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symmetry, the travel-times equations of the direct and refracted longitudinal
waves are first deduced. These linear equations are determined
from the seismic ray parameter p, and from the known term a,. The
parameter p, is connected with the velocity of the elastic waves that are
refracted on the i-th layer; «, depends on the velocity of the layers crossed
by the seismic ray and on their thickness.
Subsequently, the equations of the first arrivals, observed in quite a
number of stations surrounding the Straits of Messina during the seismic
crisis of the Gulf of Patti (1978), are utilized for working out a crustal model
for the Messina Straits area. Given the inadequatly of the passive seismology
data both in number and in characteristics the most superficial layers
of the model are defined using the results of deep seismic exploration
carried out in areas contiguous to the Straits. The thickness and velocity
of the longitudinal waves in the underlying layers are, instead, determined
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