Thesis (Ph. D.)--University of Wisconsin--Madison, 1968. / Typescript. Vita. eContent provider-neutral record in process. Description based on print version record. Includes bibliographical references.

The salient points of the thesis are summarised as follows. 1. The first chapter is essentially a review of chemical and mineralogical transformations accompanying the weathering of some primary rock forming minerals, and includes a discussion of feldspars, trioctahedral and dioctahedral mica, quartz, chalcedony, opal, metamorphic, accessory, and opaque minerals, and ferromagnesian minerals. Included therein is a hypothesis for the mechanism of formation and layered structure of hydrobiotite. 2. A brief review of the geology, geomorphology, <and age of weathering in north east Scotland is presented in chapter 2. 3. The geology, field work and laboratory investigations of the weathe~ing in a meta-sediment, a quartz-mica-schist, and the Tertiary gravels at two sites, are presented in chapters 4, 5, 6 and 7 respectively. Some features found are considered to be relic, and formed under previous conditions. The weathering products include 2:1 type and kaolin minerals. 4. Secondary silica in a minute form was found to be common and is referred to as "aphanitic silica". The main optical properties and occurrence have been noted. 5. Secondary deposits of Ti02 (leucoxene) are also common, and because of the great opacity of Ti02, may be very ;caospicuous in thin sections even though actual concentrations are very low. Some of the leucoxene is shown to contain rutile and anatase. The source of much Ti02 may be biotite, and very rarely Ti02 may apparently completely pseudomorph biotite. 6. A comparison of the kaolin minerals (poorly ordered kaolinite, well-crystallised kaolin'ijte,and halloysite) from some sites has been made by a variety of techniques including thin sections, X-ray diffraction, DTA, infrared spectroscopy, chemical intercalation, and electron microscopy. Some problems in the study of these clays are considered, particularly with respect to monomineralic and polymineralic mixtures. It is concluded that there are fundamental differences between the structures of kaolinne and halloysite, other than the occurrence of interlayer water in the natural state of halloysiteamphiboles and pyroxenes (generally), tremo1ite-actino1ite, and accessory minerals in the weathered materials is discussed and summarised. 8. The age of weathering and the contribution of weathering products to contempotary soils is assessed from a consideration of the evidence found and that available. It is concluded that in north east Scotland contemporary weathering has very little effect upon weathered rocks beneath soils

The Statfjord Formation, reaching a maximum thickness of 1,000 ft in the Brent Field area, comprises a highly heterolithic alluvial sandstone, siltstone, shale and mudstone succession (the Eriksson and Raude Member). The uppermost Statfjord Formation is, however, made up of a thin succession of medium-coarse grained shallow marine sandstones (Nansen Member). Analysis of material from 11 cored wells, and wireline log suites from a further 61 non-cored wells has revealed a distinct pattern of "sequence" development which is present throughout the Statfjord Formation of the Brent Field. A sparsely preserved fossil assemblage (pollen spores etc. ) has precluded biostratigraphic correlation of the main Statfjord Formation fluvial suite. Furthermore, the positions of lithostratigraphic markers (e. g. the base of the Nansen Member) within a sedimentary succession frequently reflect variations in the spatial development of facies, rather than chronostratigraphically equivalent events. Thus, if derived from purely lithostratigraphically driven correlation, the reservoir geologists' perception of parameters essential for flow unit designation prior to field simulation studies (e. g. sandbody connectivity), are often poorly constrained. Palaeosols are abundant within the fluvial Statfjord Formation succession, where they can be readily recognised in core. The palaeosol development is controlled by parent material, climate, biological factor, topography and time. The Statfjord Formation palaeosols are classified into five groups in terms of soil maturity. Understanding of wireline log (i. e. GR, Sonic and CNL) responses of different palaeosols allows identification of the Statfjord Formation palaeosols in non-cored wells. Whole rock geochemical analyses reveal variations between different types of Statfjord Formation palaeosols, however it is difficult to distinguish the five groups of palaeosols purely on the basis of chemical compositional variations because the palaeosols were complicated by mixed parent material. This study has also resulted in subdivision and correlation of the fluvial Statfjord Formation reservoir in the Brent Field into a series of reservoir units which are identified on the basis of their petrophysical and geochemical characteristics. Reservoir units are sequences which have distinctive geochemical compositions, and are recognisable on the basis of their petrophysical log response using a "Formation Lithology Factor" (FLF, defined by this study) based upon variations in sonic and compensated neutron log responses. Variations in geochemical composition are interpreted as reflecting varying amounts of sediment input from different provenances. Variations in FLF for both sandstone and mudstone lithotypes can be used to define reservoir units. This simple and novel technique may be applied to other sandstone suites in understanding reservoir connectivity and flow unit definition. High resolution reservoir correlation using palaeosols has allowed the interpretation of reservoir sandstone interconnectivity within the Statfjord Formation. The successful application of the pedofacies model (Bown and Kraus, 1987) and pedofacies sequences (Kraus, 1987) identified in the Statfjord Formation of the Brent Field has proved that they can be applied to a wide rane of fluvial deposits. In summary, this study has applied a multidisciplinary approach to the problem of correlation using palaeosols as potential indicators of "channel proximity" within a floodbasin. Using these, together with petrophysical, chemostratigraphic, heavy mineral data and field production data has allowed an integrated novel approach to be used in the interpretation of reservoir sandstone interconnectedness.

No description available.

Palynological and stratigraphic investigations have been conducted on sediment cores for three sites in Lothian Region, Scotland: Balgone House, Broxmouth and Corstorphine. All phases of the Lateglacial period, as far as they are manifested in the Lothians at the sites studied, have been investigated with particular reference to the Younger Dryas, the main Interstadial, or Allerod, and also the evidence for the colder conditions that preceded it which are presumed to represent Older Dryas-type vegetation. Further light has been cast on the development of the Postglacial broad - leaved forests. The Cambridge computer program POLLDATA MKV was used to perform the necessary calculations and controlled a graph plotter to generate pollen diagrams. A series of subroutines is described that translated the calls to the Cambridge graphics subroutine library. This may serve as a model for other installations. Objective numerical zonation methods are applied to the pollen data. These methods are used not only to zone the pollen series but also to aid in the generation of hypotheses regarding vegetation changes. Chemical analyses of the sediments from Balgone House were undertaken. The results obtained are at variance with those from published work and it is proposed that the reason is that the chemical pre-treatment of samples employed locally may be less efficient in leaching the cations from the mineral fraction.

No description available.

Palaeosol development is controlled by topography, drainage, substrate, climate and time. The types and maturities of soil developing within fluvial systems are also controlled by avulsion and terracing. Soil forming models relate variations in pedogenic maturity and morphology to these processes. The pedofacies model and pedofacies sequences apply to lateral and vertical packages deposited under aggradational conditions while the chronosequence model applies across floodplain terraces. The Upper Triassic, Upper Petrified Forest Member, Arizona contains fluvial channel sandstones encased in thick mudstones. Differences in palaeosol development were produced by variations in sedimentation rate, terracing and drainage conditions. The pedofacies and chronosequence models apply to these palaeosols. The Owl Rock member was deposited in lacustrine and lacustrine margin environments. Soil forming models were not recognised here because pedogenic horizons were subject to intense burrowing and reworking by advancing lacustrine margins. Continued basin subsidence and decreasing sediment supply caused the change in depositional environments between the two Members. The Upper Silurian, Old Red Sandstone, Dyfed comprises thick fluvial deposits and numerous stacked palaeosols. Fluvial architecture and palaeosol development was controlled by avulsion, phases of erosion and influxes of volcanic ash. Channel morphologies were broad and sheet-like. Soil morphology and structure reveals complex cycles of varying aggradation and erosion within the sediments. Palaeosols contain variations in maturity consistent with the pedofacies relationship and pedofacies sequences. Upper Triassic to Lower Jurassic Lunde and Statfjord Formations, Snorre Field, North Sea comprise fluvial channels which change from isolated ribbons encased in thick mudstones to laterally extensive channels and palaeosol development decreases from moderate to poor. Regional changes in climate and basin configuration controlled the evolution of the fluvial regime and patterns of pedogenic maturity were not apparent.

Thesis (M.Sc.) --University of Adelaide. / Typewritten copy.

Habilitationsschrift--Würzburg. / Summary also in English. Bibliography: p. 190-201.

Habilitationsschrift--Würzburg. / Summary also in English. Bibliography: p. 190-201.