Rectorite (REC) was modified with dodecyl benzyl dimethyl ammonium chloride (1227) to form an organic-modified rectorite, termed OREC. The OREC was used as a filler additive to modify gel polymer electrolytes (GPEs) which consisted of polymethyl methacrylate (PMMA), propylene carbonate (PC) and LiClO4. Studies of ionic conductivity and viscosity of liquid electrolytes and pure PC, respectively, clearly showed that these properties are greatly influenced by temperature and the amount of OREC added; a consequence of the interactions between the components of CPEs. The Fourier transform infrared (FTIR) spectroscopy results indicated that there were two kinds of interaction: namely (1) a strong hydrogen bond between Si–OH and C=O of PC and (2) a weak interaction between Li+ and C=O. Inverse gas chromatography (IGC) research supported the FTIR interpretation, indicating that the two interactions exist and that the H bond is the stronger of the two. In CPEs, the polymer matrix of PMMA merely supports the active components and does not influence the interactions between them. The OREC greatly increased the crucial plasticizer maintenance property when the amount of clay added was optimum.

Microanalytical data on Plio-Pleistocene sediments from a Salton Sea Geothermal Field well define the evolution of textures and mineral assemblages from sediment to metamorphic rock in an open hydrothermal system.

At shallow depths detrital grains occur within a fine-grained matrix of I-S and illite. As depth and temperature increase, grains lose their detrital characteristics; they subsequently form a continuous intergrown array of irregular domains, with phyllosilicates occupying the progressively decreasing pore space.

Illite and chlorite are authigenic phyllosilicates down to 2500 m, where biotite occurs. Authigenic phyllosilicates occur as subhedral crystals (200 –600 Å thick). Alkali feldspar has end-member compositions, implying exchange of alkalis with convected fluids. Changes in texture imply dissolution of detrital phases and neocrystallization of authigenic phyllosilicates directly from pore fluids. Changes with depth are not time-dependent for phyllosilicates: they formed simultaneously at all depths as a result of a single hydrothermal event in an open system.

A pyridine-vermiculite complex has been investigated by three dimensional X-ray diffraction techniques. The preparation of the complex was carried out at a pH ∼ 4 using a solution of pyridinium hydrochloride. Exsolved magnesium from the octahedral positions satisfied approximately one-half of the cation exchange capacity. The rest of the exchange capacity is satisfied by hydrogen ions and pyridinium ions which are statistically distributed over crystallographic sites so that less than three electrons per Å3 are present at any given point. Three dimensional difference electron density maps did not locate the carbon atoms except to indicate that the organic molecule occupies positions in the true and in the two pseudo mirror planes in the unit cell. Water molecules were present in the interlayer in octahedral arrangement around the cation as in the natural mineral.

The present study examines the characteristics of clay minerals in shale gas reservoirs and their influence on reservoir properties based on X-ray diffraction and scanning electron microscopy. These analyses were combined with optical microscopy observations and core and well-log data to investigate the genesis, distribution characteristics, main controlling factors and pore features of clay minerals of the Lower Silurian Longmaxi Formation in the East Sichuan area, China. The clay mineral assemblage consists of illite + mixed-layer illite-smectite (I-S) + chlorite. This assemblage includes three sources of clay minerals: detrital, authigenic and diagenetic minerals. The lower section of the Longmaxi Formation in the Jiaoshiba area has sealing ability which resulted in abnormal high pressures during hydrocarbon generation which inhibited illitization. Therefore, an anomalous transformation sequence is present in which the mixed-layer I-S content increases with depth. This anomalous transformation sequence can be used to infer the existence of abnormal high pressures. The detrital components of the formation also affect the clay-minerals content indirectly, especially the abundance of K-feldspar. The transformation of mixed-layer I-S to illite is limited due to the limited availability of K+, which determines the extent of transformation. Three types of pores were observed in the shale reservoir rocks of the Longmaxi Formation: interparticle (interP) pores, intraparticle (intraP) pores and organic-matter pores. The clay-mineral content controls the development of intraP pores, which are dominated by pores within clay particles. For a given clay mineral content, smectite and mixed-layer I-S were more conducive to the development of shale-gas reservoirs than other clay minerals.

High-performance mullite-based composite ceramics were prepared successfully using natural kaolin and alumina as raw materials and ZrO2 as an additive. The influence of sintering temperature and ZrO2 content on the sintering behaviour and mechanical properties of zirconia-toughened mullite ceramics was studied systematically. With increasing sintering temperature from 1450°C to 1560°C, the primary phases of as-sintered composite ceramics were mullite and corundum with a small amount of ZrO2, and the bulk density of the composite ceramics increased from 2.29 to 2.72 g cm–3. Furthermore, the ZrO2 phase transition promoted transgranular fracture, and ZrO2 grains were pinned at the grain boundaries, thereby enhancing the mechanical strength of the composite ceramics. Moreover, the AZS12 sample, with 12 wt.% ZrO2 and sintered at 1560°C, had the greatest flexural strength and fracture toughness of 91.6 MPa and 2.47 MPa m–1/2, respectively. Adding ZrO2 to the composite ceramics increased their flexural strength by ~37.6%.

Clay mineral ‘Crystallinity Index Standards’ (CIS) composed of Palaeozoic mudrocks from southwest England were investigated systematically in five sub-fractions per sample for the first time. X-ray diffraction was used to determine mineral assemblages, calibrated 001 illite full-width-at-half-maximum (FWHM) values and illite polytype compositions, in addition to K–Ar isotopic analyses of all fine fractions. The FWHM results of the <2 µm fraction are consistent with previous studies and reflect the range of diagenetic to epizonal grades covered by the sample set SW1 to SW7 (~0.61–0.26°2θ). Diagenetic and lower anchizone samples also show significant broadening of 001 illite reflections in the finer fractions and contain mixtures of authigenic 1M + 1Md illite and detrital 2M1 white mica polytypes suitable for illite age analysis. The estimated end-member ages of the Bude (SW1-1992) and younger Crackington (SW3-2000) mudstones yield detrital ages of Late Cambrian to Middle Ordovician (493–457 Ma) and a broad range of 1M + 1Md illite ages between Middle Permian and Early Jurassic (271–190 Ma). The detrital age of the stratigraphically older Crackington Formation mudrock (SW2-1992) is Late Devonian (384–364 Ma) with 1M + 1Md illite ages between Late Triassic and Early Jurassic (219–176 Ma). The origin of Mesozoic 1M + 1Md illite ages may represent neocrystallized illite associated with Mesozoic hydrothermal events or similar events that thermally reset older authigenic illite with partial loss of radiogenic argon and no renewed crystal growth. In contrast, upper anchizonal and epizonal Devonian slates (SW3-2012, SW4-1992, SW6-1992 and SW7-2012) contain only the 2M1 polytype, with K–Ar ages younger than the stratigraphic age. The three finest fractions of SW4-1992 yield consistent Late Carboniferous ages (331–304 ± 7 Ma) that are considered to date the neocrystallized 2M1 mica. Most fractions of epizonal slate (SW6-1992, SW7-2012) yield Early Permian ages (293.6–273 Ma) corresponding to published cooling ages of the Tintagel High-Strain Zone and the intrusion of the Bodmin granite (291.4 ± 0.8 Ma). These first K–Ar age constraints for the fine fractions of the CIS should provide useful reference values for testing analytical procedures of illite age analysis.

A recent article by Refait & Génin (1997) was devoted to Ni(II)-Fe(II)-Fe(III) pyroaurite-like hydroxychlorides obtained by aerial oxidation of mixed Ni(II)-Fe(II) hydroxides with various P = Fe/Ni ratios in chloride-containing aqueous solutions. Corresponding to the ideal composition Ni3-xIIFexIIFeIII(OH)8Cl.nH2O , the Fe(III)/[Ni(II)+Fe(II)] ratio is 1/3 when P is >1/3. These hydroxyehlorides oxidize quickly and the final product depends on P. In the absence of nickel, P = ∞, FeII3FeIII(OH)8Cl.nH2O, known as Green Rust one (Bemal et al, 1959) oxidizes into γ-FeOOH. When P is >5/3, the X-ray diffraction (XRD) analyses of the end-product reveal lepidocrocite and some Ni(II)-Fe(III) hydroxychloride.

A scanning and transmission electron microscopy study has been performed on Oligocene glacio-marine sediments, Devonian sandstones, and Jurassic dolerites recovered during CRP-3 drilling in the Ross Sea (Antarctica). Newly formed clay minerals occur in the rock matrices and as fillings in veins and faults which crosscut the whole sequence. Authigenic clays in sediments consist of beidellite-montmorillonite, berthierine/chlorite intergrowths and illite. Al,K-rich smectites and kaolinite occur in the Devonian sandstones. Saponite, berthierine/chlorite intergrowths, and Fe-hydroxides develop in the altered dolerites. Hence, the composition of the secondary phases depends also on the geochemistry of the rock they grow in. Within each sample, the same authigenic minerals form in the matrix and in the vein/fault. Clays precipitated from fluids, with variable fO2 values, which circulated in the system during the contemporaneous diagenetic and faulting events.

The mineralogy of the glazed surfaces of Japanese sekishu roof tiles covered by a crustose lichen – Lecidella asema (Nyl.) Knoph & Hertel – was investigated using transmission electron microscopy (TEM). The study sought to identify the Ti-Fe mineral observed as a low concentration of Ti and Fe in a previous study of the glazed surfaces of the same roof tile. The TEM analysis revealed that: (1) a thin layer of the Ti-Fe mineral pseudobrookite exists on the glaze surface; (2) the pseudobrookite consists of well-ordered single crystals, continuously and widely distributed on the glaze surface.

The Lòn Ostatoin stream section, Trotternish Peninsula, Isle of Skye, exposes a sequence of Middle Jurassic mudstones and limestones which have been locally metasomatized by a transgressive sill of Tertiary age. Limestones in the sequence, including some previously reported as bentonite, have been altered to an unusual assemblage of grossular garnet and saponite clay. The mudstones also contain large proportions of saponite together with pyroxene and zeolites. Saponite also occurs within the basalt intrusion. Grossular and pyroxene represent artifacts of relatively high-temperature assemblages that formed during an early phase of alteration. As the intrusion and adjacent altered country rocks cooled, lower-temperature fluids flowed through a late set of contraction (micro)fractures. Back-reacted saponite, analcime and clinoptilolite were formed, possibly as alteration products of the unstable higher-temperature minerals. The lower-temperature mineral assemblage eventually sealed the late fracture system.

This paper highlights an important concept for the study of analogue sites used to investigate thermal effects on engineered liners or barrier host rocks for the landfill and radioactive-waste industries. This is that the original thermally altered mineral assemblage may be overprinted by later, lower-temperature back-reactions. A detailed understanding of both processes is necessary in order to construct a sensible model for the thermal and mineralogical evolution of the site.

Many analyses of montmorillonite indicate liberation of water above 300°C in excess of the amount required by the structure proposed by Hofmann, Endell and Wilm (1933). The structure of Edelman and Favejee (1940) will account for a larger quantity of water, but other inconsistencies with experimental results seem to arise.

Using as an analogy the hydrogarnets (Flint et al.; Pabst ; McConnell), it is suggested that hydroxyl ions can occur as tetrahedral groups within the silica sheets in substitution for SiO4 groups. Liberation of this "tetrahedral water" is believed to be associated with the second high-temperature endotherm which is occasionally a small deflection on the D.T.A. curve but is, nevertheless, characteristic of montmorillonite.

Data are presented for the effects of wet and dry grinding on dickite from Ouray, Colorado. With increase in dry grinding time the endothermic d.t.a. peak becomes broader and moves towards a lower temperature, while the exothermic reaction is greatly sharpened. Weight loss data, demonstrate greater water loss from ground material and over a longer temperature range. X-ray powder photographs show that after a relatively short period of grinding little further destruction of the lattice occurs, and this lattice destruction apparently proceeds only to a certain stage, for high order spacings of hkl are very persistent.

In a series of test tubes, increasing amounts of pure cetyltrimethyl ammonium bromide (Lissolamine A) are added to a dilute clay suspension containing a known amount of clay. Visual examination of the contents of the tubes shows a stability minimum to exist at a certain concentration of the bromide. It may be assumed that in this stability minimum the clay micelles are neutralized by quantitative exchange of the exchangeable ions of the clay by an equivalent amount of strongly adsorbed organic cations of the bromide. Consequently the b.e.c, of the clay may be calculated from the concentration of the cation-active compound at the stability minimum. Since, however, by visual examination the stability minimum cannot be distinguished sharply enough, a better criterion had to be developed. As there are reasons to assume that the neutralized micelle will act as an emulsifier for oil-water systems, an emulsification test was expected to offer a way out. It was indeed found that on shaking the contents of the tubes with gas-oil, a rather stable emulsion was formed at a certain critical concentration of the cation active compound. Taking this concentration as an indication of quantitative exchange, the b.e.c, of the micelle may be easily calculated. Results of preliminary experiments are in good agreement with those obtained by application of conventional methods.

For several decades clays have been used for decolorising mineral oils. A simple method is percolation of the oil through a layer of clay. Some twenty times the amount of oil is usually treated with such a layer. The first oil filtered through the fresh clay is much more changed than the rest of the oil. It has a very light colour and its low refractive index indicates a high content of paraffinic and naphthenic hydrocarbons.

Most of the aromatic hydrocarbons are left behind in the clay. This suggests adsorption analysis of oils using clay in the same large quantities that have been successful with other adsorbents (Mair and White, 1935; Willingham, 1939; Allibone, 1941). Quantities of the order of 100 gm. alumina per gm. hydrocarbon were used by Winterstein and associates (1934) when separating a number of aromatic hydrocarbons.

A simple method is described for determining the approximate positions of Li+, Mg2+ and Ca2+ in three montmorillonite samples saturated with these cations and subsequently dehydroxylated. The method depends only upon changes in the relative intensity of the three lowest order basal reflections, and its applicability to other problems is illustrated.

Clays from the Saïss basin (northern Morocco) used traditionally in the ceramic industry in the Fez area were studied using mineralogical and physicochemical techniques to evaluate their potential suitability as raw materials for ceramics manufacture. X-ray diffraction was used to determine their mineralogical composition. The physical properties determined were particle-size distribution and consistency limits. The chemical composition was determined using X-ray fluorescence analysis and Fourier-transform infrared spectrometry. The structural changes of the mineral phases in the raw materials during firing were studied over a temperature range of 500–1000°C. In the pottery site from Fez, generally potters use a mixture of 25% fine clay (ARFS) from the upper part of the Miocene marls and 75% sandy clay (ARFR) from the lower part of the Miocene marls. The ARFS clay yielded very rigid specimens after firing that artisan potters would find difficult to handle so as to produce desired shapes and sizes. However, the specimens obtained from ARFR clay show signs of faltering. The mixture of these two clayey materials from this pottery site is therefore necessary to obtain the optimal paste for ceramics purposes. The chemical compositions indicated that SiO2, Al2O3, CaO and Fe2O3 are the major minerals, with trace amounts of K2O and MgO. Quartz, feldspars and clay minerals prevail in all samples. Kaolinite, illite and smectite are the dominant clay mineral phases, with traces of chlorite and interstratified illite–smectite. The classification of these samples using appropriate ternary diagrams showed that the proportions used in the mixture produce a new material with adequate characteristics for the production of traditional ceramics.

Basalts and related magmatic rocks such as diabase are frequently used as raw materials in the building and construction industry as dimension stones or as aggregates, where they may form the sub-bases of roads or railway embankments. A major characteristic controlling the quality of the raw materials is the rock strength, which can be affected by the presence of swellable clay minerals (smectites). Increasing smectite content is generally considered to increasingly affect rock integrity. Industrial practice, in which the smectite content is monitored via cation exchange capacity (CEC) methods, on the other hand, showed that both mechanically stable smectite-rich and unstable smectite-poor materials exist. We therefore studied the CEC–strength relation based on twelve samples from a German diabase quarry.

As could be expected, the sample with the highest CEC was the least stable. However, the comparison of the rock strength with the CEC of the other samples was less clear. Comparing the CEC of powders and of the 1–2 mm fraction of the same sample provided additional information. In the case of samples which are relatively stable (in spite of high CEC values), the CEC values of the powders were significantly higher than those of the 1–2 mm fraction. Samples with less rock strength, on the other hand, showed equal CEC values of the powder and the 1–2 mm fraction. This difference may be explained by different accessibilities of the smectites for CEC exchange solutions during typical experiments.

In conclusion, the application of the CEC method for quality control considering both powdered and 1–2 mm samples allows a more precise estimation of the rock strength to be made, particularly for the comparison of different materials. Although measurement of two CEC values (after both sieving and grinding) would complicate quality control, the present study indicates that valuable additional information, i.e. semi-quantitative information on the accessibility of smectites, is gained.

Fluid pressures in argillaceous sediments depend on, inter alia, mechanical stresses, temperature, diagenetic volume changes and permeability. However, the relative influence of the pressuring mechanisms depends critically upon the long time-scale compliance, C, of the overpressured layer.

In sediments undergoing first-time burial and currently exposed to their historically maximum applied stresses, C can be relatively large. Here, fluid pressure increases are principally due to mechanical causes, and overpressuring will be associated with undercompaction. The tendency for undercompaction (compaction disequilibrium) depends on the sediment thickness, burial rate and vertical permeability. In other cases, when applied stresses have been reduced by uplift, or when impermeable hard caps or seals have been formed, C may be substantially smaller. Here pore pressures may be predominantly controlled by diagenetic and aquathermal processes, with mechanical (undercompaction) phenomena being relatively less significant.

Three-dimensionally sealed overpressured zones may exhibit vertical fluid pressure discontinuities. Within a sealed aquifer, fluid pressures may rise to almost lithostatic values, relieved by episodic fracturing of the seal.

An X-ray diffraction technique has been used to determine the orientation pattern of the (001) planes of 10 Å micaceous minerals in slate. The guiding principle of this technique is the direct measurement of the diffracted radiation from the pre-selected family of crystallographic planes as a function of the orientation of the specimen.

Results obtained indicated that the basal planes of these minerals are mostly oriented in a direction parallel to the cleavage planes and the possibility of another orientation was considered to be slight.