Crystal settling in sills: A model for suspension settling

Gray, Norman H.; Crain, I. K.

doi:10.1139/e69-122

Cited by 23 publications

(13 citation statements)

References 2 publications

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“…They compared their results to observations at Shonkin Sag, but due to a misnumbered sample the calculated profile did not match that observed. The production of S-shaped profiles was analyzed again by Gray and Crain (1969) and Fuijii (1974). They were taken to task for this point of view by Walker (1956) and Hess (1956) who could not understand Jaeger's straightforward analysis.…”

Section: Historical Note On Solidification Front Fractionationmentioning

confidence: 99%

Magmatism, Magma, and Magma Chambers

Marsh

2007

Treatise on Geophysics

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Section: Historical Note On Solidification Front Fractionationmentioning

confidence: 99%

Magmatism, Magma, and Magma Chambers

Marsh

2007

Treatise on Geophysics

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“…The first quantification of this process was by Osborne and Roberts (1931). Since that time the mechanism has been repeatedly rediscovered by Jaeger and Joplin (1955), Gray and Crain (1969), Fujii (1974), and Marsh (1988a), and its effects have been noted in a great number of sills (Mangan and Marsh, 1992).…”

Section: Dynamics Of Solidification Frontsmentioning

confidence: 99%

Solidification fronts and magmatic evolution

1996

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From (3. F. Becker's and L. V. Pirsson's early enunciations linking the dynamics of magma chambers to the rock records of sills and plutons to this day, two features stand at the centre of nearly every magmatic process: solidification fronts and phenocrysts. The structure and behaviour of the envisioned solidification front, however, has been mostly that akin to non-silicate, non-multiply-saturated systems, which has led to confusion in appreciating its role in magmatic evolution. The common habit of intruding magmas to carry significant amounts of phenocrysts, which can lead to efficient ffactionation, layering, and interstitial melt flow within extensive mush piles, when coupled with solidification fronts, allows a broad understanding of the processes leading to the rock records of sills and lava lakes. These same processes are fundamental to understanding all magmas.The spatial manifestation of the liquidus and solidus is the Solidification Front (SF); all magmas, stationary or in transit, are encased by SFs. In the ideal case of an initially crystal-free, cooling magma, crystallinity increases from nucleation on the leading liquidus edge to a holocrystalline rock at the trailing solidus. The package of SF isotherms advances inward, thickening with time and, depending on location --roof, floor, or walls --and the initial crystallinity of the magma, is instrumental in controlling magmatic evolution. Bimodal volcanism as well as much of the structure of the oceanic crust may arise from the behaviour of SFs.In mafic magmas, somewhere near a crystallinity (N) of 55% (vol), depending on the phase assemblage, the SF changes from a viscous fluid (suspension (0

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“…However, with the exception of brief discussions in Jaeger's 1964 and papers, and a recent paper by Gray and Crain (1969), these studies were essentially concerned with intrusions in which crystal settling was not appreciable. Gray and Crain gave a model that predicts the distribution of settled crystals in a sill where the crystals were initially carried as a uniform suspension in the magma.…”

Section: Introductionmentioning

confidence: 99%

Heat transfer during solidification of layered intrusions. I. Sheets and sills

Irvine¹

1970

Can. J. Earth Sci.

130

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With the advent of crystal settling in a solidifying igneous intrusion, the roof contact of the intrusion may be continuously subjected to temperatures approaching those of the magma itself. This causes steeper temperature gradients in the roof rocks and, consequently, more rapid heat loss and solidification than would occur if the crystals were frozen to the roof. By contrast, the accumulation of crystals in the lower parts of the intrusion acts to lower the floor contact temperature and so reduces temperature gradients in the floor rocks; but since the proportion of liquid near the floor is reduced, the overall effect also is to speed solidification, specifically in this case, from the floor upwards. The present paper reviews in a qualitative way the relation between crystallization mechanisms and temperature in a magma body when crystal fractionation is a major process. It then examines quantitatively, by means of one-dimensional solutions of the heat flow equation, the influence on crystal accumulation rates and roof rock temperatures of ( a ) variations in magma temperature, (b) pre-intrusion temperature gradients in the roof rocks, (c) shallow emplacement, ( d ) formation of an upper border zone or floating of crystals, and (e) latent heat effects associated with contact metamorphism. Finally, it considers the effects of heat loss to the floor rocks on ( i ) crystallization in the magma above the accumulating pile of crystals, (ii) solidification of trapped pore magma, and (iii) contact metamorphism of the floor rocks. Some of the more important equations presented also apply to sills, sheets, and dikes showing no crystal fractionation.

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Crystal settling in sills: A model for suspension settling

Cited by 23 publications

References 2 publications

Magmatism, Magma, and Magma Chambers

Magmatism, Magma, and Magma Chambers

Solidification fronts and magmatic evolution

Heat transfer during solidification of layered intrusions. I. Sheets and sills

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