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The use of a very dense seismic array to characterize the Cavola, Northern Italy,
active landslide body. By P. Bordoni , F. Cara , M. Cercato , G. Di Giulio , A.J. Haines , G. Milana , A. Rovelli , S. Ruso
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The analysis of data coming from a dense 95-station array installed on the Cavola landslide
(northern Apennines) is presented. The array extended along a 112X80 m2 area covered by
clay deposits related to a recent and still active landslide. It operated along a four month time
period in a continuous mode recording. Both earthquake and noise data are used to assess
the amplification effects and relate them to thickness and geophysical properties of
outcropping terrain. Compared to a reference site, earthquake data recorded on the landslide
show a ground motion amplification up to a factor of 4 in the 2.5 to 5 Hz frequency band.
Moreover, the study of the predominant frequency distribution derived from spectral analysis
of ambient noise allows to infer thickness variations along the array. We then identify zones
with small lateral variations to select sub-arrays with homogenous geometrical subsoil
conditions where passive and active 1D and 2D array data analysis techniques are applied to
evaluate shear waves velocity in the landslide body. Available drilling and down-hole data are
used to calibrate the velocity model inferred from seismic surface data. This analysis permits
to reconstruct an approximate 2D geometry used as a base for modelling waveform changes
along the array.
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Geographic location of the Cavola array (red triangle), along with the earthquakes recorded during the
experiment (black circles)
Array geometry and topography of landslide. P3 station is installed on
outcropping marls, all the other stations are installed on the landslide body
Geological Setting
The geology of the area is well known, the major outcropping units are the Ranzano and Monte Piano Marls that represent the bedrock for the landslide body. Monte Piano Marls were found at a depth respectively of 44 and 25 metres in
borehole 1 and 2. Geophysical prospecting were realized in the area including geoelectrical and seismic profiles. Along the profiles X – X’ and Z – Z’ were also collected data for MASW and NASW analysis. In borehole 2 a down hole
measurements were also performed. The analysis of geological and geothecnhical data allowed a preliminary reconstruction on the bedrock along the profile A – D.
Spectral analysis on earthquakes and noise
EW/H noise
NS/H noise
NS/V noise
NS/H noise
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EW/H earthquakes
NS/H earthquakes
NS/H earthquakes
Spectral analysis was performed on all the stations of the array using both seismic noise and earthquakes recordings. The top plot represents H/V results for the North
component of noise along the line 3, central plot is the H/H result for the same noise record, bottom plot is the H/H analysis obtained as an average on about 20 earthquakes
with different azimuth and good signal to noise ratio. The complete H/H analysis on the entire array is represented on the side plot respectively for seismic noise (top) and
earthquakes (bottom) . We notice an increase of resonance frequency moving from line A line M suggesting some decreasing on the landslide thickness. The presence is
clear of an area with homogeneous behaviour suggesting the occurrence of a 1D situation from line G to line M. The end of landslide body is marked by lines N and O.
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Active and passive surface waves techniques for velocity structure determination
The data for refraction and MASW – NASW analysis were
recorded with 48 geophones (4.5 Hz natural frequency)
spaced as shown on the top-left plot. The total layout
length was of 141 meters. The dispersion curves are
obtained performing both MASW and NASW analysis. In
particular high frequency dispersion (f > 6Hz) is mainly
derived from MASW, while low frequency data are inferred
by NASW data. This is shown on the top–right plot were
the picking of maxima on the frequency slowness plane is
performed on the maximum energy areas and on the lower
envelop at high and low frequency, respectively. Velocity
model inversion results are shown (bottom–left) along with
the final velocity model (bottom-right). For the Z – Z’ line we
are able to reach the landslide bedrock and to find results
in good agreement with both refraction and down hole data.
For the X – X’ line the surface velocities are comparable
with the velocities found in the Z – Z’ line, while a deeper
bedrock is clearly shown by dispersion data, in agreement
with borehole 1 results. Due to the limited extension on the
geophones layout we are not able to clearly define the
bedrock depth for line X – X’.
NASW Data
MASW Data
LINE Z - Z’
LINE X - X’
Undefined Bedrock
(1) INGV, Rome, Italy.
(2) University “La Sapienza”, Rome, Italy.
(3) Cambridge University – Bullard Laboratories, Cambridge, United Kingdom.
Referring author: Giuliano Milana, INGV,
Via di Vigna Murata 605, 00143,
Roma, ITALIA
e-mail: [email protected]
CONCLUSIONS
•The performed analysis allows to detect a geometry variation along the landslide body.
•Complexities due to strong topography variations are also shown by data.
•A preliminary model of bedrock geometry can be constructed using all the available data.
•Some extra investigation can be useful to better define bedrock depth in the upper lines of the array.
•A preliminary model of wave propagation wiil be tried using the results obtained at this stage of the work.