GNGTS 2023 - Atti del 41° Convegno Nazionale

Session 1.2 - POSTER GNGTS 2023 host rocks, assumed as isotropic elastic (Young modulus E = 10 MPa), the hydrothermal system (E = 2.5 MPa), and the surrounding rocks (E = 5 MPa). The Poisson coefficient is fixed at 0.25). The modelled fluid is assumed as water, with density ρ = 1000 kg/m 3 , and dynamic viscosity μ=0.0001 Pa s. The permeability is assumed constant and equal to k=1e-15 m 2 . We analyse the evolution of the model by imposing the inflation of the magma chamber (DP in Figure 1) as modelled in Trasatti et al. (2015) for the 1982-84 unrest, and in Trasatti (2022) for the 2011-2013 unrest. We consider the development of excess pore pressure, fluid flow and ground deformations for one year assuming three different scenarios: ● Linear elastic model without water and linear inflation of the magma chamber; ● Poroelastic model with linear inflation of the magma chamber; ● Poroelastic model with impulsive inflation of the magma chamber. Figure 1. Sketch of the axi-symmetric Finite Element model. The inset shows details on the hydraulic boundary conditions and the applied overpressure (DP) on the deep magma chamber. Preliminary results and discussion