Albarello, D.

Barani, S.

Compagnoni, M.

Lovati, S.

Martelli, L.

Mascandola, C.

Massa, M.

Pergalani, F.

Poggi, V.

C. Mascandola

M. Massa

D. Albarello

L. Martelli

S. Lovati

V. Poggi

S. Barani

F. Pergalani

M. Compagnoni

Archivio istituzionale della ricerca - Politecnico di Milano

GNGTS 2017 SeSSione 2.2383CombInInG pAssIVe-GeophysICAl And strAtIGrAphIC dAtA for A prelImInAry mAppInG of the po plAIn seIsmIC bedroCk (northern ItAly)C. Mascandola1, M. Massa1, D. Albarello2, L. Martelli3, S. Lovati1, V. Poggi, S. Barani4, F. Pergalani5,M. Compagnoni51 Istituto Nazionale di Geofisica e Vulcanologia (INGV), Milano, Italy2 Dip. di Scienze Fisiche, della Terra e dell’Ambiente, Università degli Studi di Siena, Italy3 Regione Emilia-Romagna, Servizio Geologico, Sismico e dei Suoli, Bologna, Italy4 Dip. di Scienze della Terra dell’Ambiente e della Vita, Università degli Studi di Genova, Italy5 Dip. di Ingegneria Civile e Ambientale, Politecnico di Milano, ItalyAccording to the actual Italian and European seismic codes (NTC, 2008; CEN, 2003), the transition between soft and hard soil is ascribable where the shear-wave velocity exceeds 800 m/s. This interface represents the seismic bedrock and it is of relevant importance for the seismic site effects evaluation. This issue is particularly significant in the Po alluvial basin, which is the deepest and most extended sedimentary basins in Italy. The recent case of the 2012, Mw 6.1, Emilia (Northern Italy) seismic sequence highlighted the importance of the site effects estimation in the Po Plain, where despite the low-to-moderate seismic hazard, the high density of both population and infrastructure makes this area a high seismic-risk zone.The aim of this work is to preliminary map the Po Plain seismic bedrock through the association of the available passive geophysical analysis and the known regional stratigraphic discontinuities. This study is based on an extensive collection of geophysical and geological data in the entire area. In particular:- all permanent and temporary (i.e. seismic emergency or project ) seismic stations installed in the area in the previous years and now available, for a total of 73 measure points;- 56 new single station measures of ambient noise have been performed throughout the basin in order to obtain a regular grid of equidistant measures; - 8 microtremor array measurements recently executed in the framework of several projects;- borehole data if available, in particular the cross-hole tests in Medolla, Mirandola (Paolucci et al., 2015; Laurenzano et al., 2017) and Casaglia (Laurenzano et al., 2013), besides the down-hole test in Mirabello (Minarelli et al., 2016); - a huge dataset collected by Regione Emilia-Romagna, with 60 shear-wave velocity profiles and 2000 H/V executed in the Po Plain area, has been reviewed and selected obtaining a representative subdataset composed of 47 single station measure and 15 microtremor array measurements;- regarding the stratigraphic data, different regional unconformities corresponding to different aquifers limits have been extensively mapped throughout the basin in two subsequent publications (i.e. Regione Emilia-Romagna, ENI – AGIP, 1998; Regione Lombardia, Eni Divisione Agip, 2002). These works have been the primary source of geological and stratigraphic information. However, other different studies in the Po Plain area have been considered (e.g. Pantaloni 2007; Scardia et al., 2012; Fantoni and Franciosi 2010; Fontana et al., 2014; GeoMol Team 2015; Martelli et al., 2017). All available data of ambient noise (Fig. 1) were analyzed with the Nakamura technique (Nakamura, 1989) to determine the H/V amplification function and the collected microtremor array measurements were homogeneously reprocessed to obtain the relative shear-wave velocity profile, through a joint inversion of the Rayleigh wave dispersion curve (fundamental mode only) and the ellipticity curve estimated from the H/V results. Moreover, 71 H/V curves were inverted with the Sanchez-Sesma et al. (2011) method in order to obtain the correspondent velocity profile for 71 scattered sites in the basin (Fig. 2). Based on these analyses, the H/V peaks corresponding to the seismic bedrock interface have been selected and a frequency-depth 384GNGTS 2017 SeSSione 2.2Fig. 1 - Available data of ambient noise, located throughout the basin. White triangles: H/V from permanent and temporary seismic networks; yellow triangles: H/V curves selected from the dataset of Regione Emilia-Romagna; black triangles: H/V from single station measures. Fig. 2 - Available shear-wave velocity profiles. Black stars: velocity profiles from microtremor array (i.e. data set of Regione Emilia Romagna; DPC-INGV 2014-2015 S2-seismological project; DPC-INGV 2016-2017 agreement, All. B2); white stars: velocity profiles from inverted H/V curves.empirical relation has been developed for the study area, allowing preliminary mapping the Po Plain seismic bedrock. The method proposed in Paolucci et al. (2015) for estimating depth of the resonant interfaces has also been applied and compared. In this case, the frequency-depth relation has been performed with the Eq. (1) (Ibs Von Seht and Wohlemberg, 1999),  (1)estimating the necessary coefficients (V0 and x) from curves of the average Vs values up to any value of the depth h.  GNGTS 2017 SeSSione 2.2385Finally the seismic bedrock interface has been mapped throughout the basin, showing values in general ranging between 100 m and 300 m of depth, deepening toward the Adriatic Sea, where the velocity gradients are lower and the H/V peak corresponding to the seismic bedrock interface moves at lower frequencies. The seismic bedrock interface appears related to different stratigraphic discontinuities based on the zone. In particular, in the western part of the plain near Pavia and Milano, it seems corresponding to the base of the 2nd aquifer (Regione Emilia-Romagna, ENI – AGIP, 1998; Regione Lombardia, Eni Divisione Agip, 2002), except for a few stations in the northern sector where it may be related to a deeper surface. In the central and most extended part of the Plain, it could be related to the base of the 1st aquifer (Regione Emilia-Romagna, ENI – AGIP, 1998; Regione Lombardia, Eni Divisione Agip, 2002), but for those sites in the northernmost sector (near the Garda Lake) and for some in the southernmost sector (near the Apennines) it seems still related to the base of the 2nd aquifer. For the stations in correspondence of the top of the buried structural highs of S. Colombano, Mirandola and Casaglia (Pieri and Groppi 1981; Martelli and Romani 2013), the seismic bedrock interface could be related to the base of the Quaternary sediments, in correspondence of the contact with Low-Pliocene or Miocene Marls, raised to shallow depth by buried structural highs. East of Ferrara Arc (Pieri and Groppi 1981), the seismic bedrock interface deepens toward the Adriatic Sea and it could be related to a deeper discontinuity inside the 2nd aquifer.The preliminary map of the Po Plain seismic bedrock, allows for a site effects estimation useful for both scientific and applied purpose. In particular, considering that in the target area the seismic bedrock interface lies well below the depth range (0-30 m) considered in the engineering practice (MASW, refraction, etc.), this study can be a benchmark for local seismic response analyses and new hazard studies at regional scale, when just Near-Surface Geophysics is available. ReferencesCEN; 2003: prEN 1998-1- Eurocode 8: design of structures for earthquake resistance. P1: General rules, seismic actions and rules for buildings. Draft 6, Doc CEN/TC250/SC8/N335.Fantoni R., Franciosi R.; 2010: Tectono-sedimentary setting of the Po Plain and Adriatic foreland. Rendiconti Lincei, 21(1), 197-209.Fontana A., Mozzi P., Marchetti M.; 2014: Alluvial fans and megafans along the southern side of the Alps. Sedimentary Geology, 301, 150-171.GeoMol Team; 2015: GeoMol – Assessing subsurface potentials of the Alpine Foreland Basins for sustainable planning and use of natural resources. Project Report, 188 pp. Ibs-von Seht M., Wohlenberg J.; 1999: Microtremor measurements used to map thickness of soft sediments. Bulletin of the Seismological Society of America, 89(1), 250-259.Laurenzano G., Priolo E., Barnaba C., Gallipoli M.R., Klin P., Mucciarelli M., Romanelli M.; 2013: Studio sismologico per la caratterizzazione della risposta sismica di sito ai fini della microzonazione sismica di alcuni comuni della Regione Emilia Romagna. Atti del, 32, 247-252.Laurenzano G., Priolo E., Mucciarelli M., Martelli L., Romanelli M.; 2017: Site response estimation at Mirandola by virtual reference station. Bulletin of Earthquake Engineering, 15(6), 2393-2409.Martelli L., Romani M.; 2013: Microzonazione Sismica e analisi della condizione limite per l’emergenza delle aree epicentrali dei terremoti della pianura emiliana di maggio-giugno 2012, relazione illustrativa. Servizio geologico, sismico e dei suoli Regione Emilia Romagna.Martelli L. (coord.), Bonini M., Calabrese L., Corti G., Ercolessi G., Molinari F. C., Piccardi L., Pondrelli S., Sani F., Severi P.; 2017: Carta sismotettonica della Regione Emilia-Romagna e aree limitrofe, scala 1:250.000 (edizione 2016). Con note illustrative. Regione Emilia-Romagna, SGSS; CNR, IGG sez. FI; Università degli Studi di Firenze, DST; INGV sez. BO. D.R.E.AM. Italia.Mascandola C., Massa M., Barani S., Lovati S., Santulin M.; 2017: Long-Period Amplification in  Deep Alluvial Basins and Consequences for Site-Specific Probabilistic Seismic-Hazard Analysis: An Example from the Po Plain (Northern Italy). Bulletin of the Seismological Society of America, 107(2), 770-786.Minarelli L., Amoroso S., Tarabusi G., Stefani M., Pulelli G.; 2016: Down-hole geophysical characterization of middle-upper Quaternary sequences in the Apennine Foredeep, Mirabello, Italy. Annals of Geophysics, 59(5), 0543.Nakamura Y. ; 1989: A method for dynamic characteristics estimation of subsurface using microtremor or the ground surface. Quart. Rep. Rail. Tech. Res. Inst. (RTRI), 30 (1).386GNGTS 2017 SeSSione 2.2NTC; 2008: Ministero delle Infrastrutture e dei Trasporti. Nuove Norme Tecniche per le Costruzioni. Part 3: Categorie di sottosuolo e condizioni topografiche. Gazzetta Ufficiale n. 29 del 4 febbraio 2008 (in Italian).Pantaloni M.; 2007: La nuova Carta Geologica d’Italia alla scala 1: 1.250. 000. GEOmedia, 11(3).Paolucci E., Albarello D., D’Amico S., Lunedei E., Martelli L., Mucciarelli M., Pileggi D.; 2015: A large scale ambient vibration survey in the area damaged by May–June 2012 seismic sequence in Emilia Romagna, Italy. Bulletin of Earthquake Engineering, 13(11), 3187-3206.Pieri M., Groppi G.; 1981: Subsurface geological structure of the Po Plain. Pubbl.414, PF Geodinamica, C.N.R., 23 pp.Regione Emilia-Romagna, ENI – AGIP; 1998: Riserve idriche sotterranee della Regione Emilia-Romagna. A cura di G. Di Dio. S.EL.CA. (Firenze), 120 pp.Regione Lombardia, Eni Divisione Agip; 2002: Goelogia degli acquiferi Padani della Regione Lombardia. A cura di Cipriano Carcano e Andrea Piccin. S. EL.CA. (Firenze).Sánchez-Sesma F. J., Rodríguez M., Iturrarán-Viveros U., Luzón F., Campillo M., Margerin L., Garcıa-Jerez A., Suarez M., Miguel A. Santoyo, Rodríguez-Castellanos A.; 2011: A theory for microtremor H/V spectral ratio: application for a layered medium. Geophysical Journal International, 186(1), 221-225.Scardia G., De Franco R., Muttoni G., Rogledi S., Caielli G., Carcano C., Sciunnach D.; Piccin A.; 2012: Stratigraphic evidence of a Middle Pleistocene climate-driven flexural uplift in the Alps. Tectonics, 31(6).

Combining passive-geophysical and stratigraphic data for a preliminary mapping of the Po Plain seismic bedrock (Northern Italy)

Combining passive-geophysical and stratigraphic data for a preliminary mapping of the Po Plain seismic bedrock (Northern Italy)

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