bluuebunny/crossref_metadata_2025_split huggingface dataset:
Effect of Dry Grinding on Kaolin Minerals
Authors: Takahashi Hiroshi 
Published: August 2006

AbstractThe effect of dry grinding of kaolin minerals by a mechanical mortar was examined by x-ray, thermal, and electron microscopic methods. Base exchange capacity and apparent density were also measured. In the early stage of grinding, kaolin crystals cleave and fracture and then split into fine crystals which are considered unit crystallites. Such crystallites gradually change to a disordered kaolin and partially decompose into a noncrystalline substance as grinding progresses. The crystalline and the noncrystalline substances promptly reaggregate and these reaggregated particles have a radial shape. After further grinding, the structure of the reaggregated particle seems to be zeolitic. Finally, the kaolin mineral thoroughly changes to a completely amorphous substance similar to a silica-alumina mixed gel. Consequently, the effect of dry grinding of kaolin is related to the degree of crystallinity of the original kaolin mineral.
Postdiagenetic Clay Mineral Environmental Relationships in the Gulf Coast Eocene
Authors: Burst J. F. 
Published: August 2006

AbstractAn extensive survey of clay mineral relationships in the subsurface Wilcox formation (Eocene) has shown progressive diagenetic conversions with depth. Montmorillonite, a common constituent of Wilcox outcrop material, becomes loss evident below 3000 ft and is not normally found in an unmixed state below the 9000—10,000 ft overburden level. At depths between 3000 and 14,000 ft, montmorillonite lattices are commonly interpersed with illite components, the frequency of which increases with depth to a virtual elimination of montmorillonite swelling characteristics below 14,000 ft.Chlorite is present at all stratigraphic levels including surface exposures. It appears to be a more dominant constituent at depth; however, observed increases in basal intensities in samples that had been more deeply buried may result from more perfect crystal development rather than quantitative differences.The diagenetic conversion of montmorillonite to illite and possibly to chlorite has resulted in a distribution of the last two minerals that is related to estimated depositional environments as reconstructed from micro-paleontological criteria in at least one well in southern Louisiana. It is inferred, therefore, that different chemical characteristics in the ancient Wilcox seas are responsible for the distribution coincidence even though the mineral groups defining the distribution were not necessarily indigenous to the ancient Wilcox sea.Correlations between clay minerals and environment are not particularly noted in the investigation of analogous environmental situations in Recent sediments, and it is thus concluded that the environment indicators which appear as minerals in lithified sediments such as the Wilcox are present in freshly deposited sediments in the form of submineralic chemical constituents such as absorbed ions, molecular groups or subcrystalline lattice configurations which are not detected by the ordinary clay mineral identification procedures. The change to mineralic form is aided by the natural “bombing” resulting from normal increases in temperature and pressure due to burial. The process is apparently a continuum through the entire subsurface residence of the sediment and the results are seemingly in accordance with phase equilibria.
Argillization in the Cochiti Mining District, New Mexico
Authors: Bundy Wayne M. , Murray Haydn H. 
Published: August 2006

AbstractVolcanic and intrusive rocks (mainly andesite and monzonite) of Tertiary age are associated with gold- and silver-bearing quartz veins. Hydrothermal alteration took place in two stages. The first and less intense alteration stage is associated with economic mineralization; metallization during the second and more intense stage is limited to pyrite.Alteration zones from the vein outward include: (1) dickite, (2) illite—kaolinite, (3) vermiculite—halloysite, and (4) chlorite—montmorillonite. Mixed-layer associations of 2:1 clay minerals are abundant and represent transitions between discrete clay minerals. Apparent occurrence of allophane in the illite-kaolinite zone indicates that amorphous aluminum silicates are intermediate phases in transitions from 2: 1 to 1: 1 clay minerals.Alteration of ferromagnesian minerals and plagioclase resulted largely in the formation of 2: 1 clay mineral types. Orthoclase is altered chiefly to illite and kaolinite. Dickite and quartz are end products of the most intense alteration in the area.Chemical analyses of the altered rocks in general show a decrease in basic ions toward the vein. Less significant changes are shown by acidic ions. Analyses of illites indicate that substitution of K by Na, Fe, Ca and Mg has taken place near the vein as shown by an overall decrease in KNa,KFe,KCa$\frac{K}{Na}, \frac{K}{Fe}, \frac{K}{Ca}$ and KMg$\frac{K}{Mg}$ ratios. Both sodium and potassium seem to be instrumental in the formation of well-developed illite crystals.Alteration stages operative in the Cochiti district were developed by the action of solutions probably ranging in pH from 4 to 10. Alteration zones were formed penecontemporaneously with gradual outward migration of the least intense zones.
Alteration of Micaceous Minerals by Sulfide Solutions
Authors: Weintraub Judy , Sand L. B. 
Published: August 2006

AbstractA mineralogical study by the Bureau of Mines and the University of Utah of the shale beds on the 1600 ft level of the Ophir Hill mine, Utah, disclosed that the micaceous minerals in the shale were altered as a function of proximity to the sulfide ore zones. The principal mineral in the shale distant from ore is 2M serieite. Within 100 ft along the bedding plane and 15 ft normal to the bedding plane, the serieite was altered successively to a modified form of serieite, two polymorphs of chlorite, and finally phlogopite.A general sequence of the mineral changes from barren to ore-bearing ground was: (I) serieite; (2) modified serieite; (3) modified serieite and 7Å chlorite; (4) modified serieite, 14Å chlorite, and phlogopite; (5) 14Å chlorite and phlogopite; and (6) phlogopite. This sequence of alteration of serieite in the shale was not noted in the mine areas barren of ore.
Halloysite Formed in a Calcareous Hot Spring Environment
Authors: Ames L. L. , Sand L. B. 
Published: August 2006

AbstractAn unusual halloysite deposit occurs on the west side of the Lake Mountains in Utah County, Utah. A field and laboratory study was made of this Fox deposit to determine the paragenesis of the clay minerals, especially halloysite. Successive lenses of unaltered tuff, partially altered tuff, clay and travertine beds, indicate that the clays have resulted from alteration of siliceous volcanic tuffs in a Tertiary (?) calcareous hot spring environment. Clay minerals identified were montmorillonite, kaolinite, halloysite·4H2O (endellite) and halloysite·2H20. Montmorillonite, which developed in a zone of less intensive silica leaching farthest from the hot spring vents, is the predominant clay mineral. Irregularly distributed pockets of halloysite and kaolinite developed nearest the hot spring vents in a high-calcium environment. In the clay, or associated with it, are calcite as travertine, quartz as rounded carbonate-corroded grains, feldspar, tridy- mite, biotite and glass.Experiments that approximate the chemical environment prevalent in the halloysite alteration zone were conducted on phase relations in part of the system lime—alumina- silica—water. Results suggest the formation of halloysite·4H2O in this kinetic system from intermediate calcium aluminate or calcium silicate hydrates with halloysite-type structures, or both.
Occurrences of Shales Partially Altered to Pyrophyllite
Authors: Ehlmann Arthur J. , Sand L. B. 
Published: August 2006

AbstractExamination of samples from shale outcrops on the periphery of the Utah Valley graben has revealed an unusual association of disseminated pyrophyllite with various clay minerals. Numerous samples were obtained from exposures in brick clay pits located in the Manning Canyon formation of Mississippian-Pennsylvanian age and from the Long Trail member of the Great Blue formation of Mississippian age. Associated clay minerals in these beds include illite, illite-montmorillonite mixed-layer clays, 7 Å chlorite, 14Å chlorite, kaolinite and sericite. Associated nonclay minerals include quartz, calcite, and small amounts of dolomite. Associated secondary minerals are calcite, aragonite, jarosite, gibbsite and gypsum.Three possible explanations of genesis have been considered in the present study: deposition of detrital pyrophyllite, surface weathering under special conditions, and hydrothermal or pneumatolytie activity. The third alternative explanation, hydrothermal or pneumatolytie activity, is believed to be the most acceptable. It is hypothesized that magnesium, iron, and interlayer cations have been removed from some of the original 2 : 1 layer clays in the shale by solutions localized along fault zones.
Effect of Sea-Water on Clay Minerals
Authors: Carroll Dorothy , Starkey Harry C. 
Published: August 2006

AbstractSamples of a montmorillonite, a mixed-layer mineral (mica and montmorillonite) “illite”, kaolinite, and halloysite were immersed in 50 ml sea-water for 10 days, and additional samples of the first three were immersed for 150 days. The exchangeable cations were determined both before and after treatment. It was found that Mg2+ ions from sea-water moved into the exchange positions in the minerals in preference to Ca2+ and Na+ ions. The H-form of these minerals showed a gradual adjustment to sea-water as measured by change in pH and filling of the exchange positions with cations other than H+. Kaolinite adjusted very rapidly, but montmorillonite and the mixed-layer mineral were slow. All the minerals reacted to yield appreciable amounts of SiO2, Al2O3, and Fe2O3 to the sea-water. The quantities yielded are in the order:montmorillonite > mixed-layer mineral > “illite” > kaolinite > halloysite The solubility is considered to be due to direct solution of SiO2 in the sea-water and to removal of Al2O3 from the octahedral layer of the minerals.When H-clays were titrated with sea-water three distinct kinds of curves were obtained: (a) kaolinite; (b) mixed-layer mineral, “illite,” and halloysite; and (c) montmorillonite. The curves are similar to those obtained with clay minerals titrated with other alkaline solutions. Kaolinite reacts somewhat like a number of simple acids, but the curves for the other minerals are more complex and are related to the neutralization of H and its replacement in the exchange sites by metallic cations. The exchangeable cations were determined in the minerals after titration, and the results are similar to those obtained after immersing the minerals in sea-water. The volume of sea-water required to reach an end point at about pH 7.6 varies from 11 ml for kaolinite to 135 ml for montmorillonite and is related to the titratable alkalinity of the sea water and to the exchange capacity of the minerals.
Clay Mineralogy of the Bottom Sediments, Rappahannock River, Virginia
Authors: Nelson Bruce W. 
Published: August 2006

AbstractBottom sediment clay mineral assemblages from the Rappahannock River and estuary contain kaolinite, illite, unorganized illite, dioctahedral vermiculite, 12.4Å montmorillonite, 14.2 Å montmorillonite, chlorite, feldspar and quartz. The x-ray diffraction characteristics of these species and their thermal modifications at 25–500°C are described and illustrated. Progressive changes in the mineralogical composition of bottom sediments occur between the fresh-water and saline-water portions of the Rappahannock system. Chlorite and feldspar occur exclusively in the saline portions of the estuary. Illite shows progressive increase in crystallization quality. There appears to be less kaolinite, proportionately, in the estuarine sediments of the most saline zone. x-Ray diffraction diagrams showing these progressive changes are illustrated.
Regional clay Mineral Patterns in the Gulf of Mexico
Authors: Pinsak Arthur P. , Murray Haydn H. 
Published: August 2006

AbstractA semiquantitative study of the surficial clay mineral distribution from 79 cores in the Recent sediments in the Gulf of Mexico shows a regional pattern which can be related to source and environment. The dominant factor controlling distribution of these surflcial sediments appears to be source. Montmorillonite is the most abundant clay mineral, and illite, chlorite, kaolinite and mixed-layer minerals are present in almost every sample.Alteration of the clay minerals is influenced by (a) change of environment, and (b) length of exposure. Initial ion exchange, which is caused by a tendency to reach equilibrium with a new environment, occurs so rapidly in the clay minerals after they enter the marine environment that rate of sedimentation is a minor factor in comparison to environmental change. Slow alteration and adjustment toward a stable end state are most complete in areas of slow deposition and extended exposure of the clay minerals to the environment.
Geology of the Clay Deposits in the Olive Hill District, Kentucky
Authors: Patterson Sam H. , Hosterman John W. 
Published: August 2006

AbstractTHE Olive Hill fire clay bed of Crider (1913) is the principal source of the raw material used in the refractory industry of eastern Kentucky. The bed is a discontinuous underclay from 1 to 20 ft above a prominent unconformity which separates Mississippian and Pennsylvanian rocks. Upper Mississippian rocks consist of ten marine limestone and shale units all truncated by the unconformity. Pennsylvanian rocks are chiefly: (a) massive deltaic sandstone; (b) cut-and-fill deposits of shale, siltstone and sandstone which contain several beds of coal and underclay including the Olive Hill fire clay of Crider (1913); and (c) dark-gray shale beds.The Olive Hill fire clay of Crider consists of approximately one-third flint clay, two-thirds semiflint clay, and minor amounts of plastic clay. The clay mineral content ranges from nearly pure kaolinite to kaolinitic clay containing about 40 percent illite and mixed-layer clay. The kaolinite ranges from highly crystalline to very poorly crystalline “fireclay” kaolinite. The degree of crystallinity of the kaolinite and hardness of the clay vary inversely with the amount of illite and mixed-layer clay present. The nearly pure kaolinite is believed to have formed by removal of silica and alkalies from mixtures of kaolinite, illite and mixed-layer clay by leaching shortly after deposition.An isopach map shows that Crider’s Olive Hill fire clay occurs in irregular, lens-shaped deposits. Fossil plant rootstocks with rootlets attached in the clay clearly indicate it supported plant growth. The overlying coal and presence of some organic material in the clay suggest that the Olive Hill fire clay was deposited under a reducing environment in swamps.
Clay Partings in Gypsum Deposits in Southwestern Indiana
Authors: Harrison Jack L. , Droste John B. 
Published: August 2006

AbstractGypsum deposits of Mississippian age in southwestern Indiana contain several argillaceous partings. A study of these partings was made to find out what clay minerals are present in such an evaporite association.The most abundant minerals in the clay partings are dolomite, gypsum, quartz, illite, chlorite and mixed-layer illite-montmorillonite. No kaolinite was found in any of the samples.
Time Factor and the Genesis of Soils on Early Wisconsin Till
Authors: Hensel D. R. , White Joe L. 
Published: August 2006

AbstractRadiocarbon dates indicate that the maximum time of weathering for soils of the Tazewell substage may be about 6400 years longer than that available for weathering of soils of the Cary substage.Detailed mineralogical and chemical studies were made of the 2–0.2 μ fractions of 0–6 in. and 30–36 in. samples from 24 sites along a traverse extending from the Cary substage across the Tazewell substage in east-central Indiana. The major clay mineral constituents of the 0–6 in. samples were illite and 14 Å material; illite and montmoril-lonite were the main components in the 30–36 in. samples. The correlation coefficients between illite content and percentage K2O for the 0–6 in. and 30–36 in. samples were 0.85 and 0.92, respectively.The end and terminal moraines of the Tazewell substage were found to have a higher illite content than the ground moraines. This was attributed to superglacial movement and enrichment of foreign materials, i.e. mica schists from the Canadian shield, on end and terminal moraines.The results of saturation of the clay fraction with potassium and magnesium on the proportion of 10Å, 12.7Å and 14Å spacings indicated that weathering had lowered the surface charge density of the micaceous minerals in the 0–6 in. samples to a greater extent than in the 30–36 in. samples. This effect, in addition to other weathering reactions, resulted in partially expanded micaceous minerals in the 0–6 in. samples which were much more resistant to collapse than were the minerals in the 30–36 in. samples.The rate of weathering of K2O from the 2–0.2μ fraction of the 0–6 in. samples located on ground moraines was estimated to be about 0.1 percent per 1000 years. This value was used in estimating the ages of the morainie systems of the Tazewell in Indiana. The estimated ages were as follows: Mississinewa, (radiocarbon date) 13,140 years; Union City, 14,500 years; Bloomington, 15,500 years; Champaign, 18,700 years; Shelbyville, (radiocarbon date) 19,500 years.The fertility status of the soils on the Tazewell has been influenced appreciably by the length of the weathering period, the potassium-supplying power of the soils decreasing with increasing age.
Review of the Relationships in the Montmorillonite Group of Clay Minerals
Authors: Ross Clarence S. 
Published: August 2006

AbstractSince the publication of the paper on the minerals of the montmorillonite group by Ross and Hendricks (1945) some species have been added to the group, and minor changes in the acceptable species have become advisable. No radical changes are proposed, but a review of the members and their grouping will be presented. The acceptable dioctahedral members of the group appear to be montmorillonite, nontronite and volchonskoite. Beidellite should be discontinued. The acceptable trioetahedral members of the group appear to include saponite, hectorite, sauconite, stevensite and medmontite. Griffithite is probably a useful term for an iron-rich saponite. Representative chemical analyses and formulas have been assembled to illustrate relationships.
A Discussion of the Water Content of Vermiculite
Authors: Bradley W. F. , Serratosa J. M. 
Published: August 2006

AbstractSelected chemical and diffraction analyses from the literature, supplemented by thermal and thermogravimetric analyses and infrared absorption observations, are utilized to construct a rational model of the water arrangement in natural vermiculites.A super cell is arranged by simple modification of the Hendricks water nets to accommodate the somewhat higher water contents, indicated by weight loss analyses, and the exchangeable cations.A three-cell unit (15.6 × 9 Å) contains two Mg2+·6H2O octahedra centered at the corners and face centers and four 4H2O squares centered about ±5.2 Å along a between the octahedra. The arrangement affords twenty hydrogen bonds near 2.75 Å, twelve between silicate and water layers and eight between water layers, and thirty-two hydrogen bonds near 3.0 Å within water layers. The remaining four hydrogens are not active in the bonding system. The environment of each water molecule is a distorted tetrahedron.A broad infrared absorption band shows maxima at about 3600, 3450 and 3350 cm−1 at normal incidence, with increased activity in the highest and lowest energies when a flake is tilted. It is concluded that OH axes in the shortest bonds are more inclined to the cleavage planes than are the intermediate length axes.
Some Aspects of the Mineralogy of the Northern Atlantic Coastal Plain
Authors: Groot Johan J. , Glass Herbert D. 
Published: August 2006

AbstractStudies of the mineralogy of the northern part of the Atlantic Coastal Plain indicate that the heavy mineral content of the Cretaceous and Cenozoic sediments consists basically of two suites, a restricted mineral suite characterized by very stable minerals, and a full suite consisting of a great variety of igneous and metamorphic minerals. The restricted suite occurs in the nonmarine sediments and the full suite in the marine deposits.The nonmarine Cretaceous deposits consist of kaolinite, with variable amounts of illite and its alteration products. Transition sediments like those of the Magothy formation contain kaolinite, illite, chloritic material and, occasionally, some montmorillonite. The marine sediments are characterized primarily by illite and montmorillonite. Thus, a limited heavy mineral suite and kaolinite are associated in nonmarine deposits, and a full suite and montmorillonite are found in marine sediments.On the basis of available data the conclusion is reached that the different heavy mineral and clay mineral suites are a result of different source areas for the marine and non-marine sediments.The suggestion is made that the formational concept cannot be employed with regard to the nonmarine sediments of the northern Coastal Plain but that, instead, a new concept be adopted based on depositional conditions within the framework of the control of the heavy and clay mineral assemblages.
Geology of the Clay Deposits in Parts of Washington and Idaho
Authors: Hosterman John W. 
Published: August 2006

AbstractThe clay deposits of eastern Washington and northern Idaho are along the eastern edge of the Columbia River Plateau physiographic province. Three types of clay occur in the area: (a) residual clay derived from the Columbia River basalt of Tertiary age; (b) residual clay derived from the Cretaceous granodiorite and related intrusive rocks of the Idaho batholith; and (c) transported clay. The two types of residual clay were formed during a protracted lull in the outpouring of the Columbia River basalt, when the relief of land surface was low to moderate and the climate was warm and humid. The topography and climate during this interval were probably ideal for leaching and oxidation. The transported clay is chiefly a product of the weathered granodiorite and related intrusive rocks. Most of it accumulated in basins formed by damming of streams by basalt flows.Kaolinite and halloysite are the principal clay minerals found in the area. The residual clay derived from basalt is chiefly composed of halloysite. Most of this clay is colored blue, gray or grayish black by finely disseminated ilmenite and locally it is stained blown by limonite; most of it has a relict basaltic texture.The residual clay derived from granodiorite and related intrusive rocks contains both kaolinite and halloysite, and the transported clay is predominantly kaolinite. Both of these clays are white and contain abundant quartz grains and mica flakes. The residual clay has a relict granitic texture, and the transported clay has a well-developed bedding and is interbedded with elastic material.