Accurate assessment of 3D crustal velocity and density parameters: Application to Vesuvius data sets

Tondi, R.; Franco, R. de

doi:10.1016/j.pepi.2006.07.001

Cited by 12 publications

(15 citation statements)

References 38 publications

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“…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%

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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%

“…negative density body inside the volcano edifice that is clearly visible in the c profile; -several negative density bodies around Mt. Vesuvius, which are mainly W and SE and which were also seen by TONDI and DE FRANCO (2006).…”

Section: Analyses Results and Discussionmentioning

confidence: 94%

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

Berrino

Camacho²

2008

Pure appl. geophys.

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“…2. Through a slight modification of equation (1) of Tondi and de Franco [2006], α is now inverted and optimized independently for each model parameter:

α_{m} = {((), G^{T} C_{gg}^{- 1} boldG true(v_{0} + normalΔ v_{s} true))}^{- 1} ({boldG}^{T} {boldC}_{italicgg}^{- 1} g)

…”

Section: Optimization Of the Velocity And Density Model With The Sequmentioning

confidence: 99%

“…As shown inFigure 5, each body is characterized by a point origin (the bottom left node) that is denoted as ρ 0 , and three density gradients in the x , y , z directions, with respect to this point. The expression that was derived by Pohánka [1988] for a polyhedral body with a density that is linearly dependent on some coordinates is used for the computation of the three components of the gravity field [ Tondi and de Franco , 2006]. The use of polyhedral bodies with linearly varying density allows us to appropriately match the density gradients with the shear velocity gradients during the sequential integrated modeling.…”

Section: Optimization Of the Velocity And Density Model With The Sequmentioning

confidence: 99%

“…We address this problem in the present study, and we contribute to the precise knowledge of both the density and the shear‐wave velocity structure of the upper mantle below the European continent with a lateral resolution of 1° × 1°. The new shear‐wave and density models are recovered using the inversion approach of Sequential Integrated Inversion (SII; [ Tondi and de Franco , 2006]), which has been recently parallelized to allow for a large data set and a large number of parameters [ Tondi et al , 2012]. We specify an initial 3‐D velocity model that is iteratively updated and scaled to a 3‐D density model through the combined use of seismological and gravity observations.…”

Section: Introductionmentioning

confidence: 99%

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Upper mantle structure below the European continent: Constraints from surface‐wave tomography and GRACE satellite gravity data

Tondi¹,

Schivardi²,

Molinari³

et al. 2012

J. Geophys. Res.

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We here exploit fundamental mode Rayleigh and Love seismic wave information and the high resolution satellite global gravity model GGM02C to obtain a 1° × 1° 3‐D image of: (a) upper‐mantle isotropic shear‐wave speeds; (b) densities; and (c) density‐vScoupling below the European plate (20°N–90°N) (40°W–70°E). The 3‐D image of the density‐vScoupling provides unprecedented detail of information on the compositional and thermal contributions to density structures. The accurate and high‐resolution crustal model allows us to compute a reliable residual topography to understand the dynamic implications of our models. The correlation between residual topography and mantle residual gravity anomalies defines three large‐scale regions where upper mantle dynamics produce surface expression: the East European Craton; the eastern side of the Arabian Plate; and the Mediterranean Basin. The effects of mantle convection are also clearly visible at: (1) the Eastern Sirt Embayment; (2) the West African Craton northern margins; (3) the volcanically active region of the Canarian Archipelago; (4) the northern edge of the Central European Volcanic Province; and (5) the Northeastern part of the Atlantic Ocean, between Greenland and Iceland. Strong connections are observed among areas of weak radial anisotropy and areas where the mantle dynamics show surface expression. Although both thermal and additional dependencies have been incorporated into the density model, convective down‐welling in the mantle below the East European Craton is required to explain the strong correlation between the estimated negative mantle residual anomalies and the negative residual topography.

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The stress field beneath a quiescent stratovolcano: The case of Mount Vesuvius

D’Auria

Massa

Matteo

2014

J. Geophys. Res. Solid Earth

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We have analyzed a focal mechanism data set for Mount Vesuvius, consisting of 197 focal mechanisms of events recorded from 1999 to 2012. Using different approaches and a comparison between observations and numerical models, we have determined the spatial variations in the stress field beneath the volcano. The main results highlight the presence of two seismogenic volumes characterized by markedly different stress patterns. The two volumes are separated by a layer where the seismic strain release shows a significant decrease. Previous studies postulated the existence, at about the same depth, of a ductile layer allowing the spreading of the Mount Vesuvius edifice. We interpreted the difference in the stress pattern within the two volumes as the effect of a mechanical decoupling caused by the aforementioned ductile layer. The stress pattern in the top volume is dominated by a reverse faulting style, which agrees with the hypothesis of a seismicity driven by the spreading process. This agrees also with the persistent character of the seismicity located within this volume. Conversely, the stress field determined for the deep volume is consistent with a background regional field locally perturbed by the effects of the topography and of heterogeneities in the volcanic structure. Since the seismicity of the deep volume shows an intermittent behavior and has shown to be linked to geochemical variations in the fumaroles of the volcano, we hypothesize that it results from the effect of fluid injection episodes, possibly of magmatic origin, perturbing the pore pressure within the hydrothermal system.

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Accurate assessment of 3D crustal velocity and density parameters: Application to Vesuvius data sets

Cited by 12 publications

References 38 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)

Upper mantle structure below the European continent: Constraints from surface‐wave tomography and GRACE satellite gravity data

The stress field beneath a quiescent stratovolcano: The case of Mount Vesuvius

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