible-light absorption of quartz with different valence states of iron

Synthetic colorless quartz with ion-implanted iron is compared with natural citrine quartz containing iron to study their coloring mechanisms after heating in different atmospheres.

Thermoluminescence properties and new insights on the UV-vis absorption features of colorless quartz after γ-ray irradiation.

In this paper, we present the results of research on the thermoluminescence (TL) and optical absorption (OA) properties of colorless natural quartz (including natural quartz samples, sodium ion (Na+) rich samples (by diffusion), and alkali metal (M+) ion poor samples (by sweep)). In detail, the relationship between the TL glow peaks and the emission wavelength was determined. The dynamics parameters (E T, s, τ) have been computed for all TL peaks on the glow curve. The recombination mechanism electron-hole with the participation of the region energy has been determined for all electron traps in the temperature range of 50-430 °C through thermally stimulated conductivity measurement (TSC). Nonlinearity and approaching signal saturation are observed at doses above 22 Gy for the electron trap at 110 °C, above 45 Gy for the electron trap at 238 °C, and 80 Gy for the electron traps at 325 °C and 375 °C. The role of irradiation and heat treatment in the formation of absorption centers as well as the relationship of these centers to electronic traps have been also investigated in detail. The role of M+ ions and hydrogen ions (H+) for the absorption bands in the UV-vis region has been discussed. The results of the combination of the TL measurement and monochromatic light absorption according to temperature show that the TL process occurs concurrently with the reduction of the absorbent center produced in the irradiation process.

Distinctive characteristics of Cheniah river sand from Dungun, Terengganu Malaysia

Mineral ilmenite sand depositin the Hulu Dungun, Terengganu, Malaysia, has prompted a huge interest in their viability as a new resource survey of titanium dioxide feedstock in Malaysia. In accordance with this necessity, this study is executed to conduct mineral characterisation onthe ilmenite sand (IS) located at the catchment area, Cheniah River, Kelip Hill, Hulu Dungun, Malaysia. Characterization of raw ilmenite sand was done by X-Ray Fluorescence (XRF) for exploring elements in the sample. Digital microscopy (DM) for optical imaging purpose with polarizing filterand Scanning Electron Microscope (SEM) analyses were developed for surface morphological studies. As determined through this data research, chemical analysis reveals that IS has the highest amount of 44.0% TiO2, and come after with 37.8% Fe2O3, 12.0% SiO2 and other impurity elements such as Mn, V, Cr and Mg. DM images has the same point of view regarding to the mineral constituents from XRF data wherein majority of the IS grains display black dark to steel grey colour as the ilmenite and few of colourless quartz. Meanwhile, the surface morphology from both analyses, DM and SEM can be concluded that IS has heterogenous surface. Most of the IS grains have angular shape with moderate sphericity and few subrounded and high sphericity. Nearly all of the IS are found to be associated with iron oxide as displayed through Backscattered image (BSE) from SEM-EDX analysis. This characterization study's data and information assist in the ilmenite sanddiscovery and createsa design of a viable treatment procedure which will be developed in future workfor the localmineral exploitation.

Absorption spectra and crystal chemistry of quartz implanted with cobalt ions

Background. High-dose implantation of cobalt ions into the crystal structure of natural colourless quartz was carried out. Samples of crystal plates of rock crystal from the Svetlinskoye deposit in the South Urals plane-parallel were studied. All samples were crystallographically oriented perpendicular to the symmetry axis of the third order. Cobalt implantation into quartz was carried out using an ILU-3 ion-beam accelerator along the С axis of symmetry.Aim. To determine the ranges of thermal annealing for a controlled change in the sample colour and to establish the crystal-chemical features of the changes occurring in quartz matrix due to ionbeam modification of mineral properties.Materials and methods. Implantation modes included: room temperature, residual vacuum 10–5 torr, radiation dose from 1.0×1017 to 1.5×1017 ion/cm2 at a constant ion current density of 10 μA/cm2. Post-implantation heat treatment was carried out in three stages. The control of crystallochemical changes was carried out using a highly sensitive spectrophotometer with a wide range of wavelengths.Results. It was found that the revealed absorption bands are associated with electronic transitions in cobalt ions (Со2+ and Со 3+) coordinated in the crystal matrix of implanted and heat-treated rock crystal. The formation of an independent ultradispersed spinel phase in the irradiated quartz matrix was confirmed. The newly formed phase belongs to a partially reversed cobalt spinel.Conclusions. Taking into account the quantum-optical properties of cobalt spinel (laser shutters), the method of ion-beam modification of mineral crystal structures, quartz in particular, is highly promising in terms of creating new composite materials based on natural and artificial mineral raw materials.

Potential development of green and purple colors in colorless natural quartz from geodes in rhyodacites, Serra Geral Group, Brazil

Abstract Colorless quartz can develop a green color when submitted to gamma irradiation and its development is related to the presence of molecular water and hydroxyl groups in the quartz crystalline structure. In the present study, colorless quartz crystals hosted in geodes within rhyodacites of Serra Geral Group, Southern Brazil, were selected to test the potential development of green color. The samples were analyzed by infrared (IR) and thermogravimetric (TGA) techniques, in addition to the Amethyst Factor (fa) method. All samples showed an absorption bands in the IR, indicating possible development of a green or purple color, and fa analysis indicated the samples would develop a green color. All samples became colored after irradiation, presenting color zoning: from colorless to grayish-green, and from grayish-green to slightly purplish. Some samples showed a greenish colored zone and developed an amethyst phantom crystal in its apical portion. In addition, a high content of water in samples that remained colorless after irradiation was detected. It is here interpreted that water concentration varied during quartz crystallization, enabling the development of the green color, and that the excess of water can inhibit the development of radiation-induced color in colorless natural quartz crystals.

Mineralisation of amethyst-bearing geodes in Ametista do Sul (Brazil) from low-temperature sedimentary brines: evidence from monophase liquid inclusions and stable isotopes

Fluid inclusion studies in combination with hydrogen, oxygen and sulphur isotope data provide novel insights into the genesis of giant amethyst-bearing geodes in Early Cretaceous Parana continental flood basalts at Amestita do Sul, Brazil. Monophase liquid inclusions in colourless quartz, amethyst, calcite, barite and gypsum were analysed by microthermometry after stimulating bubble nucleation using single femtosecond laser pulses. The salinity of the fluid inclusions was determined from ice-melting temperatures and a combination of prograde and retrograde homogenisation temperatures via the density maximum of the aqueous solutions. Four mineralisation stages are distinguished. In stage I, celadonite, chalcedony and pyrite formed under reducing conditions in a thermally stable environment. Low δ34SV-CDT values of pyrite (−25 to −32 ‰) suggest biogenic sulphate reduction by organotrophic bacteria. During the subsequent stages II (amethyst, goethite and anhydrite), III (early subhedral calcite) and IV (barite, late subhedral calcite and gypsum), the oxidation state of the fluid changed towards more oxidising conditions and microbial sulphate reduction ceased. Three distinct modes of fluid salinities around 5.3, 3.4 and 0.3 wt% NaCl-equivalent characterise the mineralisation stages II, III and IV, respectively. The salinity of the stage I fluid is unknown due to lack of fluid inclusions. Variation in homogenisation temperatures and in δ18O values of amethyst show evidence of repeated pulses of ascending hydrothermal fluids of up to 80–90 °C infiltrating a basaltic host rock of less than 45 °C. Colourless quartz and amethyst formed at temperatures between 40 and 80 °C, while the different calcite generations and late gypsum precipitated at temperatures below 45 °C. Calculated oxygen isotope composition of the amethyst-precipitating fluid in combination with δD values of amethyst-hosted fluid inclusions (−59 to −51 ‰) show a significant 18O-shift from the meteoric water line. This 18O-shift, high salinities of the fluid inclusions with chloride-sulphate composition, and high δ34S values of anhydrite and barite (7.5 to 9.9 ‰) suggest that sedimentary brines from deeper parts of the Guarani aquifer system must have been responsible for the amethyst mineralisation.

Estudo da suscetibilidade ao escurecimento por radiação gama de quartzo róseo-leitoso da província pegmatítica da Borborema

This work has investigated the changes induced by γ-radiation on impurity-related point defects in massive rose quartz from one deposit located at The Borborema Pegmatite Province (Northeast Region, in Brazil). Samples extracted from rose and colorless (milky) quartz blocks were irradiated with doses of 60Co, from 0.5 to 96 kGy. Point defects related to Al, Ge, Li and OH were measured by optical, infrared, and electron paramagnetic resonance spectroscopy, prior and after irradiation. The contents of Al, Li, Ge, Fe, Ti and other impurities were measured by inductively-coupled plasma mass spectrometry in quartz fragments exhibiting rose, pale-rose, and milky colorations. It was found that [AlO4]0, [AlO4/H]0 and [GeO4/Li]0 were generated by the dissociation of [AlO4/Li]0 and [Li-OH] centers with doses as lower as 0.5 kGy. Above 8 kGy, the electron paramagnetic resonance signal related to [GeO4/Li]0 decreases due to the intense mobility of Li species throughout the quartz lattice, giving rise to E’1 centers perturbed by Ge. The increase in [AlO4]0 content with γ doses and the consequent rise in the intensity of smoky color were similar for both rose and colorless quartz. Scanning electron microscopy carried out in insoluble residues obtained after chemical dissolution of each type of quartz revealed the presence of nanometric fibers only in rose specimens. These results suggested that the cause of rose color in massive quartz from Borborema Pegmatite Province is probably related to the presence of dumortierite inclusions.

Determination of the potential for extrinsic color development in natural colorless quartz

Colorless natural quartz can develop many extrinsic colors after exposure to ionizing radiation and heat due to trace elements such as aluminum, iron, hydrogen, lithium, and sodium. The infrared spectrum of colorless natural quartz is correlated to the development of these colors, because the bands between 3200 and 3600 cm-1 are related to the presence of trace elements. The colors produced by γ-ray or electron beam irradiation are caused by displacements of electrons in the quartz lattice and can be bleached by ultraviolet irradiation. Colors produced by irradiation and additional heating, however, are resistant to ultraviolet rays, probably due to Li+ diffusion. The infrared spectra of colorless natural quartz crystals can be used to identify the crystals’ potential for color development by irradiation and heating. At room temperature, all natural colorless samples of alpha quartz show bands at 2499, 2600, 2677, 2771, 2935, and 3063 cm-1. The samples that do not develop color after irradiation also show bands at 3202 and 3304 cm-1. The samples that become grayish to black after irradiation show three additional bands at 3381, 3433, and 3483 cm-1. This last band is related to the development of the colors greenish yellow, yellow, or brown (citrine) after irradiation and heating. The samples that become grayish olive green after irradiation and olive green after additional heating show a pair of bands at 3404 and 3510 cm-1 in addition to the former bands noted. The samples that become violet (amethyst) or green (prasiolite) after irradiation, or sky blue after irradiation plus heating show a broad band at ~3441 cm-1 and a band at 3585 cm-1.

Identificação de quartzos incolores para joalheria

Quartzos incolores são irradiados e aquecidos para adquirirem cores esverdeadas, amareladas e amarronzadas para confecção de jóias. Somente uma pequena fração dos quartzos naturais incolores pode desenvolver cores por esse processo. A sua identificação é feita através de testes de irradiação e aquecimento em amostras representativas, que são enviadas para irradiadores para depois serem aquecidas. Trata-se de um procedimento demorado, que não atende a necessidade do mercado de pedras semipreciosas. Um novo teste é apresentado, que dispensa irradiação e aquecimento, para identificação de amostras com potencial para desenvolver cores, cujos resultados podem ser obtidos em apenas alguns minutos. Ele pode ser realizado no campo com um espectrofotômetro infravermelho portátil.

The optical absorption of gamma irradiated and heat-treated natural quartz

Quartz with aluminum as impurity absorbs energy from ionizing radiation and modifies its color. Colorless quartz becomes smoky or dark smoky (morion quartz) when exposed to gamma rays. By heat-treatment, smoky quartz may become successively greenish, yellowish, or brownish as the irradiation dose increases. Natural, colorless quartz is routinely colored by irradiation with gamma rays and heat-treatment for jewelry production. The color formation in natural quartz through this procedure is explained based on EPR, UV-VIS, and IR studies of irradiated and irradiated and heat-treated samples. Smoky quartz shows absorption bands in the visible region and a strong EPR signal. After heat-treatment it shows absorption bands in the near UV region with extensions into the visible region and a weak EPR signal. The intensity of the absorption bands is proportional to the irradiation dose. These changes of color are explained by the model of Itoh, Stoneham, and Stoneham. [AlSi O4 /h+]0 centers are produced by irradiation, causing the EPR signal and the absorption bands in the visible region. [AlSi O4]- centers are created from [AlSi O4 /h+]0 centers by heat-treatment. They cannot cause an EPR signal and have absorption bands in the near UV region with extensions into the visible region. The highest concentration of [AlSi O4]- centers occurs when the charge compensators have medium mobility. Lithium should give the best condition for color formation. Sodium (low mobility) and hydrogen (high mobility) should make smoky quartz colorless after heat-treatment.

What Oxidation State of Iron Determines the Amethyst Colour?

A colourless quartz crystal doped with 57Fe3+ was obtained by hydrothermal synthesis in an NH4F solution. The crystal was transformed into violet amethyst by gamma-irradiation. The change in colour was accompanied by changes in the Mossbauer spectrum that can be interpreted as the conversion of trivalent iron into the tetravalent state: Fe3+ → Fe4+.

Genesis of amethyst geodes in basaltic rocks of the Serra Geral Formation (Ametista do Sul, Rio Grande do Sul, Brazil): a fluid inclusion, REE, oxygen, carbon, and Sr isotope study on basalt, quartz, and calcite

In the Ametista do Sul area, Rio Grande do Sul, Brazil, amethyst-bearing geodes are hosted by a ~40- to 50-m-thick subhorizontal high-Ti basaltic lava flow of the Lower Cretaceous Parana Continental Flood Basalt Province. The typically spherical cap-shaped, sometimes vertically elongated geodes display an outer rim of celadonite followed inwards by agate and colorless and finally amethystine quartz. Calcite formed throughout the whole crystallization sequence, but most commonly as very late euhedral crystals, sometimes with gypsum, in the central cavity. Fluid inclusions in colorless quartz and amethyst are predominantly monophase and contain an aqueous liquid. Two-phase liquid–vapor inclusions are rare. Some with a consistent degree of fill homogenize into the liquid between 95 and 98 °C. Ice-melting temperatures in the absence of a vapor phase between –4 and +4 °C indicate low salinities. Chondrite-normalized REE patterns of calcites are highly variable and show generally no systematic correlation with the paragenetic sequence. The oxygen isotope composition of calcites is very homogeneous (δ18OVSMOW=24.9±1.1‰, n=34) indicating crystallization temperatures of less than 100 °C. Carbon isotope values of calcites show a considerable variation ranging from –18.7 to –2.9‰ (VPDB). The 87Sr/86Sr ratio of calcites varies between 0.706 and 0.708 and is more radiogenic than that of the host basalt (~0.705). The most likely source of silica, calcium, carbon, and minor elements in the infill of the geodes is the highly reactive interstitial glass of the host basalts leached by gas-poor aqueous solutions of meteoric origin ascending from the locally artesian Botucatu aquifer system in the footwall of the volcanic sequence. The genesis of amethyst geodes in basalts at Ametista do Sul, Brazil, is thus considered as a two-stage process with an early magmatic protogeode formation and a late, low temperature infill of the cavity.

Electron irradiation damage in quartz, SiO2

Crystallographically orientated samples of synthetic optical-grade colourless quartz with high chemical purity and low dislocation density together with synthetic gem-grade amethyst with high Fe-concentration and ca. 250 H/106 Si (“dry”) or 600 H/106 Si (“wet”) and with very high dislocation densities were irradiated using TEM. Samples of cuts perpendicular ( -cuts) and parallel ( -cuts) to the c-axis, that were as-grown or pretreated for 5 days at 820 K on air or under p(H2O)=108 Pa were prepared. Characterization methods used include AAS, FTIR, Raman-spectroscopy, X-ray-topography, REM, TEM in SAED and bright-field mode and polarized light microscopy. Radiolysis was carried out in TEM from 10 to 300 K with 100 kV and from 70–850 K (low-high-transition temperature of quartz) with 200 kV. Irradiation damage was investigated by decay of Kikuchi-lines or of Bragg reflections in SAED and in bright-field mode by development of strain contrast centres and of noncrystalline volume areas. Special preparates where the irradiation damage was of microscopic dimensions were investigated using Raman-spectroscopy. Radiolysis of quartz is able to proceed at 10 K with measurable velocity. The required electron dose for a standardized irradiation damage decreases with increasing temperature. At ca. 500 K it goes through a minimum and then increases steadily up to ca. 700 K. From there the increase is steep until ca. 820 K where it culminates sharply, showing strong fluctuations until 850 K. The -cuts in the as-grown state show significantly higher irradiation damage sensitivity than -cuts. Dry or hydrothermal preheating increases the overall sensitivity of irradiation damage and levels out the orientation differences. The high Fe-concentrations in amethyst in comparison with very pure quartz have no detectable influence on the damage sensitivity. This is also true for different water concentrations independently from the ratio of silanole-group to molecular water. Sample thinning by ion etching with different gun currents produces differences in irradiation sensitivity. Thinning by crushing produces samples with sensitivities comparable with ion-etching at low gun current.

Leisingite, Cu(Mg,Cu,Fe,Zn)2Te6+O6·6H2O, a new mineral species from the Centennial Eureka mine, Juab County, Utah

AbstractLeisingite, ideally Cu(Mg,Cu,Fe,Zn)2Te6+O6·6H2O, is hexagonal, P3 (143), with unit-cell parameters refined from powder data: a = 5.305(1), c = 9.693(6) Å, V = 236.2(2) Å3, c/a = 1.8271, Z = 1. The strongest six reflections of the X-ray powder-diffraction pattern [d in Å (I) (hkl)] are: 9.70 (100) (001), 4.834 (80) (002), 4.604 (60) (100), 2.655 (60) (110), 2.556 (70) (111) and 2.326 (70) (112). The mineral is found on the dumps of the Centennial Eureka mine, Juab County, Utah U.S.A. where it occurs as isolated, or rarely as clusters of, hexagonal-shaped very thin plates or foliated masses in small vugs of crumbly to drusy white to colourless quartz. Associated minerals are jensenite, cesbronite and hematite. Individual crystals are subhedral to euhedral and average less than 0.1 mm in size. Cleavage {001} perfect. Forms are: {001} major; {100}, {110} minute. The mineral is transparent to somewhat translucent, pale yellow to pale orange-yellow, with a pale yellow streak and an uneven fracture. Leisingite is vitreous with a somewhat satiny to frosted appearance, brittle to somewhat flexible and nonfluorescent; H(Mohs) 3–4; D(calc.) 3.41 for the idealized formula; uniaxial negative, ω = 1.803(3), ɛ = 1.581 (calc.). Averaged electron-microprobe analyses yielded CuO 24.71, FeO 6.86, MgO 6.19, ZnO 0.45, TeO3 36.94, H2O (calc.) [21.55], total [96.70] wt.%, leading to the empirical formula based on O = 12. The infrared absorption spectrum shows definite bands for structural H2O with an O-H stretching frequency centered at 3253 cm−1 and a H-O-H flexing frequency centered at 1670 cm−l. The mineral name honours Joseph F. Leising, Reno, Nevada, who helped collect the discovery specimens.

Stable-isotope, fluid-inclusion, and mineralogical studies relating to the genesis of amethyst, Thunder Bay Amethyst Mine, Ontario

The Thunder Bay Amethyst Mine exploits a vein system in which the main zoned sequence consists of chalcedony, colorless quartz, and three to four stages of amethyst. The main sequence surrounds fragments of a brecciated earlier sequence containing chalcedony, colorless quartz, and prasiolite, which appears to be thermally bleached amethyst. The vein system occupies a fault in Archean granodiorite and is associated with a narrow zone of chloritic and hematite alteration overprinted by weak argillic alteration. Fragments of Proterozoic (1339 Ma) Sibley Group rocks occur in the vein system, indicating the former presence of a shallow cover during deposition of quartz and limiting the maximum age of the deposit. These downfallen fragments and the abundance of vugs indicate near-surface formation of the deposit.Main-stage fluid-inclusion homogenization temperatures are in the range from 91.2 to 40.9 °C (mean 68.4 °C) in amethyst, whereas in colorless quartz homogenization temperatures range from 146.5 to 114.7 °C (mean 132.1 °C). Eutectic temperatures fall in three ranges with means of −50.9, −48.7, and −43.9 °C, which are related to paragenetic position and indicate an NaCl–CaCl2–H2O system, with possible additional components in later inclusions. Salinities in amethyst-hosted inclusions decrease in the growth direction from 22.9 to 15.3 equiv.wt% NaCl.Trace sulfide and other mineral inclusions indicate a trend of decreasing Eh and pH from an initially rather oxidized (sulfate stable) to a reduced (sulfide stable) condition during deposition. Sulfur isotopic composition in pyrite and chalcopyrite ranges from δ34S = −0.4 to −1.4‰ and is similar to values obtained from lead–zinc–barite in other vein deposits surrounding the Sibley depositional basin. Oxygen isotopes in quartz range from δ18O = +12.7 to +17.1‰, corresponding to δ18O(H2O) = −2.1 to −12.8‰ using fluid-inclusion temperatures. Fresh quartz monzonite wall rock (δ18O = +11.82‰) and altered quartz monzonite (δ18O = +11.01‰) do not seem to have undergone significant isotopic exchange with the hydrothermal solution, and the trend of isotopic change does not account for the trend of δ18O(H2O) determined in quartz. Rather, mixing of local meteoric water with a basinal brine appears to explain the observed trend.The amethyst deposits are believed to have been formed by basinal brines expelled from Sibley Group sediments. The brines dissolved silica by alteration processes accompanying their passage through granitic basement rocks in basin marginal faults. Amethyst was deposited on mixing with meteoric water. The temperature interval for amethyst formation appears to be restricted to less than ~90 °C. Temperatures causing thermal bleaching of amethyst are as low as 145 °C, and possibly 115 °C, as indicated by these results. This low range of temperature is not in agreement with bench-type experiments indicating bleaching at hundreds of degrees Celsius.

An Electrolytically Generated, Localized Hole Center in Quartz

Abstract In natural smoky quartz and neutron-irradiated, initially colorless quartz a new hole center was formed electrolytically at temperatures near 1100 K in addition to the well-known smoky quartz center. Unlike the latter its electron paramagnetic resonance spectra can already be measured at room temperature due to firm localization of the hole on one oxygen. It is characterized by fairly small hyperfine splittings due to Al impurity and significant deviations of all three principal g factors from that of a free electron. A tentative model for the structure of this center is proposed. An activation energy of 215 kJ/mol was determined for this electrolytic coloration from the temperature dependence of the electrolysis currents.

Tribobreakdown in glasses induced by subthreshold high-intensity radiation

In the experiments we used the procedure for determining the emission of electromagnetic waves presented in [6], in which the signals are measured to within 0.i mV. The experiments were performed with careful shielding of the samples from external signals. The high-intensity radiation (% = 1.06 units, T ~ 10 -3 and 3"i0 -s sec) with different intensity acted on the sample placed in a metallic jacket. Electromagnetic signals (noise) from the light interaction were not recorded, which was monitored by tests: without and with a sample, but no fracturing (the sample was additionally shielded). A sample with a mechanical break was also placed in the same jacket the entire mechanical action system was carefully shielded. The samples consisted of K-8 silicate glass with dimensions of i  1  5 cm, organic glass (polymethyl methacrylate -- PMMA) with dimensions 1 x 1 x 3 cm, and colorless quartz with dimensions of 1.5 x 1.5 x 2 cm. The radiation was focused inside the samples by a lens with a focal length F = 5 cm. The radiation intensity (I) wasequal to0.1, 0.3,0,5, 0.7,0.9, 1.5,2 Ith(with one-time action of threshold radiation with I = Ip single mechanical fractures with minimum dimensions of ~50-i00 ~m appear). At least 20 experiments were performed for each type of sample and value of E. Figures la and 2a show the measurements of the electromagnetic signals (EMS), which appear with "purely mechanical" fracture of the PPM and K-8 glass samples. The maximum magnitude of the EMS in the experiments is equal to 30-40 mV. In the presence of fracturing (motion of the crack) new free surfaces, on which charge is located and the field of the charge is sufficient to breakdown the gas filling the space between the surfaces being formed, are constantly forming [7, 8]. Thus, it can be conjectured that the EMS recorded is produced by tribobreakdown accompanying the mechanical fracturing of the samples. Figures la and 2a contain an entire series of separate spikes-signals, which can be attributed to the appearance of a series of cracks: new cracks appear in front of the main cracks [9]. Judging from the duration of the EMS, the time for the motion of the cracks is equal to ~i0 -2 sec in PMMA and ~2"i0 -3 sec in K-8 glass, which is an entirely reasonable value. In fracturing the K-8 glass samples, we made a cut on their surfaces, which probably encourages the forward motion of the crack.

Permittivities of single-crystal quartz at X band

Although fused quartz (Si02) is known to have good dielectric properties at microwave frequencies, and, although Fe3+ in quartz is a possible maser material, the principal values of the permittivity for single-crystal quartz do not appear to have been determined in the microwave region. Preliminary measurements are presented of these at X band for high-quality, colourless mineral quartz, as used for piezoelectric crystals.

Beobachtungen über Lamellenbau an Bergkristallen1

A mimetic structure consisting of optically weakly biaxial lamellae was observed in clear colourless quartz crystals from Madagascar in those areas which show an enrichment in the trace elements Al, Li and H. Different types of lamellae can be established on the basis of their optics, colouration on irradiation and orientation with respect to the morphology. Several observations support a secondary origin for the lamellae.