Showing papers on "Clay minerals published in 1974"

Clay-containing fabric softening detergent compositions

Abstract: Granular, built laundry detergent compositions containing particular smectite clay minerals. Compositions containing such clays provide softening and/or antistatic benefits to fabrics washed therein.

The formation of goethite and hydrated clay minerals on Mars

Abstract: Laboratory studies reported by Huguenin (1973) on the kinetics and mechanism of the photostimulated oxidation of magnetic and preliminary laboratory data on the weathering of silicates, reported herein, are applied to Mars. Basalts in the Martian dark areas are predicted to alter to hydrated Fe(2 plus or minus) depleted clay minerals, minor goethite, and minor to trace amounts of transition metal oxides such as TiO2, MnO2, and Cr2O3 at a rate of 10 to the minus 1.5 plus or minus 1.5 micron/yr. Some Ca-Mg carbonates are also expected to be formed. The clay minerals are predicted to be more silica-rich than the silicate source material, SiO2 contents of 60% or higher being expected, and strongly depleted in Fe(2+). The oxygen, OH, and H2O contents of the bulk weathering product are predicted to be significantly greater than those of the dark-area source materials, whereas the relative bulk metal abundances should be the same.

Chemical Weathering of Serpentinite in the Eastern Piedmont of Maryland

Abstract: Weathering processes in a small watershed (Soldiers Delight) underlain by Serpentinite in the Piedmont of Maryland were studied by means of a mass balance technique and were compared with the processes operative in a watershed uncertain by schist. The two terranes are downwasting at a rate of 2.4 m per m.y., but chemical weathering much more strongly affects the Serpentinite (2.2 m per m.y.) than the schist (1.2 m per m.y.). The serpentinite lacks a saprolite cover because resistate minerals are absent and alumina in the bedrock is scarce. In contrast, the schist contains both quartz and a source of alumina in the alumino-silicate minerals and, as a result, has a thick saprolite mantle. Relatively small amounts of secondary quartz, chalcedony, and 14A clay minerals are synthesized in the serpentinite watershed, but relatively large amounts of gibbsite and clay minerals (kaolinite and vermiculite) are formed during the weathering of the schist. The hydrologic consequences in the serpentinite terrane compared with the schist watershed are increased flood-flow discharge, greater fluctuation in seasonal, instantaneous base-flow discharge, and pronounced seasonal fluctuations in total discharge. The serpentinite stream water averaged 205 ppm of total dissolved solids in the base flow compared to 25 ppm in the schist. Stream water from the serpentinite is of the magnesium bicarbonate type; that from the schist is sodium–calcium bicarbonate type. On the serpentinite, substantial land-surface reduction (denudation) is effected by chemical weathering; mechanical weathering is secondary. On the schist terrane, mechanical weathering is the primary agent that lowers the land surface, even though chemical weathering has reduced the rock mass ay almost one-half.

Diagenesis of Clay Minerals from Lower Cretaceous Shales of North Eastern British Columbia

Abstract: Clay minerals from shale outcrops of the Lower Cretaceous Buckinghorse Formation (4250 fl thick) were investigated in order to assess their degree of diagenesis and their oil-generating potential. Crystallinity index, sharpness ratio, per cent of illite which is the 2M polymorph and presence of discrete minerals have been studied in the whole clay fraction, while the very fine clay fraction has been subjected to X-ray diffraction, differential thermal, thermogravimetric, differential thermogravimetric, i.r. spectros- copy, surface area and chemical analyses. With information derived from these studies and from published data, a classification scheme was devised which relates variation of clay mineralogy to diagenetic stages and burial depth. Data on the < 2 #m size fraction show that the crystallinity index decreases while the sharpness ratio and per cent of illite which is the 2M polymorph increase with burial depth. Results on the <0.08/zm fraction reveal that a three-component interstratified clay mineral exists. In addition, Fourier transform calcula- tions and chemical and physicochemical analyses indicate that both the ratio of the amounts of non- hydrated clays (illite) to hydrated clays and the K2O content of clays increase with burial depth: cation exchange capacity and surface area decrease with burial depth. Based upon a classification scheme, which was devised by combining criteria and data derived from the studies of Weaver (1961a), Kubler (1966), Burst (1969)and Dunoyer de Seconzac (1970), the upper and middle parts of the formation (upper 3250 ft) fall within the middle stage of diagenesis whereas the lower part (1000 It) is allocated to the beginning of late diagenesis. In terms of Burst's (1969) work, the upper 3250 ft are transitional between the stability and dehydration zones indicating that, prior to uplift, hydrocarbons may have been in the process of migration. The lower 10000 ft of the formation are in the restricted dehydration zone, indicating that hydrocarbon migration should have been completed.

Absorbent product containing flocculated clay mineral aggregates

Abstract: The difficulties in using clay minerals as absorbents in articles such as diapers, floor mats, utility wiping cloths, etc. is overcome by flocculating the clay into granular aggregates. The dry aggregates are dispersed into a flexible fibrous support to prepare the absorbent products. The aggregates, additionally, show enhanced water absorbing properties in many instances.

Clays as Catalysts for Natural Processes

Abstract: Clay minerals are important constituents of the earth's crust not only because of their abundance but merely because of their chemical activity. Clays found in soils and in sediments are distributed among three main mineralogical groups: the kaolin, hydrated micas, and smectite groups. Allophanes derived from volcanic glasses and amorphous Al-Si or Fe-Si mixed oxide gels are also abundant in large areas. These clays and clay-like materials share two common characteristics: a high specific surface area and the presence of exposed cations on their surface. In the natural environment these cations are either Na +, K +, Ca2+, or Mg2+, and/or polynucleic Al or Fe basic cations such as [AI(OH-)x(H20)yJ�+ or [Fe(OH-)x(H20)yJ�+. They balance the excess negative charge of the lattice, generated by isomorphic substitutions (for instance substitution of Si4+ by AI3+ in tetrahedral position, or AI3+ by Mg2+ in octahedral position). A clay microcrystal may thus be considered as the salt of a weak acid, whose anion (i.e. the lattice) has an infinite radius of curvature. In this situation the electrical charges of the cations generate a high electrostatic field because of the very incomplete screening of the positive charges by the anionic lattice charges. Since the lattice charges have fixed positions, the electrical neutrality is easily achieved by monovalent alkali cations, while for divalent cations the situation is much less favorable. Oxygen atoms or hydroxyl groups are the main surface constituents. They may play an important role by forming hydrogen bonds with proton donor or acceptor molecules. In addition, van der Waals (or dispersion) forces are expected to be quite active because of the magnitude of the surface area. In the natural environment a variable number of layers of water molecules but also polar organic molecules do form an adsorbed phase in which many kinds of chemical transformations may occur. The surface constituents and the adsorbed water may show a high catalytic activity in these transformations. The aim of this contribution is to review the recent progress of our knowledge in this field. After a paragraph in which the surface properties of clays and clay-like minerals

Mineralogy and genesis of clays in red‐black soil toposequences on basic igneous rocks in kenya

Abstract: Summary The clay mineralogy of two red-black soil toposequences on basic igneous rocks in Kenya has been investigated. Besides some illite and amorphous material kaolinites predominate in the slope soils (ultisols) whereas smectites are the main clay minerals in the soils of the depressions (vertisols). The kaolinites are poorly crystalline and have high surface area. According to chemical analysis, IR spectroscopy, and D.T.A. the smectites appear to be a ferriferous member of the montmorillonite-beidellite series having approximately 0·5 Fe3+ in octahedral and 0·2 Al per O10(OH)2 in the tetrahedral position. The profile and slope distribution of kaolinites and smectites led to the conclusion that the smectites are the first weathering product and, depending on hydrological conditions governing the soil solution composition (Si, Mg, pH), either persist (depression) or are decomposed (slope) and followed by kaolinites.

Ironstones in the Upper Oxfordian of southern England

Abstract: The Upper Calcareous Grit, the last of the four upward shallowing cycles that comprise the Corallian Beds of southern England, is relatively enriched in iron minerals, having local developments of chamosite oolite mudstone and much more widespread deposits of sand and mud containing variable amounts of siderite and disseminated chamosite. The chamosite oolite mudstones have a restricted fauna dominated by oysters and probably accumulated in slightly hyposaline lagoons where the ooids formed from mixed iron-, alumina- and silica-bearing gels. Siderite was produced during diagenesis from iron carried on the surface of clay minerals. This intimate association with the terrigenous clay fraction means that siderite occurs in sediments deposited in a variety of environments ranging from offshore shelf to lagoonal. The most important factor responsible for ironstone development was a very low rate of clastic supply throughout Upper Calcareous Grit times. The iron was probably derived by normal processes of weathering and erosion of sedimentary rocks exposed around the basin margin, but this cannot be conclusively proved and quite different iron sources may have been involved.

Electrolyte concentration-permeability relationships in sodium illite-silt mixtures

Abstract: To examine the effects of clay swelling and dispersion on electrolyte concentration-permeability :relationships of low clay content soils, flow experiments were conducted on a silt of fixed particle size distribution containing 0, 5, 7.5, 10 and 15 per cent clay (sodium illite, 2 #m fraction). Flocculated specimens were sedimented using both slow and rapid procedures. After compression each specimen was permeated successively with electrolyte solutions which caused (1) swelling of the clay fraction (0.10 N), and (2) dispersion (0.05 N). Absolute permeabilities varied with clay content, sedimentation procedure, compression rate, and electrolyte concentration; however, the form of this variation plotted against through-put volume was similar for all specimens containing electrolyte solutions causing only swelling of the clay. Increasing the hydraulic gradient above a critical value apparently increased the swelling slightly as evidenced by further reductions in permeability. The permeability of mixtures permeated with electrolyte solution causing dispersion of the clay was more complex and depended on clay content, the hydraulic gradients used to introduce the dispersing electrolyte solution and the pre-dispersion gradients to which the specimens had been subjected. Permeability decreases were attributed to the last stages of swelling prior to dispersion and to pore plugging. Increases in permeability were the result of erosion of dispersed particles. Specimens previously sub- jected to the highest gradients while swelling dispersed more rapidly and had a greater tendency to erode. The effects of predispersion gradients diminished with increasing clay contents. It is concluded that both compositional and mechanical factors play an important role in determining electrolyte con- centration permeability relationships for soils containing active clay minerals.

Hydrothermal Origin of the Clays from the Upper Slopes of Mauna Kea, Hawaii

Abstract: The soils of the summit region of Mauna Kea are similar to the soils of the high mountain deserts and to the soils of cold deserts. Dramatic differences, however, exist between the soils of the summit and other neighboring cones and the soils of the glaciated terrain. The soils of some of the cones of the summit area are clay rich and contain phyllosilicate minerals; the soils of the glaciated terrain are sandy and contain X-ray amorphous clay. Montmorillonite and a Mg-rich trioctahedral mineral identified as saponite are the clay minerals of the summit. Because the summit area of Mauna Kea supported an ice cap at the time of the formation of the cones, the origin of the smectite minerals could have resulted from the alteration of the tephra by steam and water released in the melting of the ice. Hypogene fluids are, however, more likely to be responsible for the genesis of the phyllosilicate minerals.

Effect of Clay Minerals on Hetrotrophic Microbial Activity in Soil

Abstract: The heterotrophic activity of the soil microbiota (expressed as either CO2 production or O2 consumption) was determined after the addition of various organic substrates (e.g., saccharides, aliphatic and aromatic acids and aldehydes, amino acids; total of 25 compounds) to soils with which 0, 5, 10, or 20 percent montmorillonite or kaolinite or 5 percent mica-vermiculite had been incorporated. With the exception of aldehydes, the decomposition of which was accelerated by the presence of montmorillonite, no clear relationship was observed between the type of organic substrate and the type of clay mineral added. The initial rate and/or the extent of oxidation were either increased, decreased, or not affected by the addition of different clay minerals. In general, the initial rate of decomposition was influenced more by montmorillonite, whereas the extent of oxidation was affected more by kaolinite.

Properties of two fragipan soils in nova scotia including scanning electron micrographs

Abstract: About 250,000 acres of soil with fragipan have been mapped in Nova Scotia. The fragipan horizons of two soils (Tormentine and Debert) reported in this paper are typical for the province. They have high bulk densities and low saturated hydraulic conductivity. They are also low in organic carbon and free oxides. They are high in fine sand and silt but low in clay, and the fragments of fragipan are readily slaked in water. Mica, chlorite, vermiculite, and kaolinite were found in the clay fractions of both soils throughout the two profiles. A moderate amount of smectite was found in the clay fractions of the Ae horizon of Debert but not in the Tormentine profile. A significant amount of clay increase in both fine and total clay fraction was found in the Bf horizon of the Tormentine soil and the Bmgj and Btx horizons of the Debert soil, and results from translocation or lessivage. The brittleness and other associated properties of the fragipans were attributed to clay bridges linking coarser particles, which w...

Mineralogy of suspended sediment and concentration of Fe, Mn, Ni, Zn, Cu, and Pb in water and Fe, Mn, and Pb in suspended load of selected Kansas streams

Abstract: When concentration levels of the elements studied in the suspended sediment are compared to average reported values for shales, they show Fe to be low. The other elements are higher. Values for these elements in the dissolved portion are variable, reflecting in some cases possibly lithologic differences. The dissolved trace element composition of the water is not reflected in the chemistry of the detrital load. X-ray diffraction study of the mineralogical content of the suspended sediment indicated that mortmorillonite was the clay mineral present in all cases. Other minerals present in almost all the samples were calcite and quartz. Gypsum, dolomite, feldspar, illite, and kaolinite were present in lesser amounts in some of the samples. Some question of the source of specific trace elements in these stream waters exists. For Ni and Pb, however, pollution is a possible source. The iron and manganese levels in the suspended sediments of all streams are not unusual. Significant correlations of the Pb with Mn and Fe are strongly suggestive of coprecipitation with Fe and Mn oxides.

Adsorption of pentachlorophenol by soils

Abstract: The adsorption studies using soils various in the species of clay minerals and organic matter content indicate: 1) That apparent adsorption occurs to the greatest extent on the strong acid soil system compared to the moderate acid soil system, regardless of the species of clay mineral and organic matter content. And there is no adsorption on the slightly acid or neutral soil system. 2) The apparent adsorption involves adsorption of molecules and/or anions and precipitation of molecules in the micell and the external liquid phase. 3) The magnitude of adsorption occurs in the decreasing order of humus-allophanic, allophanic, montmorillonitic, and halloysitic soils. 4) The major factor governing the magnitude of apparent adsorption is pH.

Clay mineral distribution and origin in the soil types of israel

Abstract: Summary The mineralogical composition of clays (< 2μm) in representative profiles of all soil types of Israel was investigated. The soils were classified according to their clay mineral assemblages into three groups. I. Montmorillonitic soils. Montmorillonite is the dominant mineral and exceeds 65 per cent of the total minerals found; each of the other minerals comprises less than 15 per cent. 2. Montmorillonitic-kaolinitic soils. The soil clay fractions contain 50-60 per cent montmorillonite and 15-25 per cent kaolinite, generally adding up to more than 75 per cent of the clay fraction. 3. Montmorillonitic-calcitic soils. The clays contain more than 10 per cent calcite. Montmorillonite is the dominant clay mineral (except for one soil type, mountain rendzina, where calcite is dominant). The first and second assemblages are typical of the soils of the Mediterranean zone, whereas the soils of the desert zone are characterized by the third assemblage. The origin of montmorillonite, kaolinite, and illite, the three main clay minerals, was found to be detritic, as was the origin of palygorskite which was mainly found in the calcite rich soils of the desert zone. The cation exchange capacity of montmorillonite seems to be higher under higher precipitation. Montmorillonite content and cation exchange capacity of the clays were found to be highly correlated. The carbonate content of the clay fraction and the amount of carbonate in the soil were also highly correlated.

Non-exchangeable ammonium in soils of israel and its relation to clay and parent materials

Abstract: Summary The occurrence of non-exchangeable ammonium in the main soil groups of Israel and its relation to various factors were determined in 129 samples from thirty-one profiles. In arid and semiarid soils the level ranged from 0·18-0·53 me/100 g, with most values falling between 0·25 and 0·40 me/100 g. In the sub-humid Mediterranean region the values ranged between 0·04 and 1·0 me/100 g, with most of them falling between 0·14 and 0·65 me/100 g. In most cases the percentage of non-exchangeable ammonium-N in the total soil nitrogen was in the range of 2–25 per cent. The clay fraction is a significant factor influencing the amount of non-exchangeable ammonium in the soils tested. The relatively low amounts of non-exchangeable ammonium found are consistent with the predominant clay mineral in most of the soils being montmorillonite. A good correlation was obtained with the content of illite, which is the main carrier of the non-exchangeable ammonium. The mean non-exchangeable K/non-exchangeable NH, ratio in the Israeli soil clays was 17. In soils derived from or affected by aeolian dust, the level of non-exchangeable ammonium calculated for the clay fraction spans that of aeolian dust and is, in general, higher than in soils developed from limestone, dolomite, marl, tuff, or basalt.

Treatment of clay mineral pigment

Abstract: The invention provides a process for improving the rheological properties of an aqueous suspension of a clay mineral in which the aqueous suspension is mixed with a water-soluble organic compound having a plurality of basic groups and a number average molecular weight not greater than 1,000. The treated clay minerals may be used, for example, as the pigment in a paper coating composition.

An interstratified illite-smectite from denchworth series soil in weathered oxford clay

Abstract: A B S T R A C T : The very fine (< 0.04 p.m) clay fraction of a Denchworth series subsoil in weathered Oxford Clay has been investigated in detail. It contains a layer silicate mineral, almost free from impurities, that is a randomly interstratified mixture of approximately 45 % expanding and 55 % non-expanding interlayers with the following unit formula: Na0.33K0.29(All.41Fe0.34Mg0.26)(Si3.60AI0.40)Oll. Computersimulated diffraction patterns showed that experimental patterns are best matched when an average diffracting packet consists of between 4 and 5 2 : 1 layer silicate units. Correction of the chemical composition for external exchangeable ions associated with such small packets gives non-expanding interlayers a charge density of 0'69K/Si4Oll and expanding interlayers one of 0"57M~/Si4011. The relationship between these values and those of mica and regularly expanding minerals is briefly discussed.

Weathering Of Clay Minerals By Simulated Acid Coal Spoil-bank Solutions

Abstract: Kaolinite and mica clay minerals were subjected to simulated sulfuric acid coal strip-mine solutions for periods up to six months. These data indicate that the mode of attack of the acid on both clays was at the edges. The acid released Al, Fe, K, Si, and possibly other ions to the solution phase, thereby serving as one possible explanation for the large amounts of Al3+ found in coal spoil solutions. It appears in the case of mica that the dissolution of the edges (octahedral layer) precedes the removal of K+ from the interlayer positions. The rate of dissolution of kaolinite and mica were similar and one would not expect large changes in mineralogies of natural spoil-bank materials from acid dissolution when these spoil materials are dominated by these two minerals.

The clay mineralogy and some trace element contents of the speeton clay

Abstract: Summary Pronounced time-related trends are evident in the clay mineralogy of the Speeton Clay (Lower Cretaceous): the kaolinite/illite ratio decreases consistently as the sediments get younger, and the other main mineral, probably an illitesmectite, becomes progressively more illitic. It is suggested that these changes reflect weathering conditions at the source rather than differences in actual source-rock type or weathering of the Speeton Clay itself. This conclusion is supported by the relative consistency in trace element contents, which might be expected to reflect major changes in source material.

Micromorphological, physical, and chemical properties of a podzolic soil with a fragipan

Abstract: The soil had a thick, dark brown, highly porous Podzolic B horizon with a high content of amorphous Fe, Al- organic matter complex material and a low bulk density, underlain abruptly by a dense, gray fragipan with a bulk density of nearly 2 g/cm3. Mean pore diameters of subhorizons within the Podzolic B ranged from about 25 to 120 μm and those of the fragipan were about 0.5 μm. The marked contrast in porosity was consistent both with hydraulic conductivity values of about 20 cm/h in the Podzolic B and 0.2 cm/h in the fragipan, and with the micromorphology. Strongly oriented argillans in the fragipan indicated some clay translocation. The clay mineralogy indicated weak weathering of phyllosilicates, but appreciable weathering of primary minerals must have occurred to produce the amorphous Fe and Al- rich amorphous material in the Podzolic B. Seepage along the surface of the fragipan, and the absence of roots in this layer indicated the significance of this horizon with respect to plant growth and to the wa...