1 Istituto Nazionale di Geofisica e Vulcanologia, Italy. Correspondent author: Paola Bordoni. Istituto Nazionale di Geofisica e Vulcanologia

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1 Preliminary results from EMERSITO, the rapid response network for site effect studies Paola Bordoni 1, Riccardo M. Azzara 1, Fabrizio Cara 1, Rocco Cogliano 1, Giovanna Cultrera 1, Giuseppe Di Giulio 1, Antonio Fodarella 1, Giuliano Milana 1, Stefania Pucillo 1, Gaetano Riccio 1, Antonio Rovelli 1, Paolo Augliera 1, Lucia Luzi 1, Sara Lovati 1, Marco Massa 1, Francesca Pacor 1, Rodolfo Puglia 1, Gabriele Ameri 1 1 Istituto Nazionale di Geofisica e Vulcanologia, Italy Correspondent author: Paola Bordoni Istituto Nazionale di Geofisica e Vulcanologia paola.bordoni@ingv.it 1 - Introduction On May 20 th, 2012 at 02:03 UTC a magnitude Ml= 5.9 reverse fault earthquake occurred in the Emilia-Romagna region, northern Italy, at a hypocentral depth of 6.3 km ( close to the cities of Modena and Ferrara in the plain of the Po river. The epicenter was near the village of Finale Emilia where macroseismic intensity was assessed at 7 EMS98 (Tertulliani et al. 2012, this issue), while the closest accelerometric station, MRN, located less than 20 km west-ward at Mirandola (Figure 1) recorded peaks of ground accelerations of about 300 cm/s 2 ( The mainshock triggered liquefaction phenomena few kilometers eastward of the epicenter around the village of San Carlo. In the same day other two shocks of magnitude Ml=5.1 followed (02:07 and 13:18 GMT On May 29 th at 07:00 UTC another magnitude Ml=5.8 earthquake ( hit the region with epicenter close to the village of Mirandola (Figure 1). Other three strong aftershocks occurred afterwards, a magnitude Ml=5.3 (May 29 th at 10:55), Ml=5.2 (May 29 th at 11:00) and Ml=5.1 (June 3 rd at 19:20). For a detailed description of the seismic sequence see Moretti et al. [2012], Scognamiglio et al. [2012], and Massa et al. [2012] this issue. The Emilia seismic sequence caused 25 casualties, several among the workers of the many factories collapsed during working hours, and extensive damage on monuments, public buildings, industrial activities and private homes. The Po plain region, struck by the 2012 Emilia seismic sequence, is a very large E-W trending syntectonic alluvial basin, which extends for about km 2. It is surrounded by the Alps to the north and the Apennines to the south and it is filled with Plio-Pleistocene terrigenous sediments of and Holocene deposits with depths varying from few hundred meters up to several kilometers. The epicentral area is located south of the Po River, in correspondence of the active front of the Northern Apennines thrust belt (north-vergence) composed of buried folds and thrust faults, which locally produce structural highs (Figure 1), known as Pieghe Emiliane and Ferraresi [Pieri and Groppi, 1981]. The top of this limestone and marl bedrock rises roughly to 150 m from the surface and has derived locally from borehole logs. The seismic response of this ~150 m deep soft cover had been investigated using weak motion events and microtremors recorded in borehole by 1

2 Margheriti et al. [2000]. The occurrence of the May 2012 seismic sequence makes it possible to study the seismic response in near-field conditions. These studies are aimed at providing tools to reduce the impact of future earthquakes on the local communities. In addition to the amplification due to 1D resonance, it is well known that seismic response of deep sedimentary basins is affected by two and three-dimensional effects (wave diffraction, conversions at the basin edges, trapping and focusing of energy within the soil volume). Evidence of basin-induced surface waves and edge effects have been observed in many basins worldwide, e. g. the Osaka basin in Japan [e.g., Kawase, 1996; Pitarka et al., 1998], various southern California basins [Graves et al., 1998; Day et al.; 2008], the Parkway basin in New Zealand [Chávez-García et al., 1999]. In Italy good examples of site amplification in alluvial basin can be found in Gubbio, Città di Castello, L Aquila and Fucino basin [Bindi et al., 2009, Milana et al. 2011, Cara et al. 2011, Bordoni et al. 2003]. Therefore the day after the mainshock the INGV rapid response network for site effect, called EMERSITO, planned the experiments presented in this paper. EMERSITO put together independent research groups from several territorial centers of Istituto Nazionale di Geofisica e Vulcanologia who, spontaneously and on the basis of data archiving and sharing policy, agree to collaborate deploying their seismic equipment in the epicentral area, building on the experience of the 2009 L Aquila earthquake [Margheriti et al., 2011, Milana et al. 2011, Di Giulio et al. 2011]. The deployment was planned also in collaboration with the geological survey of the Regione Emilia Romagna (Servizio Geologico e Sismico e dei Suoli), the University of Modena as well as in the framework of SISMIKO [Moretti et al this issue]. As a result of this effort, since the 24 th of May three linear arrays have been deployed (Figure 1), with a total of 22 sites instrumented, 16 of them equipped with both velocimeters and accelerometers. These arrays recorded most of the aftershock sequence, including the Mw th May 7:00 earthquake. The continuous recordings will be archived into the EIDA database [ under restricted access. The aim of this paper is to describe the experiments performed by the EMERSITO team as well as the main features of the recorded earthquakes. A preliminary insight in the site response of the investigated area, within the context of the geological structure of the Po plain, is also given. 2 Near-surface geology The epicentral area is characterized by a flat morphology with geomorphic features typical of the area and locally raising from the plain. They are river levees, anthropic fillings and abandoned river channels of the tributaries of the Po River, draining the northern Apennines (Figure 1). The superficial geology of the study area is dominated by paleo-river beds sediments (mainly sand, sand-silty and silty-clay) of the Secchia, Panaro and Reno rivers. Inside these sediments locally it is possible to find some confined aquifers whereas in the deep sedimentary cover there are some aquifers of regional importance [Regione Emilia Romagna ENI-AGIP, 1998]. Most of the liquefaction effects occurred between Sant Agostino and San Carlo, along a belt following the abandoned river bed of the Reno River [Emergeo and this issue; Recent very detailed investigation performed by Regione Emilia Romagna [ at San Carlo reconstructed a geological cross-section through the abandoned channel of the Reno river, where the most severe effects of the ground fracture and liquefaction occurred. In the first 20 m of subsoil they found scattered lens with confined aquifers formed by fine sands mainly in a sandy silt and silty-sand complex, which are supposed to be responsible for the surface effects. 2

3 3 The experiments The temporary stations were installed along two roughly N-S trending profiles (Figure 1), where geological cross-sections were already available (Figure 2) with the purposes of investigating, on one hand, the geometry of the sedimentary cover, which appears to thicken moving away from the structural highs. On the other hand, the site selection was focused on studying the effect of the abandoned riverbeds as well as on damage suffered by the local factories. The eastern-most profile (hereinafter CAS array) cuts through the boreholes around the village of Casaglia, where the bottom of the Quaternary deposits has been reached at 140 m depth. The seismic response had been investigated by evaluating surface-to-downhole spectral ratios [Margheriti et al. 2000]. Unfortunately this borehole instrumentation was not operating during the seismic sequence. The CAS array consists of 8 stations installed along a SW NE direction. Four of the CAS array sites were equipped at the beginning with Reftek 72A 3 channels digitizers coupled to Lennartz Le3d-5s seismometers. In the other sites, where Reftek R130 6-channels digitizers were available, Kinemetrics Episensor accelerometers were added (see Table 1). Station CAS5 is located at San Carlo village where the most serious liquefaction phenomena and ground failure took place. From the 29 th of May the Reftek 72A had been substituted with Reftek channels and re-deployed along a third array of 6 stations across the San Carlo village [hereinafter SCA array] with an E-W trending (Table 1). The western-most profile (hereinafter MIR array) cuts through the Mirandola structural high where a PGA of about 300 cm/s 2 was recorded at the MRN site during the main-shock ( The station is included in the permanent accelerometric network, RAN, operated by Dipartimento di Protezione Civile Nazionale (DPC). The MIR array is composed of 8 Quanterra330 6-channels digitizers connected to Lennartz Le3d-5s velocimeter and Kinemetrics Episensor distributed along a N S trending profile. 4 - Results and discussion Time series features and comparison with strong motion prediction law Figure 3 shows the NS horizontal component of the ground acceleration for the May 29 th event (Ml=5.8) located at hypocentral depth of about 10.2 km, and epicenter close to MIR1. Whereas the P-waves first arrival is quite clear, S-waves arrival is not easily detectable. The seismograms show high complexity due to a considerable amount of elastic energy released as local surface waves that increase in amplitude with increasing epicentral distance. They are the main features of the ground motion recorded. A fast decay of the amplitude with distance is also evident. For frequencies bigger than 10 Hz (Figure 4), the vertical component has amplitude higher than the horizontal ones. Despite this difference in the frequency content, the peak ground acceleration for horizontal and vertical component is similar. At this stage it is not possible to associate the features due to source, propagation or site effects. In term of horizontal displacement the data recorded in near-source condition show peak displacement in order of cm at low frequency. The strong motion records for the May 29th event were corrected with the procedure described by Pacor et al. [2011], and were filtered in the frequency band between 0.1 and 40 Hz. In Figure 5, the 3

4 derived PGA and PGV values for the geometric mean of the horizontal components and of the vertical one are compared to estimates from a ground motion prediction equation assessed from the database of Italian earthquake [Bindi et al., 2011, hereafter referred to as ITA10] and with the other peak values observed from INGV and RAN stations located in the distance range 0-200km. The predictions are computed for reverse fault and for site A and C in the EC8 classification (where EC8 class A corresponds to shear-wave velocity averaged over the top 30 m of the soil profile - Vs30 > 800 m/s and class C Vs30 = m/s). From the geological and geophysical information available, we attributed the sites monitored to site C in the EC8 classification. The distances from the fault were computed defining fault geometry based on geological and focal mechanism data (Quick Regional Centroid Moment Tensor The mean predictions for C site in the EC8 classification fit well the observed PGAs for both components, except for very short distances (< 5km) where the vertical peak values tend to be larger than the ITA10 mean estimates. The horizontal PGVs, at distance shorter than 10km, are within the median and the median plus one standard deviation estimates for C site in the EC8. Conversely, except for the near fault peak values at Joyner-Boore distance [Joyner and Boore, 1981] R JB = 1 km, the ITA10 predictions for EC8 C sites overestimates the observed data for the vertical component, that decay with distance following the mean curve for EC8 A sites. These comparisons indicate that the ground motion from the 29 th May event is characterized by larger low-frequency content on the horizontal components with respect to the average trend expected for the Italian territory; this is probably related to the presence of the deep sediments of the Po plain. The vertical components at short distances are more affected by high frequencies and this is clearly seen also by a visual inspection of waveforms H/V Spectral ratio from earthquake and noise measurements Because of the large distance between bedrock outcroppings and the studied area and the lack of borehole instrumentation, we could not select a site to use as reference for computing standard spectral ratios for earthquakes [Borcherdt, 1970]. Therefore, we compute the empirical transfer function using the horizontal-to-vertical spectral ratios earthquakes after Lermo and Chavez-Garcia [1993] and hereafter referred to as HVSR. The HVSR was computed over 20 seconds of waveform starting at the P wave arrival and including S-waves as well as part of the early surface waves. The use of windows containing P, S, and surface waves may violate the receiver function assumption of vertical component being amplification free, but due to the short epicentral distances it is very difficult to split the P and S arrivals (S-P time is very small) and, anyway, the S and surface waves contribution is predominant. All the analyzed sites are in the epicentral area and in a near-source condition (Table 2 lists the selected events) and therefore the differences among sites include obviously some source effects. The only exception is the June 6 th Ml=4.5 event coming from few tens of kilometers south-east of the epicentral area. Using the continuous recording, we have computed spectral ratios on ambient noise [Nakamura, 1989], hereafter referred to as HVNSR. All the signals were processed with a detrigger algorithm (SESAME, 2004) to remove noise windows containing disturb and transient phenomena. The single window length was set to 60 seconds to enhance the resolution in the low-frequency range. Fourier spectra were smoothed with a Konno Omachi (1998) algorithm, and HVNSR was evaluated on the geometrical mean of the Fourier spectra of horizontal components. 4

5 It is generally accepted (see Bard, [1998] for an overview) that HVSNR is capable of detecting the predominant period of resonance while it generally underestimate the amplitude of amplification. For this reason it cannot be used as empirical transfer function of the soil. As an example of our results we show sites MIR01 and MIR04 (Figure 6). As often found in literature, the HVNSRs have a simple shape in comparison to the HVSRs. The HVSRs are characterized by broad-band amplification including many peaks with large amplitudes. These frequency peaks do not always agree with those detected by noise. The variation of HVSR among sites is remarkable. At MIR array stations, the HVNSR frequency peak is within the range 0.6 to 0.9 Hz. Such a low-frequency peak is arguably linked to the thickness of soft deposits. The HVNSR peak between Hz, probably due to deeper interfaces, needs more investigation because it is on the resolution limits of the equipment used. The data analysis has just started therefore is not reasonable to give a detailed interpretation of the described discrepancies between earthquake and noise spectral ratios. Furthermore we need to know better the detail of the local geology in order to make correlation with the high frequency behavior of the spectral ratio. As general comment, the differences between the spectra suggest that the HVSR catch the complex wave-field interaction due to the subdued geology, which is excited only during earthquakes, though they include obviously some source and propagation effect. On the contrary, HVNSR on noise is likely capable to only catch the dominant period of resonance and that can be used to constrain the thickness of the soft sediments of the geological model using 1D assumption, provided that the impedance contrast is enough strong to insure the reliability of the method. For the further analysis it will be interesting to compute HVSR splitting the earthquakes in two datasets, a near field and far field one. 5 - Future development The dataset collected by EMERSITO network includes a remarkable quantity of good quality data that spans the entire range of ground motion from microtremor to Ml=5.8, and is also recorded in near-field conditions. It can be used in seismic response studies, non-linear soil behavior studies and ground motion prediction. It will be included in the dataset recorded by the emergency rapid response network of INGV, SEISMIKO (Moretti et al this issue). 6 - Data and sharing resources The continuous recordings will be archived into the EIDA database [ under restricted access. Acknowledgement The EMERSITO group is grateful to the Emilia Romagna people for the warm support during the deploying activities despite the grief and the difficult time. We thank two anonymous reviewers and the Editor who provided valuable comments and suggestions improving our manuscript. 5

6 References Bard, P.-Y. (1998). Microtremor measurements: A tool for site effect estimation, in Proc. of the 2 nd International Symp. on the Effects of Surface Geology on Seismic Motion, Yokohama, Japan, Bindi, D., Parolai S., Cara F, Di Giulio G., Ferretti G., Luzi L., Monachesi G., Pacor F., and Rovelli A. (2009). Site Amplifications Observed in the Gubbio Basin, Central Italy: Hints for Lateral Propagation Effects. Bulletin of the Seismological Society of America, vol. 99, p , ISSN: , doi: / Bindi, D., F. Pacor, L. Luzi, R. Puglia, M. Massa, G. Ameri and R. Paolucci (2011). Ground motion prediction equations derived from the Italian strong motion database, Bulletin of Earthquake Engineering, vol. 9, 6, , doi: /s Borcherdt, R. D. (1970). Effects of local geology on ground motion near San Francisco Bay, Bull. Seism. Soc. Am. 60, Bordoni, P., G. Cultrera, L. Margheriti, P. Augliera, G. Caielli, M. Cattaneo, R. de Franco, A. Michelini, and D. Spallarossa (2003). A microseismic study in a low seismicity area: the 2001 site-response experiment in the Città di Castello (Italy) basin. Annals of Geophysics 46(6). Cara F, Di Giulio G., Cavinato G. P., Famiani D., and Milana G. (2011). Seismic characterization and monitoring of Fucino Basin (Central Italy). Bulletin of Earthquake Engineering, vol. 9, p , ISSN: X, doi: /s Cerrina Feroni, A., L. Martelli, P. Martinelli and G. Ottria, with the contributions of R. Catanzariti (2002): Carta Geologico-Strutturale dell Appennino Emiliano-Romagnolo alla scala 1: (Regione Emilia-Romagna, Servizio Geologico, Sismico e dei Suoli, CNR, Istituto di Geoscienze e Georisorse, Pisa, S.E.L.CA, Firenze) Chávez-García, F. J., W. R. Stephenson, and M. Rodríguez (1999). Lateral propagation effects observed at Parkway, New Zealand. A case history to compare 1D versus 2D site effects, Bull. Seism. Soc. Am., 89, Day, S.M., Graves R., Bielak J., Dreger D., Larsen S., Olsen K. B., Pitarka A. and L. Ramirez- Guzmanc (2008). Model for Basin Effects on Long-Period Response Spectra in Southern California, Earthquake Spectra, Volume 24, No. 1, pages Di Giulio, G., Marzorati S., Bergamaschi F., Bordoni P., Cara F, D'Alema E., Ladina C., and Massa M. (2011). Local variability of the ground shaking during the 2009 L'Aquila earthquake (April 6, 2009-Mw 6.3): the case study of Onna and Monticchio villages. Bulletin of Earthquake Engineering, vol. 9, p , ISSN: X, doi: /s Graves, R. W., A. Pitarka, and P. G. Somerville (1998). Ground-motion amplification in the Santa Monica area: Effects of shallow basin-edge structure, Bull. Seism. Soc. Am., 88, Joyner, W.B. and Boore, D.M. (1981). Peak Horizontal Acceleration and Velocity from Strong- 6

7 Motion Records Including Records from the 1979 Imperial Valley, California, Earthquake, Bulletin of the Seismological Society of America, Vol. 71, No. 6, pp Kawase, H. (1996). The cause of the damage belt in Kobe: the basin edge effect, constructive interference of the direct S-wave with the basin induced diffracted/rayleigh waves, Seism. Res. Lett. 67, no. 5, Konno K, Ohmachi T (1998) Ground-motion characteristics estimated from spectral ratio between horizontal and vertical components of microtremor. Bull. Seism. Soc. Am. 88: Lermo, J. and E J. Chavez-Garcia (1993). Site effect evaluation using spectral ratios with only one station, Bull. Seism. Soc. Am. 83, Margheriti, L., R. Azzara, M. Cocco, A. Delladio and A. Nardi, (2000). Analyses of borehole broadband recordings: test site in the Po basin, Northen Italy. Bulletin of Seismological Society of America, 90, Margheriti, L., Lauro Chiaraluce, Christophe Voisin, Giovanna Cultrera, Aladino Govoni, Milena Moretti, Paola Bordoni, Lucia Luzi, Riccardo Azzara, Luisa Valoroso, Raffaele Di Stefano, Armand Mariscal, Luigi Improta, Francesca Pacor, Giuliano Milana, Marco Mucciarelli, Stefano Parolai, Alessandro Amato, Claudio Chiarabba, Pasquale De Gori, Francesco Pio Lucente, Massimo Di Bona, Maurizio Pignone, Gianpaolo Cecere, Fabio Criscuoli, Alberto Delladio, Valentino Lauciani, Salvatore Mazza, Giuseppe Di Giulio, Fabrizio Cara, Paolo Augliera, Marco Massa, Ezio D'Alema, Simone Marzorati, Monika Sobiesiak, Angelo Strollo, Anne-Marie Duval, Pascal Dominique, Bertrand Delouis, Anne Paul, Stephan Husen, Giulio Selvaggi (2011), Rapid response seismic networks in Europe: the example of L Aquila earthquake emergency, Annals of Geophysics, /ag-4953 Marco Massa, Rodolfo Puglia, Sara Lovati, Gabriele Ameri, Dario Sudati, Emiliano Russo, Gianlorenzo Franceschina, Lucia Luzi, Francesca Pacor, Paolo Augliera (2012), INGV Strong- Motion Data web-portal, Annals of Gephysics, this issue. Milana, G, Azzara, RM, Bertrand, E, Bordoni, P, Cara, F, Cogliano, R, Cultrera, G, Di Giulio. G, Duval, AM, and Foderella, A, (2011), The contribution of seismic data in microzonation studies for downtown L Aquila, Bulletin of Earthquake Engineering, 9-3, , DOI: /s Moretti, M., Abruzzese L., Abu Zeid N., Augliera P., Azzara R., Barnaba C., Benedetti L., Bono A., Bordoni P., Boxberger T., Bucci A., Cacciaguerra S., Calò M., Cara F., Carannante S., Cardinale V., Castagnozzi A., Cattaneo M., Cavaliere A., Cecere G., Chiarabba C., Chiaraluce L., Ciaccio M.G., Cogliano R., Colasanti G., Colasanti M., Courboulex F., Cornou C., Criscuoli F., Cultrera G., D Alema E., D Ambrosio C., Danesi S., De Gori P., De Luca G., Delladio A., Demartin M., Di Giulio G., Dorbath C., Ercolani E., Faenza L., Falco L., Fiaschi A., Ficeli P., Fodarella A., Franceschi D., Franceschina G., Frapiccini M., Frogneux M., Giovani L., Govoni A., Improta L., Jacques E., Ladina C., Lauciani V., Langlaude P., Lolli B., Lovati S., Lucente F.P., Luzi L., Mandiello A., Marcocci C., Margheriti L., Marzorati S., Massa M., Mazza S., Milana G., Minichiello F., Mercerat D., Molli G., Monachesi G., Moschillo R., Pacor F., Piccinini D., Piccolini U., Pignone M., Pintore S., Pondrelli S., Priolo E., Pucillo S., Quintiliani M., Riccio G., Romanelli 7

8 M., Rovelli A., Salimbeni S., Sandri L., Selvaggi G., Serratore A., Silvestri M., Valoroso L., Van der Woerd J., Vannucci G., Zaccarelli L., Zambonelli E. (2012). Rapid-response to the earthquake emergency of May 2012 in the Po Plain, Northern Italy, Annals of Geophysics, this issue. Nakamura, Y. (1989). A method for dynamic characteristics estimation of subsurface using microtremors and the ground surface. Quarterly Rept. RTRI Japan 30, Pitarka, A., K. Irikura, T. Iwata, and H. Sekiguchi (1998). Three-dimensional simulation of the nearfault ground motion for the 1995 Hyogoken Nanbu (Kobe), Japan, earthquake, Bulletin of Seismological Society of America 88, Pacor, F., Paolucci R., Ameri G., Massa M. Puglia R. (2011). Italian strong motion records in ITACA: overview and record processing. Bulletin of Earthquake Engineering, vol. 9, 6, , doi: /s x Pieri, M., and Groppi G., (1981). Subsurface geological structure of the Po Plain (Italy). C.N.R., Prog. Fin. Geodinamica. Pubb. N. 414, Regione Emilia Romagna (1999), Carta geologica di pianura dell Emilia Romagna, A cura di D.Preti, S.E.LCA Firenze. Regione Emilia Romagna ENI-AGIP (1998), Riserve idriche sotterranee della Regione Emilia Romagna. A cura di G. Di Dio, S.E.LCA Firenze, 120 pp. Scognamiglio, L. Margheriti, F. Mele, E. Tinti, A. Bono, P. De Gori, V. Lauciani, F. P. Lucente, A. G. Mandiello, C. Marcocci, S. Mazza, S. Pintore, M. Quintiliani (2012), The 2012 Pianura Padana Emiliana Seimic Sequence: Locations and Magnitudes, Annals of Geophysics, this issue. SESAME (2004) Guidelines for the implementation of the H/V spectral ratio technique on ambient vibrations - measurements, processing and interpretations. SESAME European research project EVG1-CT , deliverable D ( Tertulliani A., L. Arcoraci, M. Berardi, F. Bernardini, B. Brizuela, C. Castellano, S. Del Mese, E. Ercolani, L. Graziani, A. Maramai, A. Rossi, M. Sbarra, M. Vecchi (2012), Emilia 2012 sequence: the macroseismic survey, Annals of Geophysics (this issue). 8

9 Figures Figure 1: Geological map (redrawn from Regione Emilia Romagna, [1999]) showing the investigated sites and the trace of two geological cross-sections. The red star locates the epicenter of the May 29th event (Ml=5.8). Legend: (5) Medium and fine sand, channel and proximal levee deposit; (6) Sandy silt, distal levee deposit; (9) Silty clay, back-swamp deposits; (10) Sand, meander belt deposit. Figure 2: Geological cross sections redrawn from Cerrina et al. [2002], crossing the Mirandola structural high (on the left-hand side), and the Casaglia structural high (on the right-hand side). Legend: (1) Lower and medium Triassic, (2) Meso-Cenozoic Carbonatic Succession, (3) Miocene, (4) Late Messinian - Early Pliocene, (5) Late Pliocene to Holocene 9

10 Figure 3: Waveforms of the north component of ground acceleration recorded along the two arrays during the May 29 th event. MIR, in the top panel, is the NS oriented array, in the western edge of the sequence area. CAS, in the bottom panel, is the NNE- SSW oriented array, in the eastern edge of the sequence area. In each panel, from bottom to top, the waveforms are arranged for increasing epicentral distance. At the right end of each waveform PGA's expressed in gal is reported. 10

11 Figure 4: Fourier amplitude spectra of the three components of acceleration recorded at station MIR2 during the earthquake of May 29 th 11

12 Figure 5: Comparison between predictions (Bindi et al., 2011) and measurements of peak ground acceleration (left) and velocity (right) for the geometric mean of the horizontal components (top) and the vertical one (bottom) for the May 29 th event. Red circle: peak values from transect stations, grey circles: peak values from INGV stations, Black crosses: RAN stations 12

13 Figure 6: Comparison between the H/V spectral ratios for earthquakes (black) and noise (red) at two sites. HVSRs are averaged over 7 events (listed in Table 2) and one standard deviation bounds are also reported 13

14 Table 1: list of studied sites (code, coordinates, equipment description and recording start) (1 Episensor, 2 Lennartz Le3d-5s) code site lat [ ] lon [ ] 1 2 from CAS01 Occhiobello X 23/05/2012 X X 30/05/2012 CAS02 Vigarano Mainarda X X 5/23/2012 CAS03 Settepolesini, Bondeno X 23/05/2012 X X 30/05/2012 CAS04 Ca' Pontoni, Vigarano Mainarda X X 5/23/2012 CAS05 San Carlo, Sant'Agostino X X 5/24/2012 CAS06 Madonna dei Boschi, P. Renatico X X 5/24/2012 CAS07 Ceramiche S.Agostino X 23/05/2012 X X 29/5/2012 CAS08 Chiesa Nuova, P. Renatico X 22/05/2012 X X 29/5/2012 MIR01 Medolla X X 24/5/2012 MIR02 Mirandola X X 22/5/2012 MIR03 Azienda VILLA, Mirandola X X 23/5/2012 MIR04 Gavello, Mirandola X X 24/5/2012 MIR05 Villa Poma X X 23/5/2012 MIR06 Pieve di Coriano X X 23/5/2012 MIR07 sede Polizia Stradale, Ostiglia X X 23/5/2012 MIR08 Quarantoli, Mirandola X X 24/5/2012 SCA01 San Carlo, centro X 29/05/2012 SCA02 San Carlo, Via Riolo X 29/05/2012 SCA03 San Carlo, contrada San Pietro X 30/05/2012 SCA04 Casumaro, Via Gazzinella X 30/05/

15 SCA05 S. Agostino,Via dei Frutteti X 09/06/2012 SCA06 S. Agostino, Via quattro torri X 09/06/2012 Table 2: Hypocentral parameters of the earthquake selected Origin time (UTC) Lat Lon Depth M :31: :00: :36: :30: :55: :39: :08: