A model for eruption frequency of upper crustal silicic magma chambers

Degruyter, Wim; Huber, Christian

doi:10.1016/j.epsl.2014.06.047

Cited by 115 publications

(211 citation statements)

References 55 publications

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“…In order to focus on the entire crustal section, we neglect smaller-scale processes such as melt/gas extraction and thermo-mechanical feedbacks between the crust and the magma body during recharge 46,68 . We assume that the heat transfer is conductive and neglect the effects of shallow level hydrothermal circulation and internal magma chamber convection.…”

Section: Methodsmentioning

confidence: 99%

Lifetime and size of shallow magma bodies controlled by crustal-scale magmatism

et al. 2017

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Section: Methodsmentioning

confidence: 99%

Lifetime and size of shallow magma bodies controlled by crustal-scale magmatism

et al. 2017

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“…All the hypotheses proposed for the Vesuvius Plinian eruptions are considered to explain the magma chamber evolution up to the triggering of the eruption: (I) fractional crystallisation and an increase in volatiles pressure leading to magma chamber wall breakage [6], (II) limestone Assimilation and Fractional Crystallisation (AFC) with con-25 sequent explosion [7], (III) feeder dyke formation with the injection of fresh hot magma in the plumbing system and consequent destabilisation of the chamber [8,9]; (IV) a combination of the above mechanisms [10].…”

Section: Introductionmentioning

confidence: 99%

Magma evolution inside the 1631 Vesuvius magma chamber and eruption triggering

et al. 2017

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Vesuvius is a high-risk volcano and the 1631 Plinian eruption is a reference event for the next episode of explosive unrest. A complete stratigraphic and petrographic description of 1631 pyroclastics is given in this study. During the 1631 eruption a phonolite was firstly erupted followed by a tephritic phonolite and finally a phonolitic tephrite, indicating a layered magma chamber. We suggest that phonolitic basanite is a good candidate to be the primitive parental-melt of the 1631 eruption. Composition of apatite from the 1631 pyroclastics is different from those of CO 2 -rich melts indicating negligible CO 2 content during magma evolution. Cross checking calculations, using PETROGRAPH and PELE software, accounts for multistage evolution up to phonolite starting from a phonolitic basanite melt similar to the Vesuvius medieval lavas. The model implies crystal settling of clinopyroxene and olivine at 6 kbar and 1220 ∘ C, clinopyroxene plus leucite at a pressure ranging from 2.5 to 0.5 kbar and temperature ranging from 1140 to 940 ∘ C. Inside the phonolitic magma chamber K-feldspar and leucite would coexist at a temperature ranging from from 940 to 840 ∘ C and at a pressure ranging from 2.5 to 0.5 kbar. Thus crystal fractionation is certainly a necessary and probably a sufficient condition to evolve the melt from phono tephritic to phonolitic in the 1631 magma chamber. We speculate that phonolitic tephrite magma refilling from deeper levels destabilised the chamber and triggered the eruption, as testified by the seismic precursor phenomena before 1631 unrest.

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“…In this subsection, we suggest how the present study can be connected to a regime of magmatic eruptions trigerred by buoyancy, as identified in Degruyter & Huber (2014). The mush, i.e.…”

Section: A3 a Possible Link With Buoyancy Induced Volcanic Mush Desmentioning

confidence: 99%

“…The mush can be destabilized (or not) by several mechanisms: mass injection, second boiling, buoyancy. In Degruyter & Huber (2014) (Fig. 6, page 126), a four-region regime diagram for magmatic eruptions, including these mechanisms and depending on three caracteristic timescales, is proposed.…”

Section: A3 a Possible Link With Buoyancy Induced Volcanic Mush Desmentioning

confidence: 99%

“…Also note that some of the adopted simplifying assumptions on the temperature profiles were quantitatively confirmed by preliminary multi-dimensional conductive heat transfer simulations, which are shown in the Appendix, subsection A.1. Subsection A.3 suggests a possible link between the present analysis and buoyancy induced volcanic mush destabilization (Degruyter & Huber 2014). Finally, subsections A.4 and A.5 specify two technical points not explicitly included in the main text, namely the profiles of temperature with increasing temperature at the boundary and a refined scaling law for the destabilization time at small h. …”

Section: Introductionmentioning

confidence: 99%

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Buoyancy-driven destabilization of an immersed granular bed

et al. 2018

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Under suitable conditions, an immersed granular bed can be destabilized by local thermal forcing and the induced buoyant force. The destabilization is evident from the triggering and establishment of a dense fluid-like granular plume. Varying the initial granular layer average height h, time series of the free layer surface are extracted, allowing us to dynamically compute the underlying volume of the granular layer. The initial interface deformation, the lowering of the average granular interface (i.e. decrease of the granular layer volume) and the emission of a plume are observed and analyzed. We show that the phenomenon is mainly driven by heat transfer, for large h and also involves variable height thermal boundary condition & Darcy's flow triggering, for small h. Simple modeling with no adjustable parameter not only allows us to capture the observed scaling power laws but is also in quantitative agreement with the obtained experimental data.

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A model for eruption frequency of upper crustal silicic magma chambers

Cited by 115 publications

References 55 publications

Lifetime and size of shallow magma bodies controlled by crustal-scale magmatism

Lifetime and size of shallow magma bodies controlled by crustal-scale magmatism

Magma evolution inside the 1631 Vesuvius magma chamber and eruption triggering

Buoyancy-driven destabilization of an immersed granular bed

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