PRIOLO_FC_corretto_Layout 6 591 The Ferrara thrust earthquakes of May-June 2012: preliminary site response analysis at the sites of the OGS temporary network Enrico Priolo1,*, Marco Romanelli1, Carla Barnaba1, Marco Mucciarelli1,2, Giovanna Laurenzano1, Lorella Dall'Olio3, Nasser Abu Zeid4, Riccardo Caputo4, Giovanni Santarato4, Luigi Vignola5, Carmine Lizza5, Paolo Di Bartolomeo1 1 Istituto Nazionale di Oceanografia e di Geofisica Sperimentale (OGS), Centro di Ricerche Sismologiche (CRS), Udine and Trieste, Italy 2 Università della Basilicata, Dipartimento di Strutture, Geotecnica, Geologia Applicata all'Ingegneria (DiSGG), Potenza, Italy 3 Comune di Ferrara, Servizio Ambiente, Ferrara, Italy 4 Università di Ferrara, Dipartimento di Fisica e Scienze della Terra, Ferrara, Italy 5 MALLET s.r.l., Marsicovetere (Potenza), Italy ANNALS OF GEOPHYSICS, 55, 4, 2012; doi: 10.4401/ag-6172 1. Introduction Following the ML 5.9 earthquake that struck the Emilia area in northern Italy on May 20, 2012, at 02:03:53 UTC, and in co-operation with the personnel of the Municipality of Fer- rara and the University of Ferrara, a team of seismologists of the Istituto Nazionale di Oceanografia e Geofisica Sperimen- tale (OGS; National Institute of Oceanography and Experi- mental Geophysics) deployed a temporary seismographic network. This consisted of eight portable seismological sta- tions, to record the local earthquakes that occurred during the seismic sequence. The OGS intervention was integrated into the broader action of the emergency response to the earthquake sequence, which was promoted by the National Department of Civil Protection and the Istituto Nazionale di Geofisica e Vulcanologia (INGV; National Institute of Geo- physics and Volcanology) [Moretti et al. 2012, this volume]. The aim of the OGS intervention was on the one hand to ex- tend the seismic monitoring area towards the East, to include Ferrara and its surroundings, to be ready in case of migration of the seismicity in that direction, and on the other hand to evaluate the seismic response at the instrumented sites. Some days later, another team of researchers coordinated by the University of Potenza carried out some investigations at a number of sites, and in particular at three of the sites in- strumented by the OGS temporary network. These investi- gations consisted of passive seismic noise measurements: 1) recorded by single stations and processed by the horizontal to vertical (H/V) spectral ratio (HVSR) method; and 2) recorded by arrays and processed by the extended spatial autocorrela- tion (ESAC) method [Okada et al. 1987, Ohori et al. 2002]. In this report, we first describe in outline the seismic se- quence and the geological framework of the area. Then, we describe the OGS temporary network that was deployed. Fi- nally, we show the results obtained in the seismic noise analy- sis and the three ESAC surveys at these sites, and discuss them in the light of the information available to date on the geological structure of the area. 2. Outline of the seismic sequence and the geology of the area On May 20, 2012, at 02:03:53 UTC, the area of Emilia, which is located in northern Italy, was struck by an earthquake of magnitude ML 5.9, with the epicenter at few kilometers from the towns of Mirandola, Finale dell'Emilia and Bondeno, and about 30 km west of the city of Ferrara (Figure 1). The main earthquake sequence was followed by a new sequence of strong earthquakes nine days later, i.e., on May 29, 2012, the most relevant of which was the ML 5.8 earthquake that occurred at 07:00:03 UTC and was located nearly 12 km WSW of the main event. The seismic sequence involved the frontal sector of the northern Apennines, and in particular the buried front of the Romagna and Ferrara northward-verging active thrust belt (Figure 1). The frontal-most sector of the northern Apen- nines is represented by a fold-and-thrust belt that underlies the Po Plain and is buried by a thick wedge-like Pliocene- Quaternary depositional succession. Due to the overall geo- dynamic conditions, subsidence prevails on the locally growing anticlines, therefore generating a laterally variable sedimentary thickness with a depth to bedrock that varies from between a few hundred meters and several kilometers Article history Received July 27, 2012; accepted August 27, 2012. Subject classification: Surveys, measurements and monitoring, Ground motion, Emilia earthquake, Seismic monitoring, Seismic site response. 2012 EMILIA EARTHQUAKES (Figure 2). The geometry of this hidden chain has been rela- tively well defined by numerous seismic reflection profiles. The most important tectonic structures are represented by the Ferrara Arc and the minor Adriatic and Romagna Arcs (Figure 1). Recently, Toscani et. al. [2009] showed that some of these blind thrusts are probably still active. PRIOLO ET AL. 592 Figure 1. Simplified structural map of the eastern sector of the Po Plain, showing the major Ferrara Arc and the two minor Adriatic and Romagna Arcs. Triangles, OGS temporary seismographic stations installed around Ferrara following the earthquake sequence that started on May 20, 2012. Stars, events of the sequence with ML ≥5 (modified after [Pieri and Groppi 1981] and [CNR-PFG 1991]). Figure 2. Hydro-geological sections running in the WNW-ESE direction, through (a-a') the Casaglia structure (Ferrara); and (b-b') the Mirandola struc- ture (Modena) (modified after Pieri and Groppi [1981]). Both sections show the main aquifer bodies corresponding to the Middle-Upper Quaternary lithostratigraphic units that mainly consist of alluvial and shallow-water marine deposits that progressively infilled the Po River foreland basin (modified after Regione Emilia-Romagna and ENI-AGIP [1998]). 593 For the superficial geology of the area where the tem- porary seismographic network was installed, the outcrop- ping materials are represented by alluvial deposits of different environments, like channels and proximal levees, and inter-fluvial, meander and swamp deposits (Figure 3). As a consequence, the outcropping deposits are Holocene in age and everywhere they are substantially loose or poorly com- pacted in the first meters to decameters, and granulometri- cally they vary from clay to coarse sand. Two preliminary reports prepared by the National De- partment of Civil Protection in collaboration with other In- stitutes describe the data recorded by the national accelerom- etric network and complemented by additional data recorded by a number of temporary stations [Dolce et al. 2012a, b]. These reports bear witness to the strong ground-motion val- ues with an acceleration peak of about 0.9 g in the vertical component that was recorded during the ML 5.8 earthquake of May 29, 2012, by the Mirandola station, which was located about 2 km from the epicenter. The analysis of the seismic noise recorded at some of the stations shows a relatively pro- nounced peak of the HVSR in the frequency range of 0.6 Hz to 0.9 Hz, common to all stations. Finally, strong evidence of liquefaction phenomena were reported at several sites (e.g., San Carlo, Sant'Agostino and Mirabello), most of which were attributed to the occurrence of saturated sandy layer(s) at shal- low depths deposited along an abandoned reach of the Reno River [Papathanassiou et al. 2012, this volume]. 3. The OGS temporary network and passive-noise measurements The OGS temporary network consisted of eight stations that were deployed on May 21, 2012, the day after the main- shock. A ninth site (OG009) was set-up one month later, on June 25, 2012, as a replacement for station OG003, the loca- tion of which was no longer available. The removal of the stations was programmed for the end of July 2012. Details on the sites and the instruments used are given in Table 1, while their locations are shown in Figures 1 and 3. All of the sta- tions were set at sampling rates of 125 Hz, and they recorded data in continuous mode on temporary memory. None of the stations were equipped with data-transmission devices. The locations for the temporary stations were chosen in the area surrounding the city of Ferrara (Figures 1 and 3, Table 1). Detailed information on the temporary network FERRARA THRUST: SITE RESPONSE ANALYSIS Figure 3. Simplified geological map of the western portion of the Ferrara Province showing the locations of the OGS temporary stations (squares), the permanent stations (triangles) of the local microseismic network of the Ferrara Municipality that is managed by Ferrara University (http://servizi. comune.fe.it/index.phtml?id=2593). Stars, principal shocks of May 20, 2012. Legend of stratigraphic units: (a) medium to fine sand (channel and proxi- mal levee deposits); (b) silty clay, clay and clayey silt (interfluvial and swamp deposits); (c) sandy silt, fine sand and silty clay (distal levee deposits); (d) medium-to-coarse-grained sand (alluvial plain and meander deposits); (e) medium to fine sand (distribution channels and levee deposits); and (f ) silt, clayey silt (swamp deposits). The age of the outcropping sediments is Holocene everywhere. Modified after Banca Dati Regione Emilia-Romagna (http://geo.regione.emilia-romagna.it/geocatalogo/). can be found in the OGS Archive System of Instrumental Seismology (OASIS; oasis.crs.inogs.it) [Priolo et al. 2011], under the network code ZR. Here, we provide a short overview of the sites: OG001 was located East of Ferrara, in the basement of the new city hospital located at Cona. OG002 was inside a warehouse of the Ferrara Munici- pality, in front of the Chemical Industry of Ferrara, on a floor made of a concrete slab. The building is quite large, and it has a rectangular shape. The sensor was at the base of a NS- oriented wall. OG003 was deployed on farmland near the town of Sant'Agostino, a few meters from a small sand-liquefaction boil (about 3-4-m wide) that occurred during the mainshock of May 20, 2012. This accelerometer was buried in sandy soil in a 50-cm-deep hole. OG004 was deployed in Ficarolo village, in the garden of the building of a branch of the Law Courts. The Lennartz 5s sensor was buried in sandy soil at a depth of about 70 cm. OG005 was located in Poggio Renatico, in the courtyard of a private house. OG006 was located in a private box-car in Vigarano Pieve. OG007 was in the utility room of a private house in Aguscello. OG008 was in Mirabello on the ground of a box near to a free parking area of a restaurant, where several cracks in the ground were observed after the mainshock. OG009 was deployed in the basement of the church of San Carlo, where diffuse liquefaction phenomena were in- duced by the mainshock. Here, the whole floor, which was a concrete slab in a ca. 10 m × 10 m hall in the church base- ment, was uplifted by about 50 cm to 80 cm, due to sand in- jection. As already indicated, this site replaced OG003, and it was set-up one month later than the others. Unfortunately, there were some problems when the first dump of data was analysed, such that some data were lost or not usable (e.g., saturation for the largest events). However, this is not relevant for the aims of the present re- port, and will be considered in a later report. The group of Potenza University took passive noise measurements at sites OG003, OG006 and OG008. Single station measurements were performed using the Tromino® instrument, while for the array measurements, the Geode 24-channel modular acquisition system by Geometrics was used, equipped with Geospace 4.5 Hz geophones. Some tests were performed to verify the consistency of the noise measurements performed by the two different kinds of instrument. As a result, excellent agreement was found between the HVSRs calculated from the passive noise measurements using the OGS and the Tromino® instru- mentation in the frequency band of 0.3 Hz to 15 Hz, of in- terest for this study. 4. HVSR and ESAC results Figure 4 shows the HVSRs calculated from the single station measurements. The ratios were aligned along two hypothetical transects that run SW-NE (Transect 1: with sta- tions OG003, OG005 [as a lateral extension], OG008, OG006) and SE-NW (Transect 2: OG001, OG007, OG002, OG006, OG004), as shown in Figure 3. Note that Transects 1 and 2 are orthogonal and normal, respectively, to the main geological structures. The HVSRs shows relatively good co- herence; e.g., an evident, although spread, low frequency peak, at a frequency between 0.5 Hz to 1.5 Hz. In some cases, this peak is sharper, as for OG002, OG006 and OG007, while for other sites, such as OG004 and OG008, it is much broader. The amplitude of these peaks is always weak, and the HVSR ranges from 2.0 to 4.2. Figure 5 and Table 2 give the vertical profiles of the shear-wave velocity (Vs) inverted for sites OG003, OG006 and OG008 through the ESAC method, from passive noise measurements of the array and with the additional con- straint of the HVSR calculated from single station noise. The details of the array geometries are shown in Figure 6. The actual array length and the resulting investigation depth were, respectively: 345 m and 120 m for OG003; 330 m and 110 m for OG006; and 340 m and 120 m for OG008. In all PRIOLO ET AL. 594 Code Sito Epicentral distance (km) Start Recording Lat Lon Acquisition Unit Sensor OG001 Cona - Ospedale Nuovo 40.9 2012/05/25 44.78921 11.727598 Nanometrics Orion Lennartz 1s 3D Light OG002 Comune di Ferrara - Lavori Pubblici 29.5 2012/05/25 44.85249 11.59847 Nanometrics Orion Lennartz 1s 3D Light OG003 Sant'Agostino 16.7 2012/05/25 44.786163 11.38337 Reftek 130 Episensor OG004 Ficarolo (RO) 17.6 2012/05/25 44.952037 11.433883 Reftek 130 Lennartz 5s OG005 Poggio Renatico 24.3 2012/05/25 44.766983 11.48494 Nanometrics Orion Lennartz 1s 3D Light OG006 Vigarano Pieve 22.8 2012/05/25 44.861937 11.514676 Nanometrics Orion Lennartz 1s 3D Light OG007 Aguscello 35.6 2012/05/25 44.806519 11.663715 Nanometrics Orion Lennartz 1s 3D Light OG008 Mirabello 18.1 2012/05/25 44.812673 11.431863 Nanometrics Orion Lennartz 1s 3D Light OG009 San Carlo 16.9 2012/06/25 44.804401 11.408932 Reftek 130 Episensor Table 1. Detail of the OGS temporarty network 595 FERRARA THRUST: SITE RESPONSE ANALYSIS Figure 4. Single station seismic noise HVSRs estimated along the two tran- sects shown in Figure 3. Transect 1 (right) runs in the SW-NE direction and includes stations OG003, OG005 (about 6 km out of line), OG008 and OG006. Transect 2 (left) runs in the SE-NW directions and includes sta- tions OG001, OG007, OG002, OG006 and OG004. The H/V peak value is specified for each curve. Figure 5. Vs estimation by the ESAC method at the OG003, OG006 and OG008 sites. Table 2. Velocity and depth estimates using the extended spatial autocor- relation method at the OG003, OG006 and OG008 sites. Site Depth (m) Vs (m/s) OG003 0.0 – 5.86 106 5.86 – 22.76 152 22.76 – 83.24 305 > 83.25 556 OG006 0.0 – 11.5 146 11.5 – 29.0 250 29.0 – 101 337 > 101 645 OG008 0.0 – 11.30 120 11.30 – 30.20 215 30.20 – 80.80 337 > 80.80 515 cases, a four-layer model was used in the inversion. Sites OG006 and OG008 features relatively similar structures: the Vs started with very low values at the surface, which ranges from 120 m/s to 150 m/s in the shallow-most 10 m, and in- creases with depth, with values of about 215 m/s to 250 m/s at a depth of ca. 20 m to 30 m, and then of 337 m/s for a fur- ther ca. 50 m. While the Vs appears to increase uniformly for OG008 also at greater depths, with a value of 515 m/s, a ve- locity contrast is imaged for site OG006 at a depth of 95 m to 110 m, where the velocity jumps to 645 m/s. The HVSRs of those two sites (Figure 4) conform very well to this inter- pretation, with OG008 showing a much broader and smoother peak than that of OG006. Site OG003 has even lower velocity values than the pre- vious sites. We note here that some particular events of sand liquefaction occurred here. The Vs ranges from ca. 100 m/s at the surface, for the shallow-most 6 m, and progressively increases at about 150 m/s from 6 m to 22 m, and 305 m/s from 22 m to 83 m. Again, relatively weak contrast is seen at 80 m to 90 m of depth, where the Vs reaches 550 m/s. PRIOLO ET AL. 596 Figure 6. Array geometry (yellow lines) of the ESAC surveys performed at the OG003, OG006 and OG008 sites. For each site, a map and a list of the geo- phone coordinates are shown. The location of the temporary station is indicated by a white square in each map. The array geometry consists of two nearly orthogonal branches. The array length specified in the text is the total length of the two branches. 597 5. Discussion and conclusions All of the eight sites of the OGS temporary network an- alyzed in this study features common HVSR characteristics; i.e., a weak and broad peak of fundamental resonant fre- quency in the low frequency band from 0.5 Hz to 1.5 Hz. The ESAC investigations performed at three sites shows that this peak was caused by a weak S-velocity contrast at depth of ca. 80 m to 100 m. Above, the S-velocity progressively in- creases with depth, starting from very low values of about 100 m/s to 150 m/s at the surface, to 300 m/s to 340 m/s at a depth of 80 m to 100 m. Beneath that depth and down to the investigation depth of about 110 m to 120 m, the S-ve- locity settles at 500 m/s to 550 m/s, although site OG006 has a higher velocity, of 650 m/s. Coherently, the sharpest HVSR curve is estimated at this site. The very low velocities at the surface corresponds to co- hesionless soils that are characterized by very low shear-mod- ulus values, such as the sandy and silty-sandy soils that are commonly found in that area. This study provides just the preliminary results: for instance, it does not provide the ac- tual spectral amplification of the investigated sites. More thorough data will follow from the analysis of the recorded earthquakes. Finally, at site OG0004, which is the northern-most site of Transect 2 (Figure 2), the HVSR features a very broad, low-frequency lobe, with two distinct peaks at 0.3 Hz to 0.4 Hz and at 0.9 Hz (Figure 4). While the latter is well corre- lated to that of the other transect stations, the peak at the lowest frequency might indicate the presence of a deeper, structural S-velocity contrast. This hypothesis agrees rela- tively well with the thickening of the sediments previously documented in the area of Ficarolo (Figure 2), where station OG004 was located. Acknowledgements. We thank Elisa Zambonelli of the National Department of Civil Protection, and Lucia Margheriti of the Istituto Nazionale di Geofisica e Vulcanologia (INGV), who gave us many impor- tant pieces of information and helped us to keep tightly coordinated with the interventions of their Institutes. References CNR-PFG (Progetto Finalizzato Geodinamica) (1991). Syn- thetic structural-kinematic map of Italy. Structural model of Italy, Sheet n. 5, S.EL.CA., Firenze. Dolce, M., M. Nicoletti, A. Ammirati, R. Bianconi, L. Fil- ippi, A. Gorini, S. Marcucci, F. Palma, E. Zambonelli, G. Lavecchia, R. de Nardis, F. Brozzetti, P. Boncio, D. Cir- illo, A. Romano, G. Costa, A. Gallo, L. Tiberi, G. Zoppé, P. Suhadolc, F. Ponziani and A. Formica (2012a). The Emilia Thrust Earthquake of 20 May 2012 (Northern Italy): Strong Motion and Geological Observations - Re- port 1, National Civil Protection Department (DPC); http://www.protezionecivile.gov.it/jcms/it/ran.wp Dolce, M., M. Nicoletti, A. Ammirati, R. Bianconi, L. Filippi, A. Gorini, S. Marcucci, F. Palma, E. Zambonelli, G. Lavec- chia, R. de Nardis, F. Brozzetti, P.Boncio, D. Cirillo, A. Ro- mano, G. Costa, A. Gallo, L. Tiberi, G. Zoppé, P. Suhadolc, F. Ponziani and A. Formica (2012b). The Fer- rara Arc Thrust Earthquakes of May-June 2012 (North- ern Italy): Strong-Motion and Geological Observations - Report II, National Civil Protection Department (DPC); http://www.protezionecivile.gov.it/jcms/it/ran.wp Moretti, M., et al. (2012). Rapid response to the earthquake emergency of May 2012 in the Po Plain, northern Italy, Annals of Geophysics, 55 (4); doi:10.4401/ag-6152. Ohori, M., A. Nobata and K. Wakamatsu (2002). A compar- ison of ESAC and FK methods of estimating phase ve- locity using arbitrarily shaped microtremor arrays, B. Seismol. Soc. Am., 92, 2323-2332. Okada, H., K. Matsushima and E. Hidaka (1987). Compari- son of spatial autocorrelation method and frequency- wavenumber spectral method of estimating the phase velocity of Rayleigh waves in long-period microtremors, Geophys. B. Hokkaido Univ. 49, 53-62 (in Japanese with English abstract). Papathanassiou, G., R. Caputo and D. Rapti-Caputo (2012). Liquefaction phenomena along the palaeo-Reno River caused by the May 20, 2012 Emilia (northern Italy) earth- quake, Annals of Geophysics, 55 (4); doi:10.4401/ag-6147. Pieri, M., and G. Groppi (1981). Subsurface geological struc- ture of the Po Plain, Italy. Consiglio Nazionale delle Ricerche, Progetto finalizzato Geodinamica, Sottopro- getto Modello Strutturale, Roma, 414, 13 pp. Priolo, E., G. Laurenzano, C. Barnaba, P. Bernardi, L. Moratto and A. Spinelli (2011). OASIS – The OGS Archive System of Instrumental Seismology, In: M. Mucciarelli (ed.), Tecniche Speditive per la Stima dell'Amplificazione Simica. Studi teorici ed applicazioni professionali, Roma, Aracne editrice, 445 pp. Regione Emilia-Romagna and ENI-AGIP (1998). Riserve idriche sotterranee della Regione Emilia-Romagna, ed- ited by G. Di Dio, Firenze, S.El.Ca., 120 pp. Toscani, G., P. Burrato, D. Di Bucci, S. Seno and G. Valen- sise (2009). Plio-Quaternary tectonic evolution of the northern Apennines thrust fronts (Bologna-Ferrara sec- tion, Italy): seismotectonic implications, B. Soc. Geol. Ital., 128, 605-613. *Corresponding author: Enrico Priolo, Istituto Nazionale di Oceanografia e di Geofisica Sperimentale (OGS), Centro di Ricerche Sismologiche (CRS), Udine and Trieste, Italy; email: epriolo@ogs.trieste.it. © 2012 by the Istituto Nazionale di Geofisica e Vulcanologia. All rights reserved. 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