Magmatology of Mt. Pelée (Martinique, F.W.I.). III: Fractional crystallization versus magma mixing

Fichaut, Michèle; Maury, René C.; Traineau, Hervé; Westercamp, D.; Joron, Jean Louis; Gourgaud, Alain; Coulon, Christian

doi:10.1016/0377-0273(89)90037-1

Cited by 23 publications

(37 citation statements)

References 14 publications

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“…The parameters input in the program are the geometry of intrusions as illustrated in Figure 2, their thickness and diameter, the ratio of eruption over intrusion r , the liquidus and solidus temperatures of the magma, and the critical volume of the magma chamber that is not allowed to cool below 875°C. We take a critical volume of 0.3 km 3 that corresponds to the average eruption volume [ Fichaut et al , 1989]. The simulation begins with the emplacement of a first intrusion.…”

Section: Methodsmentioning

confidence: 99%

“…The second cycle lasted from 40,000 to ∼19,500 years BP and is characterized by the emission of predominantly basaltic andesites. After a gap in the activity of 6000 years, the current cycle started ∼13,500 years ago and erupted plinian and pelean products of mostly silicic andesite composition [ Fichaut et al , 1989]. Fichaut et al [1989] identified 34 eruptions for this cycle and estimated the volume per eruption at 0.1–0.5 km 3 .…”

Section: Geological Backgroundmentioning

confidence: 99%

“…After a gap in the activity of 6000 years, the current cycle started ∼13,500 years ago and erupted plinian and pelean products of mostly silicic andesite composition [ Fichaut et al , 1989]. Fichaut et al [1989] identified 34 eruptions for this cycle and estimated the volume per eruption at 0.1–0.5 km 3 . This last 13,500 years long cycle is characterized by a remarkable homogeneity in the composition of emitted products, which suggests that the physical state of the magma chamber did not vary appreciably before each eruption.…”

Section: Geological Backgroundmentioning

confidence: 99%

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Conditions for the growth of a long‐lived shallow crustal magma chamber below Mount Pelee volcano (Martinique, Lesser Antilles Arc)

Annen¹,

Pichavant²,

Bachmann³

et al. 2008

J. Geophys. Res.

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[1] The compositional homogeneity of silicic andesites emitted during the 13,500-year-long last eruptive cycle of Mount Pelee suggests that the physical state of the magma chamber was largely unmodified during this period. Experimental phase equilibria on Mount Pelee recent products indicate that pre-eruptive magma temperatures and pressures were in the range of 875-900°C and 2 ± 0.5 kbar, respectively. The estimated average eruption rate was 7.5 Â 10 À4 km 3 /a with an average volume of about 0.3 km 3 per eruption. An analytical model for a spherical magma chamber indicates that a magma flux of 4-5 Â 10 À4 km 3 /a can maintain a magma chamber of 0.3 km 3 above 875°C below Mount Pelee. However, observations of plutons suggest that magma chambers may grow by addition of sheet-like intrusions. With numerical simulation we show that a minimum sheet accretion rate of a few centimeters per year is required to grow a persistently active magma chamber independently of the intruded volumetric flux. This minimum injection rate is higher if the heat transfer is enhanced by convection processes. The limited ability of an arc crust to extend and accommodate dikes suggests that magma injections are sills or, if they are dikes, that most of the volume injected in the magma chamber is eventually erupted. In a conductively cooling igneous body formed by sills injected at a rate of a few centimeters per year, most of the injected magma completely solidifies and only a small part of the body (about 10-20%) is above 875°C and able to feed eruptions.

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Section: Methodsmentioning

confidence: 99%

Section: Geological Backgroundmentioning

confidence: 99%

Section: Geological Backgroundmentioning

confidence: 99%

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Conditions for the growth of a long‐lived shallow crustal magma chamber below Mount Pelee volcano (Martinique, Lesser Antilles Arc)

Annen¹,

Pichavant²,

Bachmann³

et al. 2008

J. Geophys. Res.

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“…That study identified more than 40 tephra layers in the last 35 kyr in a deep‐sea sediment core located 50 km northwest and downwind of Mont Pelée [ Boudon et al , ]. Fichaut et al [] estimated an average volume per eruption of 0.1 to 0.3 km 3 for the past 13,500 years B.P., which led Annen et al [] to suggest an average eruption rate of 0.75 km 3 /kyr for this period. In historical times, two phreatic eruptions took place in 1792 and 1851 and two magmatic eruptions occurred in 1902–1904 and 1929–1932.…”

Section: Regional Settingmentioning

confidence: 99%

Construction and destruction of Mont Pelée volcano: Volumes and rates constrained from a geomorphological model of evolution

2015

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This study presents long-term volumes and construction rates for the Mont Conil-Mont Pelée volcano and rate estimates at which volcanic activity creates relief. An algorithm, ShapeVolc, is used to numerically model topographic surfaces. Volcano morphology is analyzed using current digital elevation model in combination with mapped geology to produce 10 paleotopographies at the end of four constructional stages and three destructional events. , and 3.5 km 3 , thus about 37% of the total constructed volume. Integrated over the volcano's lifetime, the rate at which flank collapses removed material off the island is 0.15 km 3 /kyr. In contrast, long-term erosion rates outside collapsed areas are estimated at about 0.05 ± 0.7 km 3 /kyr, or~11 km 3 of material removed. This latter rate is not negligible, which strengthens the importance of taking into account recurrent small erosional events on the geomorphological evolution of a volcanic island in a tropical context.

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“…It has also been established that the basaltic magmas are 615 parental to the andesites via magma mixing and fractional crystallization (Fichaut et al, 1989b). We have also shown that the Phase I andesite plagioclase microlite population has elevated Fe contents 660 similar to the enclave plagioclase and the andesite microlites from subsequent phases (Table 4, Figure 661 1e), which suggests that disaggregation probably did occur during Phase I.…”

mentioning

confidence: 58%

Chapter 17 Petrological and geochemical variation during the Soufrière Hills eruption, 1995 to 2010

Christopher

Humphreys

Barclay

et al. 2014

Memoirs

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Citation for published item:ghristopherD F nd rumphreysD wFgFF nd frlyD tF nd qenreuD uF nd he engelisD FwFrF nd lilD wF nd honovnD eF @PHIRA 9etrologil nd geohemil vrition during the oufri ere rills eruptionD IWWS to PHIHF9D wemoirsFD QW F ppF QIUEQRPF Further information on publisher's website: he iruption of oufri ere rills olnoD wontserrt from PHHH to PHIHF ghpter IUF Use policyThe full-text may be used and/or reproduced, and given to third parties in any format or medium, without prior permission or charge, for personal research or study, educational, or not-for-prot purposes provided that:• a full bibliographic reference is made to the original source • a link is made to the metadata record in DRO • the full-text is not changed in any way The full-text must not be sold in any format or medium without the formal permission of the copyright holders.Please consult the full DRO policy for further details. ABSTRACT 22The andesite lava erupted at the Soufrière Hills Volcano is crystal rich with 33-63% phenocrysts, of 23 plagioclase (65%); amphibole (28%), orthopyroxene (7%) and minor Fe-Ti oxide and clinopyroxene 24 microphenocrysts. The andesite hosts mafic enclaves which have similar mineral phases to the andesite. 25The enclaves are generally crystal poor but can have up to 27% of inherited phenocrysts from the 26 andesite, the majority of which are plagioclase. The eruption is defined by discrete periods of extrusion 27 called phases, separated by pauses. The enclaves exhibit bulk geochemical trends that are consistent with 28 fractionation. We infer that the intruded mafic liquids of Phases I and II interacted and assimilated 29 plutonic residue remaining from the multiple prior mafic intrusions, while the basaltic liquids from Phases 30 III and V assimilated relatively little material. We also infer a change in the basaltic composition coming 31 from depth. The bulk Fe contents of both magma types are coupled and they both show a systematic inter-32 phase variation in Fe content. We interpret the coupled Fe variation to be due to contamination of the 33 andesite from the intruding basalt via diffusion and advection processes, resulting in the erupted andesite 34 products bearing the geochemical imprint of the syn-eruptive enclaves. 35 36The Soufrière Hills volcano is an andesitic dome complex located on the island of Montserrat in the 37Lesser Antilles arc. The present eruption began on the evening of July 18 th 1995 with ash venting 38 followed by phreatic explosions over the next weeks and months Robertson et al., 39 2000). Juvenile material arrived at the surface around November 15 th 1995 (Herd et al., 2005). The volcanic activity of Phase I is described in detail 49elsewhere (e.g. Miller et al., 1998;Calder et al., 2002; Norton et 50 al., 2002) (Herd et al., 2005). This resulted in the construction 55 of a larger volume dome than any extruded during Phase I. Dome collapses were less frequent than during 56Phase I but involved larger volumes, culminating in the largest volume collapse of the...

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Magmatology of Mt. Pelée (Martinique, F.W.I.). III: Fractional crystallization versus magma mixing

Cited by 23 publications

References 14 publications

Conditions for the growth of a long‐lived shallow crustal magma chamber below Mount Pelee volcano (Martinique, Lesser Antilles Arc)

Conditions for the growth of a long‐lived shallow crustal magma chamber below Mount Pelee volcano (Martinique, Lesser Antilles Arc)

Construction and destruction of Mont Pelée volcano: Volumes and rates constrained from a geomorphological model of evolution

Chapter 17 Petrological and geochemical variation during the Soufrière Hills eruption, 1995 to 2010

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