Magma reservoir at Mt. Vesuvius: Size of the hot, partially molten, crust material detected deeper than 8 km

Nunziata, C.; Natale, M.; Luongo, G.; Panza, G. F.

doi:10.1016/j.epsl.2005.12.002

Cited by 33 publications

(25 citation statements)

References 14 publications

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“…8, right, NW-SE profile, orange layers) that occur in coincidence with the Acerra depression (NW) and the Pompei graben (SE). Based on our current results, the low density body is unlikely to represent the sill-like structure suggested byAUGER et al (2001) andNUNZIATA et al (2006). Our results are more in support of the C shaped negative velocity/density anomaly detected byTONDI and DE FRANCO (2006).…”

supporting

confidence: 78%

“…This body was also modelled by new isotopic data (CIVETTA et al, 2004) and by a new inversion of P-wave and S-wave arrival times for local earthquakes, highlighting a lower V s velocity below the Mt. Vesuvius cone in a 0.35-kmthick layer (NUNZIATA et al, 2006). Moreover, a joint inversion of P-wave and S-wave arrival times (from local earthquakes) and shot data collected during the TOMOVES 1994 and 1996 experiments showed the presence of a high V p and V p /V s anomaly that is located around the crater axis, between 0 km and 5 km in depth, which involves the volcano edifice and the carbonate basement.…”

Section: Introductionmentioning

confidence: 99%

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3D Gravity Inversion by Growing Bodies and Shaping Layers at Mt. Vesuvius (Southern Italy)

Berrino

Camacho²

2008

Pure appl. geophys.

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To improve our knowledge of the structural pattern of Mt. Vesuvius and its magmatic system, which represents one of the three volcanoes located in the Neapolitan area (together with Campi Flegrei and Ischia; southern Italy), we analyze here the Bouguer gravity map that is already available through its interpretation by means of 2.5-dimensional modelling. We have carried out a three-dimensional interpretation using a new and original algorithm, known as 'Layers', that has been especially processed for this purpose. Layers works in an automatic and non-subjective way, and allows the definition of the structural settings in terms of several layers, each representing a specific geological formation. The same data are also interpreted in terms of isolated and shallow anomalous density bodies using a well tested algorithm known as 'Growth'. We focus our inversions on the Mt. Vesuvius volcano, while globally analyzing the entire Neapolitan area, in order to investigate the deep structures, and in particular the deep extended 'sill' that has been revealed by seismic tomography.The final models generally confirm the global setting of the area as outlined by previous investigations, mainly for the shape and depth of the carbonate basement below Mt. Vesuvius. The presence of lateral density contrasts inside the volcano edifice is also shown, which was only hypothesized in the 2.5-dimensional inversion. Moreover, the models allow us to note a high density body that rises from the top of the carbonate basement and further elongates above sea level. This probably represents an uprising of the same basement, which is just below the volcano and which coincides with the V P and V P /V S anomalies detected under the crater. The three-dimensional results also reveal that the two inversion methods provide very similar models, where the high density isolated body in the Growth model can be associated with the rising high density anomaly in the Layers model. Taking into account the density of these modelled bodies, we would also suggest that they represent solidified magma bodies, as suggested by other studies. Finally, we did not clearly detect any deep anomalous body that can be associated with the sill that was suggested by seismic tomography.

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supporting

confidence: 78%

Section: Introductionmentioning

confidence: 99%

3D Gravity Inversion by Growing Bodies and Shaping Layers at Mt. Vesuvius (Southern Italy)

Berrino

Camacho²

2008

Pure appl. geophys.

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“…This conductor was observed beneath all sites and could indicate a highly conductive brine [ Manzella et al , 2004]. While such a conductor should filter out appreciably the effect of the deep structures, our modeling based on geological and petro‐physical constraints suggested that a large magma chamber at depths proposed by other geophysical investigations [e.g., Nunziata et al , 2006] should have produced a detectable signature at the longest periods available in the data set (1–200 s). Even if field data are limited in number and probably affected by coherent electromagnetic noise (MT phases are particularly noisy), the effect of a large magma chamber is likely above the noise level, especially on the apparent resistivity.…”

Section: Discussionmentioning

confidence: 72%

“…Proposed future scenarios range from a sub‐plinian eruption, similar to 472 or 1631 AD eruptions [ Scandone et al , 1993; Santacroce et al , 2005] up to devastating AD79 Pompei‐type events associated to a larger magma storage zone that would extend well beyond the size of Mt. Vesuvius cone [e.g., Auger et al , 2001; Nunziata et al , 2006].…”

Section: Introductionmentioning

confidence: 99%

A new petrological and geophysical investigation of the present‐day plumbing system of Mount Vesuvius

Pommier¹,

Tarits

Hautot

et al. 2010

Geochem Geophys Geosyst

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[1] A model of the electrical resistivity of Mt. Vesuvius has been elaborated to investigate the present structure of the volcanic edifice. The model is based on electrical conductivity measurements in the laboratory, on geophysical information, in particular, magnetotelluric (MT) data, and on petrological and geochemical constraints. Both 1-D and 3-D simulations explored the effect of depth, volume and resistivity of either one or two reservoirs in the structure. For each configuration tested, modeled MT transfer functions were compared to field transfer functions from field magnetotelluric studies. The field electrical data are reproduced with a shallow and very conductive layer (∼0.5 km depth, 1.2 km thick, 5 ohm.m resistive) that most likely corresponds to a saline brine present beneath the volcano. Our results are also compatible with the presence of cooling magma batches at shallow depths (<3-4 km depth). The presence of a deeper body at ∼8 km depth, as suggested by seismic studies, is consistent with the observed field transfer functions if such a body has an electrical resistivity > ∼100 ohm.m. According to a petro-physical conductivity model, such a resistivity value is in agreement either with a low-temperature, crystal-rich magma chamber or with a small quantity of hotter magma interconnected in the resistive surrounding carbonates. However, the low quality of MT field data at long periods prevent from placing strong constraints on a potential deep magma reservoir. A comparison with seismic velocity values tends to support the second hypothesis. Our findings would be consistent with a deep structure (8-10 km depth) made of a tephriphonolitic magma at 1000°C, containing 3.5 wt%H 2 O, 30 vol.% crystals, and interconnected in carbonates in proportions ∼45% melt −55% carbonates.

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“…Such Vp/Vs ratio is very reasonable for the Campanian area as it has been found to vary between 1.8 (e.g. Zollo et al 2002;Auger et al 2003;Nunziata et al 2006;Nunziata 2010; Nunziata and Costanzo 2010), 1.85 (Guidarelli et al 2006) and 1.9 (Lomax et al 2001). Densities have been attributed according to the model inverted from regional dispersion data (Panza et al 2007a) and, in the top 1 km, from gravity modeling (Capuano et al 1992).…”

Section: Discussionmentioning

confidence: 95%

VS crustal models of the Roccamonfina volcano and relationships with Neapolitan volcanoes (southern Italy)

Nunziata

Gerecitano²

2011

Int J Earth Sci (Geol Rundsch)

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Shear wave velocities of the crust and upper mantle are defined beneath the Roccamonfina volcano and surrounding Apennines (southern Italy) from the simultaneous nonlinear inversion of the local group velocity dispersion data, obtained from seismic events recorded in 1988-2004 at Roccamonfina station of the INGV-RSNC network, and regional dispersion data obtained in previous studies. The main features of the representative V S models are a carbonatic basement and a low velocity zone at 6-10 km of depth. The sedimentary succession is *5 km thick below the Roccamonfina volcano and lays above a high V S (3.8 km/s) ascribable to solidified magma body, while it is *10 km thick below the surrounding Apennines. A low velocity layer with an average thickness of 10 km is detected below the Roccamonfina volcano which can be associated with the presence of partial melting and interpreted as magmatic reservoir. Such low velocity layer, also found below the surrounding Apennines but with a reduced thickness of 2-3 km, extends to the Campanian Plain and to the Neapolitan volcanic area, from Campi Flegrei to Somma-Vesuvius.

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Magma reservoir at Mt. Vesuvius: Size of the hot, partially molten, crust material detected deeper than 8 km

Cited by 33 publications

References 14 publications

3D Gravity Inversion by Growing Bodies and Shaping Layers at Mt. Vesuvius (Southern Italy)

3D Gravity Inversion by Growing Bodies and Shaping Layers at Mt. Vesuvius (Southern Italy)

A new petrological and geophysical investigation of the present‐day plumbing system of Mount Vesuvius

VS crustal models of the Roccamonfina volcano and relationships with Neapolitan volcanoes (southern Italy)

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