Halloysite and Gibbsite Formation in Hawaii

Bates, Thomas F.

doi:10.1016/b978-1-4831-9842-2.50022-5

Cited by 44 publications

(37 citation statements)

References 7 publications

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“…Gibbsite dominated the clay mineralogy in much wetter climates, with kaolinite representing a transition between the two. A similar study (Bates, 1960) on clays developed on Hawaiian basalt as a function of drainage and precipitation yielded the same results; smectite developed on the dry side of the islands while gibbsite formed in mountainous regions with heavy rainfall.…”

Section: Water Availability During Depositionsupporting

confidence: 59%

Juvenile chemical sediments and the long term persistence of water at the surface of Mars

Tosca

Knoll

2009

Earth and Planetary Science Letters

136

124

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Chemical sediments and the aqueous alteration products of volcanic rocks clearly indicate the presence of water, at least episodically, at the martian surface. Compared to similar materials formed on the early Earth, however, martian deposits are juvenile, or diagenetically under-developed. Here we examine the role of water in facilitating various diagenetic reactions and evaluate the predicted effects of time and temperature for aqueous diagenesis on Mars.Using kinetic formulations based on terrestrial sedimentary geology, we quantify the integrated effects of time and temperature for a range of possible burial and thermal histories of precipitated minerals on Mars. From this, we estimate thresholds beyond which these precipitates should have been converted to the point of non-detection in the presence of water. Surface water has been shown to be at least episodically present in recent times. Nonetheless, the integrated duration of aqueous activity recorded over geologically long intervals by hydrated amorphous silica, smectite clays and Fe-sulfate minerals suggest that where these minerals occur water did not persist much beyond their initial deposition. This geochemical conclusion converges with geomorphologic studies that suggest water limitation during the late Noachian-Hesperian peak of potentially habitable environments on Mars should address the timescales on which liquid water has persisted and the timing of aqueous episodes relative to major planetary events.

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Section: Water Availability During Depositionsupporting

confidence: 59%

Juvenile chemical sediments and the long term persistence of water at the surface of Mars

Tosca

Knoll

2009

Earth and Planetary Science Letters

136

124

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“…Soils formed on the island of Hawaii, where surface basalts range in age from 0 to 500,000 yr (Clague and Dalrymple, 1987), are dominated by smectite or semi-amorphous materials such as imogolite or allophane (Foote et al, 1972). They may contain significant amounts of halloysite (Sato et al, 1973;Bates, 1962;Parfitt et al, 1988;Wada and Wada, 1976). Even where rainfall is greater than 1000 mm/yr (on the windward side of the island) and the soil has formed from ash, there are no soils on Hawaii Island that are classified in the kaolinitic mineral family (Foote et al, 1972).…”

Section: Younger Laterite-derivative Facies and Their Paleoclimatic Imentioning

confidence: 99%

Alteration of uppermost lavas and volcaniclastics recovered during Leg 152 to the East Greenland Margin

Holmes¹

1998

Proceedings of the Ocean Drilling Program

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During the last stages of the eruption of syn-rift basalts along the East Greenland Margin, debris flows and/or pyroclastic deposits were emplaced at Ocean Drilling Program Sites 915 and 916. The deposits and the tops of the lava flows at Site 918 were altered by subaerial weathering processes as indicated by downhole changes in mineral and chemical composition, and by the mineral paragenesis. Kaolinite and goethite, which form in acidic waters, are abundant at the tops of the weathering profiles and decrease in abundance downward. They are replaced by a smectite-hematite-opal assemblage at the bases of the weathered profiles. Gibbsite is a minor component in the upper parts of the profiles. Good preservation of parent structure and stratification indicate that only the bases of paleosols are preserved at all sites. The upper parts were probably eroded when these sites subsided below sea level.Abundant gibbsite in marine sediment overlying the paleosols and of middle to late Eocene age is probably derived from the erosion of highly weathered soils formed in a subtropical to tropical climate. A highly weathered basaltic terrane supplied abundant iron oxides in addition to gibbsite, kaolinite, illite/mica, and quartz through fluvially dominated deltaic systems on the shelf through at least the late Eocene. Only small amounts of sediment spilled over into the adjacent Irminger Basin through the Eocene, as indicated by the presence of felsic terrane-derived minerals (quartz, illite, and/or mica). Sedimentation rates were low enough in the Irminger Basin to allow Mn oxide crusts to develop until quartzose turbidites spilled over in the late Oligocene. Gibbsite was not detected in sediment of early Oligocene age and younger, suggesting a regional cooling, increased aridity, and/or leveling of the source area at this time.

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“…The processes of origin of high-alumina minerals, based on first-hand observations and studies in particular districts, have been well documented in a number of papers (Mead, 1915;Harrison, 1933;Harder, 1952;Bolger and Weitz, 1952;Gordon and Tracey, 1952;and with Ellis, 1958;Bardossy, 1959;and Bates, 1962;and others). The purpose of this discussion is, not to try to improve on those excellent papers, but to find from them, plus some personal observations, common denominators of processes of origin for high-alumina minerals.…”

Section: Introductionmentioning

confidence: 99%

The Origin of High-Alumina Clay Minerals—A Review

Keller

1963

Clays clay miner. (Natl. Conf. Clays Clay Miner.)

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High-alumina minerals refer, in this paper, to Al-rich, normal sedimentary phases, including gibbsite, boehmite, diaspore, possibly "proto-diaspore" and "proto-alunite", "Al-chlorite", and corundum, in association with kaolin minerals. They may be derived from any common Al-containing rock. Processes of origin include direct bauxitization of non-clay silicate minerals and rocks, and the desilication of any of the common clay minerals, particularly of the kaolin group. Apparently aluminous gels were formed within certain marshy basins, and/or were transported into basins, giving rise to concretionary masses of high-alumina minerals. Concretionary deposits were iormed by dissolution of A1 and reprecipitation.Alumina is probably more soluble, inherently, than is interpreted from geologic occurrences. Even after A1 is dissolved under appropriate pH, or complexing reactions, its solubility is obscured by Al-immobilization through fixation within 3-layer clay minerals, or absorbed by other phases. A 14~ phase, probably aluminous, is not uncommon in certain soils, and in flint and boehmite-diaspore-containing clays. Subtraction of silica by plants, is accompanied by concentration of alumina.

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Halloysite and Gibbsite Formation in Hawaii

Cited by 44 publications

References 7 publications

Juvenile chemical sediments and the long term persistence of water at the surface of Mars

Juvenile chemical sediments and the long term persistence of water at the surface of Mars

Alteration of uppermost lavas and volcaniclastics recovered during Leg 152 to the East Greenland Margin

The Origin of High-Alumina Clay Minerals—A Review

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