Quaternary Geology and Paleoseismology in the Fucino and L’Aquila Basins

Geological Field Trips

Società Geologica Italiana

2016 Vol. 8 (1.2) ISPRA Istituto Superiore per la Protezione e la Ricerca Ambientale

SERVIZIO GEOLOGICO D’ITALIA Organo Cartografico dello Stato (legge N°68 del 2-2-1960) Dipartimento Difesa del Suolo

ISSN: 2038-4947

Quaternary geology and paleoseismology in the Fucino and L’Aquila basins

6th INQUA International Workshop on Active Tectonics Paleoseismology and Archaeoseismology Pescina (AQ) - Italy

Sara Amoroso1, Filippo Bernardini2, Anna Maria Blumetti3, Riccardo Civico4, Carlo Doglioni5, Fabrizio Galadini1, Paolo Galli6, Laura Graziani4, Luca Guerrieri3, Paolo Messina7, Alessandro Maria Michetti8, Francesco Potenza9, Stefano Pucci4, Gerald Roberts10, Leonello Serva11, Alessandra Smedile1, Luca Smeraglia5, Andrea Tertulliani4, Giacomo Tironi12, Fabio Villani1, Eutizio Vittori3

1 INGV, L’Aquila. 2 INGV, Bologna. 3 ISPRA, Rome. 4 INGV, Rome. 5 Dip. Sc. della Terra, Univ. “La Sapienza”, Rome. 6 Dip. Prot. Civile, Rome. 7 CNR- IGAG, Montelibretti, Rome. 8 Univ. dell’Insubria, Como. 9 Dep. of Civil, Arch. Env. Eng., Univ. of L'Aquila. 10 Birbeck Univ., London, UK. 11 Independent Consultant, Rome. 12 Studio Eng. Giacomo Tironi, L'Aquila.

Corresponding Author e-mail address: [email protected]

Responsible Director Claudio Campobasso (ISPRA-Roma) Editorial Board Editor in Chief Gloria Ciarapica (SGI-Perugia) M. Balini, G. Barrocu, C. Bartolini, 2 Editorial Responsible D. Bernoulli, F. Calamita, B. Capaccioni, Maria Letizia Pampaloni (ISPRA-Roma) W. Cavazza, F.L. Chiocci, R. Compagnoni, D. Cosentino, Technical Editor S. Critelli, G.V. Dal Piaz, C. D'Ambrogi, Mauro Roma (ISPRA-Roma) P. Di Stefano, C. Doglioni, E. Erba, publishing group R. Fantoni, P. Gianolla, L. Guerrieri, Editorial Manager Maria Luisa Vatovec (ISPRA-Roma) M. Mellini, S. Milli, M. Pantaloni, V. Pascucci, L. Passeri, A. Peccerillo, Convention Responsible L. Pomar, P. Ronchi, B.C. Schreiber, Anna Rosa Scalise (ISPRA-Roma) L. Simone, I. Spalla, L.H. Tanner, Alessandro Zuccari (SGI-Roma) C. Venturini, G. Zuffa. ISSN: 2038-4947 [online]

http://www.isprambiente.gov.it/it/pubblicazioni/periodici-tecnici/geological-field-trips

The Geological Survey of Italy, the Società Geologica Italiana and the Editorial group are not responsible for the ideas, opinions and contents of the guides published; the Authors of each paper are responsible for the ideas, opinions and contents published. Il Servizio Geologico d’Italia, la Società Geologica Italiana e il Gruppo editoriale non sono responsabili delle opinioni espresse e delle affermazioni pubblicate nella guida; l’Autore/i è/sono il/i solo/i responsabile/i. DOI: 10.3301/GFT.2016.02 Quaternary geology and paleoseismology in the Fucino and L’Aquila basins S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Michetti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori INDEX geological fieldtrips2016-8(1.2) Information

Abstract ...... 4 STOP 1.2 – Paleoseismology and long-term activity along the Riassunto ...... 4 Magnola fault (Fonte Capo La Maina, Forme) ...... 37 Program ...... 5 STOP 1.3 – Cerchio-Collarmele tectonic terraces: long-term General information ...... 6 activity along the Cerchio-Pescina fault ...... 42 Safety ...... 6 STOP 1.4 – The Serrone fault escarpment ...... 45 STOP 1.5 – The Venere quarries: surface faulting of the 1915 Excursion notes earthquake and paleoseismic evidence ...... 53 STOP 1.6 – 1915 coseismic rupture in the lake sediments and 1. Geological and geodynamic framework of Central trench logs ...... 58 Apennines ...... 8 2. The Fucino basin ...... 16 DAY 2 - Quaternary geology and palaeosismology in Tectonic setting ...... 16 the L’Aquila basin ...... 63 Geomorphologic setting ...... 16 STOP 2.1 - Panoramic view from San Martino d'Ocre ...... 64 Paleoseismic data ...... 21 STOP 2.2 - San Demetrio Ne’ Vestini - Quaternary composite 3 Evolutionary model of the Fucino basin ...... 22 fault scarps and paleoseismological investigations ...... 65 3. The middle Aterno Valley and L’Aquila city ...... 24 STOP 2.3 - Poggio Picenze - Early Pleistocene lacustrine The 2009 earthquake ...... 24 deposits ...... 67 Geological setting – middle Aterno Valley ...... 25 STOP 2.4 - Le Macchie - Early Pleistocene Gilbert fan delta Structural setting - middle Aterno Valley ...... 26 conglomerates ...... 68 Geological setting – L’Aquila city ...... 29 STOP 2.5 - Valle dell’Inferno - The syntectonic deposition and The 2009 earthquake in L’Aquila city ...... 33 drainage evolution ...... 69 South L’Aquila ...... 34 STOP 2.6 - South L’Aquila ...... 71 STOP 2.7 - Piazza Duomo ...... 73 Itinerary STOP 2.8 - Piazza Palazzo ...... 75 STOP 2.9 - Via San Bernardino ...... 76 index Day 1 - Quaternary geology and palaeosismology in STOP 2.10 - Palazzo Ardinghelli ...... 77 the Fucino basin ...... 35 STOP 2.11 - Castello Cinquecentesco ...... 79 STOP 1.1 - Landscape view of the Fucino basin from Mt. Salviano and general introduction ...... 36 References ...... 81

Abstract geological fieldtrips2016-8(1.2)

This 2 days-long field trip aims at exploring field evidence of active tectonics, paleoseismology and Quaternary geology in the Fucino and L’Aquila intermountain basins and adjacent areas, within the inner sector of Central Apennines, characterized by extensional tectonics since at least 3 Ma. Each basin is the result of repeated strong earthquakes over a geological time interval, where the 1915 and 2009 earthquakes are only the latest seismic events recorded respectively in the Fucino and L’Aquila areas. Paleoseismic investigations have found clear evidence of several past earthquakes in the Late Quaternary to Holocene period. Active tectonics has strongly imprinted also the long-term landscape evolution, as clearly shown by numerous geomorphic and stratigraphic features. Due to the very rich local historical and seismological database, and to the extensive Quaternary tectonics and earthquake geology research conducted in the last decades by several Italian and international teams, the area visited by this field trip is today one of the best studied paleoseismological field laboratories in the world. The Fucino and L’Aquila basins preserve excellent exposures of earthquake environmental effects (mainly surface faulting), their cumulative effect on the landscape, and their interaction with the urban history and environment. This is therefore a key region for understanding the role played by earthquake environmental effects in the Quaternary evolution of 4 actively deforming regions, also as a major contribution to seismic risk mitigation strategies.

Keywords: Quaternary geology, paleoseismology, tectonic terraces, intermountain basin, surface faulting, fault scarp, seismic hazard

Riassunto information

L’escursione ha una durata di due giorni ed è focalizzata sull’evoluzione quaternaria, la tettonica attiva e la paleosismologia dei bacini intermontani del Fucino e de L’Aquila ed aree limitrofe (Appennino Centrale). La tettonica estensionale è attiva in quest’area da almeno 3 milioni di anni. Ciascun bacino, delimitato da versanti e scarpate di faglia, è il risultato della sommatoria di più eventi di fagliazione superficiale in un intervallo di tempo geologico in cui gli eventi del 1915 e del 2009 sono i più recenti che hanno prodotto fagliazione in superficie nei due bacini.

DOI: 10.3301/GFT.2016.02 Quaternary geology and paleoseismology in the Fucino and L’Aquila basins S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Michetti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Grazie alla grande disponibilità di dati storici e sismologici ed alle numerose ricerche sulla tettonica attiva e paleosismologia condotte negli ultimi decenni da numerosi gruppi di ricercatori italiani e stranieri, la zona geological fieldtrips2016-8(1.2) attraversata dall’escursione è una delle più conosciute dal punto di vista paleosismologico. Queste indagini hanno consentito di riconoscere le evidenze stratigrafiche di diversi terremoti avvenuti nel periodo tardo Quaternario – Olocene. La tettonica attiva ha inoltre fortemente condizionato anche l’evoluzione a lungo termine del paesaggio, come chiaramente mostrato da numerose caratteristiche stratigrafiche e geomorfologiche. Nei bacini del Fucino e de L’Aquila sono dunque riconoscibili gli effetti geologici cosismici (prevalentemente fagliazione superficiale), ed il loro effetto cumulato sul paesaggio, e la loro interazione con la storia urbana e l’ambiente. Per questo motivo, è considerata una regione chiave per la comprensione del ruolo giocato dagli effetti geologici cosismici nell’evoluzione quaternaria di regioni in deformazione attiva, anche come importante contributo alle strategie di mitigazione del rischio sismico.

Parole chiave: geologia del Quaternario, paleosismologia, terrazzi tettonici, bacini intermontani, superfice di faglia, scarpata di faglia, pericolosità sismica

Program 5 The area covered by this field trip is located in Abruzzo (Central Italy), and in particular in the L’Aquila province. This area can be easily reached by the A24 (Roma-L’Aquila-Teramo) and A25 (Roma-Pescara) motorways. The area can also be reached by train, stopping at the stations of Avezzano and Pescina, on the line Roma-Pescara. The first day of the excursion focuses on the Fucino basin: after a panoramic view from its western border (Stop 1.1), the geomorphic and paleoseismic evolution of the northern border will be examined in detail along the Magnola fault (Stop 1.2) and along the Cerchio-Pescina-Parasano fault (Stop 1.3). The remaining stops will information explore in detail the paleoseismic evidence along the eastern border, including the evidence of the 1915 coseismic rupture, and in particular along the Serrone fault (Stop 1.4) and the San Benedetto-Gioia de’ Marsi fault (Stops 1.5 and 1.6). In the second day, we will move to the L’Aquila basin and middle Aterno Valley. Specific focus will be on active tectonics and paleoseismology along the middle Aterno Valley fault (Stops 2.1 and 2.2). Stops 2.3, 2.4 and 2.5 will detail the Quaternary geology of the same area. In the afternoon, we will move to L’Aquila city center, to observe the macroseismic effects caused by the 2009 L’Aquila earthquake (Stops 2.6 to Stops 2.11). DOI: 10.3301/GFT.2016.02 Quaternary geology and paleoseismology in the Fucino and L’Aquila basins S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Michetti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori General information geological fieldtrips2016-8(1.2) The best periods to undertake this field trip, in terms of climatic and expected weather conditions, are April-June and September-October. In July and August, temperatures are hot. In November and winter temperatures are cold and climate is wetter with frequent snowfalls. The average weather conditions are the following: Spring: T min = 5 °C, T max = 18 °C, Rainfall = 60 mm per month, Humidity = 72 %; Summer: T min = 15 °C, T max = 29 °C, Rainfall = 40 mm per month, Humidity = 70 %, Sudden storms can be frequent; Fall: T min = 6 °C, T max = 16 °C, Rainfall = 75 mm per month, Humidity = 75 %.

In all seasons a waterproof coat/jacket is recommended. From June to September sun protection and hats are 6 recommended. All participants need comfortable hiking boots. A rucksack is necessary to carry rain protection, spare clothing (T-shirt or a fleece/sweater), a packed lunch, water and snacks.

Safety information The aim of this document is to collate key information into a simple format for use by field and on-call staff in the event of an accident. Safety in the field is closely related to awareness of potential difficulties, fitness and use of appropriate equipment. Safety is a personal responsibility and all participants should be aware of the following issues. DOI: 10.3301/GFT.2016.02 Quaternary geology and paleoseismology in the Fucino and L’Aquila basins S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Michetti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori - The excursion takes place at moderate altitudes (between 650 and 1100 meters a.s.l.).

- Most of the outcrops are along the road and long walks are never scheduled geological fieldtrips2016-8(1.2) - Trainer or running shoes are unsuitable footwear in the field. - A waterproof coat/jacket is essential. - Each vehicle needs to carry one basic first aid kit. - Mobile/cellular phone coverage is good although in some remote places there is no signal.

Emergency Services

In case of emergency please contact the following numbers (valid all over Italy) - Medical Emergency/Ambulance: 118 - Police: 113 or 112 - Firemen: 115

Medical Facilities in the area 7 The nearest hospitals are - 1st day (Fucino): Ospedale SS. Filippo e Nicola, Via G. di Vittorio, 67051 Avezzano (AQ), Tel.: +39-0862-3681 - 2nd day (L’Aquila): Ospedale Regionale San Salvatore, Via Vetoio, 1, 67100 Coppito, L’ Aquila (AQ), Tel.: +39- 08634991 information

DOI: 10.3301/GFT.2016.02 geological field trips 2016 - 8(1.2)

8 excursion notes etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins 5) main 9) foredeep crystalline 2) 6) Alpine orogen; 4) foreland areas; Apenninic water divide; Apenninic water 1) domains characterized by a domains characterized 8) oceanic crust in the Provençal basin oceanic crust in the Provençal faults. From Scrocca et al., 2003. faults. From Scrocca et al., 3) 7) 10) Fig. 1 - Synthetic tectonic map of Italy and Fig. 1 - Synthetic thrusts; areas affected by extensional tectonics: these basin system can be considered as a back-arc roll-back of the in response to the eastward developed Apenninic subduction; west-directed surrounding seas; deposits; basement; Sea (Plio- (Miocene in age) and the Tyrrhenian oceanic crust in Pleistocene in age) and old mesozoic the Ionian basin; compressional tectonic regime; DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. 1. Geological and geodynamic framework of Central Apennines Apennines are the midmost part of The Central oriented, late the Apennines chain, a NW-SE Oligocene-Present fold and thrust belt, that composes the backbone of Italian peninsula (Fig. 1). successions stratigraphical The Meso-Cenozoic on Apennines developed cropping out in Central margin, where passive the southern Neotethyan in the area a basin-platform system developed as a consequence of rifting stage that affected region during the lower the whole Neotethyan related to the The paleogeography Jurassic. basin-platform system was lower Jurassic times. persistent until early Tertiary geological field trips 2016 - 8(1.2)

9 excursion notes 6) 7) buried 3) Plio-Pleistocene isobaths in meters of 1) 11) Meso-Cenozoic deep-water Meso-Cenozoic 8) Pleistocene volcanics; Pleistocene volcanics; carbonate platform deposits 2) limestones; clastic deposits related to the Messinian/Early Messinian clastic deposits and evaporites; Messinian clastic deposits and evaporites; 4) undifferentiated fault; 5) w-water platform domain was broken-up and new 10) w-water thrust; w-water 9) Lepini Mts., Ausoni Mts., Aurunci Mts., Ernici Mts., Aurunci Mts., Ausoni Mts., Lepini Mts., etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 2 - Geological map of the central Apennines. Fig. 2 - Geological map of the central project (Fig. 5). Modified from Cosentino et al., 2010. project (Fig. 5). Modified from Cosentino et al., marine and continental deposits; Pliocene marine sediments; limestones; the base of the Pliocene deposits. Dotted line indicates the trace of CROP 11 the base of Pliocene deposits. Dotted line indicates trace Pliocene thrust-top basins; Pliocene thrust-top foredeep siliciclastic deposits of undifferentiated age (Upper Miocene); Meso-Cenozoic shallo The pre-rifting Triassic rocks, outcropping in Central The pre-rifting Triassic carbonate platform and Apennines belong to shallow water that led to depositions of euxinic basins paleo-environments carbonates, dolostones and sulfates about shallow-marine 1986). The lower Jurassic 1.5-2 km thick (Bally et al., rifting is Jurassic tectonic phase related to the Neotethys records of Central stratigraphic evident in the Mesozoic 2010). Apennines (Cosentino et al., The shallo being characterizedplatform-basin systems developed, by to deep- downthrown sectors dominated by transitional sedimentation, with deposition of limestones, marly water Sasso Chain, Morrone limestones, and marls (Fig. 2, Gran Le Mainarde Mts. and Majella area), upthrown Mts., sectors with shallo (Fig. 2, Simbruini Mts. and Marsica area). The early-medium quite similar to that was Cretaceous regional paleogeography and the platform-basin systems led to of the late Jurassic carbonate and deep-water deposition of thick shallow- 1986). successions (up to 4-6 km thick, Bally et al., DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) excursion notes 10 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 3 - The early “east”-directedfollowed Alpine subduction was relative to the mantle (From Carminati & Doglioni, 2005). relative by the Apennines “west”-directed along subduction, which developed the retrobelt of preexisting Alps. The slab is steeper underneath drift of the lithosphere the Apennines, possibly due to “westward” DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. In the platform domain, a late Cretaceous-early followed by deposition of early Miocene hiatus was carbonates, deposited along Miocene paraconformable 2005), while in (Civitelli & Brandano, a carbonate ramp the deeper domains sedimentation continued throughout the Paleogene. During Eocene-Oligocene times a critical scenario area, Mediterranean in the proto-western developed Alpine with the existence of S-SE-directed subduction system (approaching the end of its Apennine NW-dipping existence) and the young subduction system starting its activity (Doglioni et al., 2012), which possibly developed 1998; Carminati et al., (Fig. 3). along the retrobelt of Alpine orogeny This means that two subduction systems, with nearly narrow area for were present in a relatively opposite polarity, a short time. passive During the late Miocene, southern Neotethyan of the Apennines, that in the evolution involved margin was margin during the of the passive accreted the sedimentary cover Apennines subduction roll-back of the NW-dipping “eastward” also confirmed by the system (Fig. 4) (Doglioni, 1991). This was geological field trips 2016 - 8(1.2) excursion notes 11 2) lower part of the 6) Apennine sole-thrust. Density values 8) “stripped units” in the gravity model; “stripped units” in the gravity 1) lower crust; 7) Lower part of the sediantary cover; Lower part of the sediantary cover; etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. 5) Quaternary geology and paleoseismology in the Fucino L’Aquila basins other carbonate units (or having similar density): upper part of the other carbonate units (or having 4) Apulian Platform units; 3) ) and distribution are from the gravity model of Di Luzio et al., 2009. Circles indicate local estimates of Moho depth from model of Di Luzio et al., ) and distribution are from the gravity 3 Fig. 4 - Tectonic models of subduction the Adriatic continental crust. Fig. 4 - Tectonic stations 6-12 and FRES projected on the CROP 11 profile. From Di Luzio et al., 2009. stations 6-12 and FRES projected on the CROP 11 profile. From Di Luzio et al., (g/cm Tyrrhenian upper crust; Tyrrhenian Paleozoic-Triassic sequence, undeformed, and crystalline basement; Paleozoic-Triassic Paleozoic- Triassic sequence, involved in thrusting deformation; sequence, involved Triassic Paleozoic- DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. interpretation of CROP 11 line (Fig. 5), a deep seismic profile across the Central Apennines (Fig. 2). The interpretation of CROP 11 line (Fig. 5), a deep seismic profile across the Central been Apennines slab roll-back induced subsidence and boudinage of large portions the Alps that have (Fig. 3) and the Tyrrhenian scattered and dismembered into the Apennines-related backarc basin: Provencal 1998). (Doglioni et al., sedimentary basins are Apennines tectonically-controlled Within this geodynamical setting, in the Central 2007), followed (Carminati et al., with the deposition of hemipelagic marls in a foreland environment developed by deposition of turbidites composed siliciclastic sandstones in a foredeep setting ahead the propagating 1991; Milli & Moscatelli, et al., 1991; Patacca & Scandone, 1989; Cipollari Cosentino, front (Patacca deformative geological field trips 2016 - 8(1.2) excursion notes 12 = C.B. =Casoli- CA-BO Paleozoic-Triassic sequence; Paleozoic-Triassic P-T etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins = Undifferentiated Mio-Pliocene belt; = Undifferentiated Apulian Platform. Siliciclastic units involved in the Apennine = Undifferentiated Apulian Platform. Siliciclastic units involved UMPB UAP = Lower Crust; Moho depths estimated from receiver functions are projected on the CROP 11 = Lower Crust; Moho depths estimated from receiver L.C. = Maiella unit, = Molise nappes, MN MAI Fig. 5 - Crustal geologic section along the CROP 11 profile from the axial zone of the belt (Fucino basin) to Adriatic Fig. 5 - Crustal geologic section along the CROP 11 profile from axial zone extensional faults, bordering intra-mountain basins, cutting throughout the crust. Modified From Di Luzio et al., 2009. basins, cutting throughout the crust. Modified From Di Luzio et al., extensional faults, bordering intra-mountain Bomba unit, deformation: foreland (See Fig. 2 for the location of CROP 11 trace). Carbonatic units involved in the Apennine deformation: Carbonatic units involved foreland (See Fig. 2 for the location of CROP 11 trace). Cristalline Basement; following the shallow structural axis (black circles) and the minimum-distance path (white circles). Red faults are the main axis (black circles) and the minimum-distance path (white circles). Red following the shallow structural DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) excursion notes 13 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 6 - Chronostratigraphical scheme adopted for the analysis of Fig. 6 - Chronostratigraphical recognizable in the study area. From Cosentino et al., 2010. recognizable in the study area. From Cosentino et al., syn-tectonic terrigenous deposits of the Central Apennines. In the right syn-tectonic terrigenous deposits of the Central the are shown. For Apennine tectonic events Central the recognized half, foredeep stage (in white) no siliciclastic deposits are Serravallian 2000; Critelli et al., 2007). North-eastward migration of thrust migration 2007). North-eastward 2000; Critelli et al., different tectonic units that 1995) developed fronts (Cipollari et al., onto turbiditic basins brought carbonate ridges, oriented NW-SE, 1990; Cipollari et al., (Fig. 2) (Ricci Lucchi, 1986; Boccaletti et al., 2010). & Scandone, 2001; Cosentino et al., 1995; Patacca tectonic Across the suite of both extensional and compressive front, from of the deformative features, a space-time rejuvenation the western to eastern part of Apennines, is recognizable 1995). & De Celles, 1999; Cipollari et al., (Fig. 6) (Cavinato subduction and applying the kinematics of W-dipping Following drift of the lithosphere, Apennines should float the westward a new asthenospheric mantle, which replaced the above subducted lithosphere, causing the uplift of accretionary wedge of the Apennines chain (Fig. 7) (Doglioni, 1991). by a frontal active the Apennines are characterized Nowadays accretionary wedge, below the Adriatic sea, whereas inland ridge is instead in uplift and extension, controlled by elevated (Fig. 1) (Doglioni & tensional regime oriented about NE-SW Flores, 1995). DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) excursion notes 14 n) boudinated etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 7 - Cross section from Corsica (SW), through Tyrrhenian Sea and across the Apennines (NE). The prism (light gree Fig. 7 - Cross section from Corsica (SW), through Tyrrhenian and stretched by the backarc rift. Above the cross section are reported the vertical movements. From Carminati et al., 2010. From Carminati et al., movements. the cross section are reported vertical and stretched by the backarc rift. Above developed along the retrobelt of the Alpine orogen (the blue double-wedge in the center of the section). The alpine orogen was in the center of section). The alpine orogen was along the retrobelt of Alpine orogen (the blue double-wedge developed DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Throughout the Central Apennines the eastward migrating compression is coeval with extension, coupled compression is coeval migrating Apennines the eastward Throughout the Central Sea associated with extensive basin of the Tyrrhenian of rifting in the back-arc migration a clear eastward inferred from the age of different (Fig. 7 and Fig. 4) (Doglioni & Flores, 1995). This is generally volcanism Sulmona and Fucino, sedimentary basins filled by alluvial and lacustrine sediments (e.g., intra-mountain geological field trips 2016 - 8(1.2) excursion notes 15 Fig. 8 - Centroid moment tensor solutions external zone. Modified after Cinti et al., 2004. Modified after Cinti et al., external zone. available for the Central Apennine area. Note the for the Central available zone in the intra-mountain extensional earthquake confined in the and the compressional earthquake L’Aquila basins), initiated by the extensional L’Aquila tectonic activity affecting the Central Apennine area since the late Messinian and to transverse Along a transect still active. Apennine, the onset of these the Central extension-related basins becomes younger to the Adriatic going from the Tyrrhenian 1994; et al., side of the chain (Cavinato & De Celles, 1999). Cavinato basins are mainly These intra-mountain oriented and SW-dipping bordered by NW-SE normal faults (Fig. 5) cutting throughout the most of the seismicity in crust, generating Fucino 2002) (e.g., et al., region (Cavinato 1915, Mw 7.0; L’Aquila earthquake, 2009, Mw 6.3). Extensional earthquake, in the intra-mountain regime is concentrated whereas compressional regime is zone along the confined in the external zone decolléments of the buried active et al., accretionary wedge (Fig. 8) (Lavecchia 1994). etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) excursion notes 16 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. 2. The Fucino basin Tectonic setting structure within the Apennines segmented The Fucino basin is a typical intermountain normal-fault-bounded south to the Calabrian Arc and represents one of most normal fault system, which extends from Tuscany region. Major normal faults representing nearest segments of the Mediterranean provinces seismically active 2000) and fault to the NW («D» in Fig. 9; Morewood and Roberts, of this system are the M.Magnola - M.Velino fault to the SE. the Sangro Valley 2002) indicate that the Fucino structure is et al., Seismic reflection profiles (Mostardini & Merlini, 1988; Cavinato controlled by the master fault along NE border of basin (Fig. 10), i.e. San Benedetto- a half graben subsidiary faults (e.g. the Parasano-Cerchio 1939; «A» in Fig. 9) and parallel Gioia dei Marsi normal fault (Beneo, (Quaternary normal slip on pre-existing reverse fault; «B» in Fig. 9). Within this style of faulting, tectonic inversion Nijman, 1971; Massif (e.g., front of the Velino well documented, for instance along the SW range faults) is very today. been ongoing during the whole Quaternary and is still active 1979). Normal faulting appears to have Raffy, This is documented by (a) displacement and tilting of lacustrine formations slope deposit sequences, (b) by trench investigations sediments along Holocene normal fault scarps revealed offset of young progressive (January 13, 1915, M 7 Avezzano of coseismic and paleoseismic surface faulting events and (c) observation Michetti Galadini et al.,1995; et al.,1988; and related paleoseismic studies; Oddone, 1915; Serva earthquake 1997a; Galadini & Galli, 1996; Galadini et al., et al., 1). These 2012; Figs 9, 11 and Table 1999; Galli et al., Benedetto-Gioia dei Marsi and M. Magnola- data show that the two major normal fault segments (Celano-San of 0.5 to 2.0 mm/yr and total by Middle Pleistocene to present slip-rates faults) are characterized M.Velino 2005). et al., 2002; Papanikolaou et al., Quaternary offset in the order of 2000 m (Cavinato Geomorphologic setting The Fucino basin (Figs 9 and 11) is the largest tectonic of Abruzzi region. It lies in middle 2486 m a.s.l.), sometimes higher than 2000 m (Mt. Velino, Apennines surrounded by mountain ranges central carbonate shelf sediments. The closed basin is not connected which are shaped essentially from Meso-Cenozoic geological field trips 2016 - 8(1.2) excursion notes 17 San Luco dei A) E) Trasacco fault; Trasacco F) Tre Monti fault; Tre C) Magnola fault; Ovindoli–Piani di Pezza fault. Ovindoli–Piani di Pezza Cerchio-Pescina-Parasano Fig. 9 - Tectonic map showing Fig. 9 - Tectonic the system of capable normal faults in the Abruzzi Apennines. The distribution of historical seismicity since 1000 A.D. 2011) is also et al., (Rovida represented. Note the absence in the Fucino of earthquakes and area before the 1915 event compare with paleoseismic data 1. Legend: in Table Benedetto-Gioia dei Marsi fault; B) fault; D) Marsi fault; G) Numbers locate paleoseismological sites and are 1. the same of Table to important rivers. Instead, to important rivers. around it the upper courses of flow: the Salto rivers several the Liri runs to the NW, river runs south and then SW, river the Sangro runs south and then east (Fig. 9). part of the The central closed basin, a hydrologically wide roughly round-shaped plain between about 650 and 700 m high, during the Late Glacial and Holocene was etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) excursion notes 18 locate respectively the San locate respectively B) and A) etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 10 - Geologic cross section of the Fucino basin interpreted from after Cavinato et al. (2002). after Cavinato Benedetto-Gioia dei Marsi and Cerchio-Pescina-Parasano faults. Modified Benedetto-Gioia dei Marsi and Cerchio-Pescina-Parasano seismic reflection profiles. ). In the II century A.D. the emperor ). In the II century A.D. 2 DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Claudius prompted the drainage of Fucino Claudius prompted the drainage accomplished through the This was Lake. of a 6 km long tunnel mostly in excavation limestone, one of the most Mesozoic remarkable engineering projects in the of this The final drainage history. Roman performed in the second half of area was In 1875, XIX century by Alessandro Torlonia. disappeared from maps. Fucino Lake fronts bounding the Fucino The range In particular, basin are fault-controlled. the Quaternary activity of master at its NE border normal fault zone flights of lacustrine several generated these were the Quaternary, Over terraces. uplifted, tilted and faulted progressively repeatedly terraces and younger in the down-thrown block. Therefore, tectonics has left a clear imprint on sedimentary setting. developed are grouped into three major orders, namely «upper», «intermediate» and In Fig. 11, the Quaternary terraces by prominent fault scarps. separated «lower terraces», surfaces of Late Pliocene (?) - Early Pleistocene age. The highest include two main terrace The «upper terraces», as demonstrated one culminates at 1050 m a.s.l. and represents the top of most ancient lacustrine cycle, by a depositional surface of in the bedrock. The second one is faulted and reworked terraces also by wave-cut 2003). 1995; Bosi et al., 1993; Bosi et al., the Alto di Cacchia unit, culminating at 950 m a.s.l. (Blumetti et al., fault scarps and generate and SE-NW trending normal faults border the «upper terraces» intersecting NW-SE Two 1993). 1981-1982; Blumetti et al., up to 100 meters high (Fig. 11; Raffy, occupied by the third largest lake in Italy (ca occupied by the third largest lake 150 km geological field trips 2016 - 8(1.2) excursion notes 19 2) 3) 15) 16) fluvio- V-shaped 7) alluvial fan 12) 4) 1915 coseismic fluvio-lacustrine fluvio-lacustrine fault scarp; fluvio-lacustrine Equus cf. altidens Historical lake; Historical lake; 5) 6) 17) 14) sedimentary bedrock 1) 10) trough; 9) breccias (Late Pliocene- 11) 8) Trace of cross section. Modified Trace alluvial fan; 18) 13) Fig. 11 - Geologic map of the Fucino after Michetti et al. (1996). fault scarp within the lower terraces; fault scarp within the lower terraces; Holocene normal fault; rupture; talus deposits (Late Glacial to Holocene); alluvial deposits (Holocene); deposits (Late Glacial); valley; deposits (Late Glacial); deposits (Middle Pleistocene); Middle Pleistocene); (Meso-Cenozoic); basin, displaying the surface faulting basin, displaying Site is associated with the 1915 earthquake. where remains of marked were found. Legend: lacustrine deposits (Late Pliocene?-Lower Pleistocene); edge; terrace etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. The «intermediate terraces» include two main Middle Pleistocene terrace surfaces. According to Bosi et al. include two main Middle Pleistocene terrace The «intermediate terraces» not very at base levels (1995) and Messina (1996), the higher one can be divided in three orders «developed culminating at 850-870 m a.s.l. (Fig. 11). will consider them as a single terrace different from each other». We and in the valley River there is a second surface that, in the Giovenco Slightly entrenched in this terrace, are limited to the SW by a major fault is about 800-830 m a.s.l. Both these terraces surroundings of Cerchio, from 660 ranging constitute the part of basin at elevations scarp up to 100 m high.The «lower terraces» where Upper Pleistocene to Holocene lacustrine and fluvio-glacial deposits crop out. m to ca. 720 a.s.l., 1993). 1988; Blumetti et al., 1981-1982; Giraudi, These are both depositional and erosional surfaces (Raffy, part of the basin between 649 and 660 m a.s.l. is bottom historic lake. The central geological field trips 2016 - 8(1.2) excursion notes 20 Ar 40 Ar/ 39 ) at the Ponte della Mandra site (830 della Mandra ) at the Ponte etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Equus cf. altidens Quaternary geology and paleoseismology in the Fucino L’Aquila basins DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. The following chronological constraints allow estimating the age of the above mentioned lacustrine terrace: allow estimating the age of above The following chronological constraints and well defined by a wealth of archaeological, radiocarbon is very the latest Pleistocene to Holocene evolution & Giraudi (1988) and Frezzotti 1981; Narcisi, 1993). The works by Giraudi data (Radmilli, tephrachronological review of these data, building up a detailed paleoenvironmental an extensive (1992; 1995) provide is dated ca. 20 During this period, the maximum high-stand of lake reconstruction for this time interval. sites along the basin margins at several well preserved terrace, to 18 ka BP It produced a prominent wave-cut of cross section in Fig. 11). Fig. 40, and description in Stop 1.5; trace 1970; see cross section B-B, (Raffy, dating of the Majelama fan mostly comes from radiocarbon Information on the 20 to 40 ka BP time interval (2) the formation of since ca. 30 ka BP, units. This shows (1) a fluvial sedimentary environment stratigraphic In the center of basin, parent materials at 33 to 31 ka BP. from volcanic a thick paleosoil developed originating from the Alban Hills district, ca. 40 to 50 ka old, are found 10 15 m below horizons volcanic sediments deposited during data show that in the same area lake ground surface (Narcisi, 1994). Pollen 1989). the Eemian period are ca. 60 to 65 m deep (Magri & Follieri, age is ca. 540 ka ( The only available poor. Chronological data before the Late Pleistocene are very dating) of for a tephra found 100 m deep in the center of the basin (Fig. 29; Follieri et al., 1991). et al., found 100 m deep in the center of basin (Fig. 29; Follieri dating) of for a tephra the first Middle Pleistocene mammal remains of Fucino basin: provided have The «intermediate terraces» maxillary bone with teeth of an equid ( a fragmentary m a.s.l.; Fig. 29), in a complex alluvial sequence of the Giovenco valley. This species characterizes the Italian This species characterizes valley. m a.s.l.; Fig. 29), in a complex alluvial sequence of the Giovenco fauna from the end of Early Pleistocene and is no longer documented during Late-Middle Pleistocene. to the biochronological distribution of this equid spans c.a. 1 to 0.45 Ma (latest Villafranchian In particular, latest Galerian, in terms of Mammal Age). This finding definitely confirms the Middle Pleistocene age in Fig. 11). sequence («intermediate terraces» Cerchio-Collarmele-Pescina Bosi two different interpretations are found in the literature. the chronology of «upper terraces», Regarding correlations. et al. (1995; 2003) attribute the Aielli formation to Pliocene, based on regional stratigraphic (1979), the Aielli formation is late Early Pleistocene in age, based on amount of volcanic According to Raffy deposits and regional geomorphology. in the Aielli lake minerals geological field trips 2016 - 8(1.2) excursion notes 21 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Paleoseismic data paleoseismic analyses carried out in and around the data coming from many In this section, we summarize on the growth of Fucino tectonic structure by the Fucino basin. This will lead to some considerations repeated strong earthquakes. area Along the eastern border of Fucino basin and its NW extension in Ovindoli Piano di Pezza been have 1996), the Holocene paleoseismology and deformation rates et al., (Salvi & Nardi, 1995; Pantosti of the San Benedetto sites along the traces at several investigated - Gioia dei Marsi (sites 2, 3, 4, 5, 12 and 2008), Cerchio- 1997b; Saroli et al., 1995; Galadini et al., 1996; Galadini et al., 17 in Fig. 9; Michetti et al., (sites 13, 1997b) and Ovindoli-Pezza 1995; Galadini et al., (site 1 in Fig. 9; Galadini et al., Pescina-Parasano paleoseismological 1. Recently, 1996) faults, as described in Table et al., 14 and 15 in Fig. 9; Pantosti of this fault testified the reactivation 1) have on the Magnola fault (site 16 in Fig. 9 and Table investigations during the 1915 event. and earthquake in deformation rates It is possible to view these paleoseismological results in terms of variation with distance from the vary instance, the extension rates recurrence along a single tectonic structure. For center of the Fucino basin. In fact, as already pointed out, most eastern part basin is bounded 1997b) and - Cerchio fault (or Marsicana of Galadini et al., normal faults, the Parasano by two parallel the San Benedetto-Gioia dei Marsi (Oddone, 1915; Serva during the 1915 earthquake fault, both reactivated 1995) and carrying evidence of Holocene displacement. If the extension rates 1988; Galadini et al., et al., using the San Benedetto trenches (1.0 to 1.6 mm/yr; site 12 in Fig. 9; along these two traces observed 1997b) 1996) and the Marsicana trenches (0.4 to 0.5 mm/yr; site 1 in Fig. 9; Galadini et al., Michetti et al., near the center of segment is 1.4 to 2.1 mm/yr for a 45° dipping value the cumulative are summed up, at the NW termination of Fucino structure, i.e along fault. This is significantly higher than the value area, and in the Ovindoli - Piano di Pezza of about 0.9 mm/yr, a Holocene slip rate Magnola fault, that have for a 45° dipping fault plane, interpreted of 1.0 to 1.2 mm/yr can be derived where a maximum extension rate of the master fault (Nijman, 1971). as a secondary listric splay geological field trips 2016 - 8(1.2) excursion notes 22 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Data in Table 1 also indicate that the variation in extension rates is probably due to a higher frequency of in extension rates 1 also indicate that the variation Data in Table per unit time at the center of fault system compared to its NW termination. Other capable earthquakes in the Fucino basin. Galadini et al. (1997b) have also been ruptured by Holocene earthquakes faults have trenched 2 other faults in addition to the San Benedetto-Gioia dei Marsi faults and Cerchio-Pescina-Parasano extension of horizontal and, assuming that the faults dip at 45°, implied rates in extension rate and Luco dei Marsi faults. Therefore, the overall are ca. 0.4 - 0.5 mm/yr across the Trasacco the Fucino tectonic structure during Holocene might be in order of 3 to 3.5 mm/yr. Evolutionary model of the Fucino basin Benedetto-Gioia dei with the master fault represented by Celano-San The Fucino basin is a half graben, up to 1050 of this normal fault at elevations in the footwall are stranded Marsi fault. High continental terraces lacustrine sediments of the same age are buried below modern deposits in m a.s.l.. Most likely, et al. (2002) clearly show that continental of this fault. Seismic reflection data from Cavinato hanging-wall the master fault. On southern and western borders hundreds of meters thick toward deposits are several (at ca. 720 m a.s.l.), which forms a narrow terrace only the main younger of Fucino basin we observe before the Last banquette at the foot of mountain slopes; instead, edges ancient Fucino Lake Glacial Maximum (LGM) an data indicate that the Fucino basin was are not well defined. Since all the available obliterated hardly erosional processes could have very the whole Quaternary, endoreic, closed depression over to the west can conclude that the Fucino basin extended progressively We of the previous terraces. trace any Benedetto- subsidence of the Celano-San and to the south following continuing Quaternary hanging-wall Gioia dei Marsi are during the January 13, 1915, earthquake normal fault. The geomorphic changes observed the last and most spectacular evidence of this long-lasting process. geological field trips 2016 - 8(1.2) excursion notes 23 >1 2.0 0.1; 0.1; 0.1; 0.1; 0.15 0.15 2-3.4; 2-3.4; 1.2-2.5 Event 4: 2 5,6,7: 0.15; 5,6,7: Event 1: 0.8 Event 1: 0.7 Event 1: 0.5 Event 1: 0.1 0.55; Events Vertical Slip ca.0.5; ca.0.5; 2-3.4; 1.2-2.5; 1.2-2.5; 2-3.4; Events 1,2,3,4: per Event (m) 10400-7120 BP 10400-7120 AD; 1900 BC; 3300-5000 BC AD; events); >12000 BP events); >10790 BP Paleoearthquake Ages 14000-15000 BP (2 14000-15000 events) 7120-5000 BP;10790-7120 BP 7000-5000 BP;10790-7120 BP (3 7120-5000 BP; 10790-7120 BP (2 1915 AD? or 1500-1300 BC?; after 1915 AD? 13600-12300 BP; 13600-12300 19100-18500 BP 20000-10000 BP; 32520-20000 BP AD; 4700-2800 BP; 10400-7120 AD; 1915 AD; 1200-1400 AD; 2783 BP-1300 AD; 1200-1400 1915 AD; 1915 AD; 1300-1500 AD; 7120-5340 BP; AD; 1300-1500 1915 AD; 1915 AD; 1000-1349 AD; 3700-3500 BP; 1000-1349 AD; 1915 AD; 3700-3500 BP; 1000-1349 AD; 1915 AD; 1915 AD; 1000-1349 AD; 3700-3500 BP; AD; 1000-1349 1915 AD; 1915 AD; 6500-3700 BP; 7300-6100 6500-3700 1915 AD; 5 7 8 7 Total Events (s.a.a.) 3 (20000) (20000) (33000) (33000) (12000) (12000) (10800) (10800) 500-800 500-800 3 AD 550-885 AD; 885-1349 1915 AD; Recurrence 1000-1800 3 7200-6540 BP 1100-1500 AD; 1915 AD; Event 1: 0.7 1400-2100 1400-2100 3 AD BP-150 3760 AD; 150-1349 1915 AD; 0.7 1: Event 4500-5000 4500-5000 3300-5500 3300-5500 1800-2000 1800-2000 1600-1800 1600-1800 window (yr) etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Time and Time 800-1000 (3000); (3000); 800-1000 1200-1500 (2000)1200-1500 4 1500-5000 (5500)1500-5000 3 45000 BP AD -508 AD; 508 1915 AD; 1500-1800 (2000)1500-1800 2 AD 1000-1349 1915 AD; 0.6 0.5; 1800 -2000 (7000)1800 -2000 5 Quaternary geology and paleoseismology in the Fucino L’Aquila basins .a.) (s.a.a.) 3 860-1300 3 .a.) (s.a.a.) 0.9 window( yr) window( (s.a.a.) (s.a.a.) 2 1900 BC 860-1300 AD; 0.4-0.5 0.4-0.5 0.3-0.4 0.3-0.4 0.3-0.4 0.3-0.4 0.3-0.4 0.3-0.4 1.0-1.6 0.35-0.40 0.35-0.40 0.35-0.40 0.35-0.40 0.35-0.40 0.35-0.40 0.35-0.40 0.14-0.35 0.14-0.35 (last 4200) (last (last 8000) (last (last 7000) (last 7000) (last (last 7000) (last 7000) (last Vertical Slip-Rate Slip-Rate Vertical (last 7000) (last (last 2000) (last (last 20000) 20000) (last (last 10000) 10000) (last (last 20000) 20000) (last (mm/yr) and time- (last 14000-15000) 14000-15000) (last 8.5 5.5- Holocene Horizontal Offset (m) Vertical Holocene Offset (m) SW >3 none SW >3 ESE N22W WSW >3 none N60W SW >3 none WNW- N120E N120E SW N135E SW 12-16 3.5 none none (s.a (Holocene) 0.7-1.2 (5000) 800-3300 2 1900 BC AD; 860-1300 1.2-2.5 2-3.4; NW-SE SW NW-SE 10-15 NW-SE SW none >3 none NW-SE SW 5 > none NW-SE NW-SE NE >3 none 1500) 0.8 (last (1500) 1000-1800 2 AD 500-1500 1915 AD; NW-SE NW-SE NE >3 none 1500) 0.8 (last (s.a.a.) 2 AD 500-1500 1915 AD; NW-SE SW >3 none NW-SE SW >3 none NW-SE SW 5 none NW-SE SW >3 none Marsi (Cave) Locality Strike Dip Locality Strike Trasacco Trasacco Trasacco Trasacco Marsicana (Fosso 41) (Strada 42) (Strada 45) (Strada 10) (Strada 37) (Strada 38) Vado di Pezza Casali D’Aschi D’Aschi Casali Luco dei Marsi Luco dei Marsi Piano di Pezza Strada Statale Molini di Venere Colle delle Cerese San Benedetto dei 4 1 3 2 Colle delle Cerese N50W SW >3 none 5 6 8 9 7 Table 1 – Synopsis of paleoseismological analyses in the Fucino basin and nearby areas (site numbers as Fig. 9); data 1 – Synopsis Table 16 Magnola fault N115E SW >7 none N115E fault Santilli 16 Magnola 17 Cave 15 Campo Porcaro N165E W 6.5-11 N165E Porcaro 15 Campo 14 11 12 13 10 Site Galli et al., 2012. Galli et al., Trench from the ITHACA - Italy Hazards from Capable Faults, available at the webpage http://sgi.isprambiente.it. Data sources are at the webpage http://sgi.isprambiente.it. available from the ITHACA - Italy Hazards Capable Faults, 2008; 1995; 1997a; 1997b; Galadini & Galli, 1999; Saroli et al., 1996; Galadini et al., et al., 1996; Pantosti Michetti et al., DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) excursion notes 24 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 12 - Modified after Civico et al., 2015. Fig. 12 - Modified after Civico et al., (colored area). Coseismic seismological and geodetic data in modelling the seismic source as a NW- converge 12 to 19 km-long normal fault striking, SW-dipping, 2012; Vannoli - for details: Chiaraluce, box (yellow 2012). The inset shows the direction of et al., Apennines (black extension across the central arrows) and the felt area for 6 April mainshock DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. 3. The middle Aterno Valley and L’Aquila city The 2009 earthquake On April 6, 2009, a Mw 6.1 earthquake 2011) struck a densely (Herrmann et al., populated region in the Abruzzi Apennines, felt in a caused ca. 300 fatalities and was Italy (Fig. 12). Due to wide area of central shallow its location and relatively depth (~10 km), the hypocentral damage in the caused heavy earthquake and surrounding villages. town of L’Aquila - the Paganica Soon after the earthquake, (PSDFS), System San Demetrio Fault bounding to the east middle Aterno interpreted as the surface was Valley, expression of the 6 April 2009 earthquake geological field trips 2016 - 8(1.2) excursion notes 25 sector ~3-13 km of primary coseismic ruptures were observed (Fig. 13; ruptures were observed causative fault, and along its NW causative Falcucci et al., 2009; Boncio et al., et al., Falcucci 2010; EMERGEO Working Group, 2010; Group, 2010; EMERGEO Working Galli et al., 2010; Lavecchia et al., 2010; et al., 2010; Lavecchia Galli et al., Vittori et al., 2011). Vittori et al., Geological setting – middle Aterno Valley The middle Aterno Valley is a ca. 18 km-long, 3 to 6 Valley The middle Aterno etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. km-wide Quaternary intramontane basin located Quaternary intramontane km-wide south-east of the town of L’Aquila. The basin is south-east of the town L’Aquila. characterized by the presence of an extensive cover of cover by the presence of an extensive characterized lacustrine and fluvial/alluvial Quaternary deposits accumulated upon a Meso-Cenozoic mainly carbonatic accumulated upon a Meso-Cenozoic Quaternary geology and paleoseismology in the Fucino L’Aquila basins bedrock and generally separated by unconformities and/or separated bedrock and generally juxtaposed by the several fault splays detectable in the area fault splays juxtaposed by the several (Figs 14 and 15). Continental deposits overlying the bedrock sequence have Continental deposits overlying been investigated by several authors (Bertini & Bosi, 1993; by several been investigated Giaccio et al., 2012; Pucci et al., 2015) and can be referred to six 2012; Pucci et al., Giaccio et al., main depositional cycles: (1) Early Pleistocene slope-derived carbonatic (1) Early Pleistocene slope-derived main depositional cycles: DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Fig. 13 - Surface rupture along the Paganica fault. The breaks consist of open cracks (av. 10 cm) with vertical dislocations (max 15 cm), SW-side down. The ruptures occurred with a persistent orientation of N130°–140°, regardless of slope angle, type deposits crossed and the presence of man-made features (EMERGEO W.G., 2010). breccias (L’Aquila megabreccias and Valle Valiano fms. – MBR, VVB, VVC); (2) Early Pleistocene lacustrine and fms. – MBR, VVB, Valiano megabreccias and Valle breccias (L’Aquila silts with fluvio-lacustrine sequence (Limi di San Nicandro fm. - SNL), composed of whitish silts and clayey fm. - VOC), partially lenses, up to 100 m thick; (3) Early Pleistocene alluvial sequence (Vall’Orsa gravel heteropic with the Limi di San Nicandro showing foreset and consisting of deltaic carbonatic conglomerates fm., Inferno fm. - VIC), Pleistocene alluvial fan sequence (Valle and bottomset beds (100 m thick); (4) Early-Middle and showing topset beds, with sparse silty layers consisting of well-bedded carbonatic conglomerates palaeosoils and (5) Middle-Late Pleistocene fluvial alluvial sequence, made of silts, sands gravels, geological field trips 2016 - 8(1.2) excursion notes 26 aimed at defining the subsurface geometry of the middle Aterno basin (among the others: MS-AQ Working Group, 2010; Balasco et Group, Working al., 2011; Improta et al., 2012; 2011; Improta et al., al., Santo et al., 2013). Santo et al., Balasco et al., (2011) investigated Balasco et al., the large-scale structure of northeast part of the basin by means of a ~8 km-long ERT and a means of a ~8 km-long ERT magnetotelluric profile. They suggested the existence of complex lateral and vertical complex lateral resistivity changes in the NE sector (between Mt. Bazzano and Paganica), that can be related to Paganica), the presence of a shallow conductive alluvial filling (~200 m- conductive thick) above a rugged carbonate thick) above substratum. In the same area, substratum. Improta et al., (2012) performed a Improta et al., high-resolution seismic survey over an 8 km long section. Their over tomographic images highlighted tomographic the presence of a complex etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. SMF, SMA). All these deposits are covered by (6) Late SMA). All these deposits are covered SMF, – The 2009 L’Aquila earthquake triggered several studies triggered several earthquake The 2009 L’Aquila Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 14 – Scheme of the stratigraphic relationship of the Fig. 14 – Scheme of the stratigraphic the identified unconformities (red arrow). Quaternary deposits (modified after Pucci et al., 2015). Quaternary deposits (modified after Pucci et al., units and one of Pictures show a selection of the stratigraphic DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. interbedded with volcanoclastic layers (San Mauro fm. layers interbedded with volcanoclastic Pleistocene-Holocene fluvial/alluvial sediments, mainly related to the Aterno River, and by slope debris River, Pleistocene-Holocene fluvial/alluvial sediments, mainly related to the Aterno colluvial deposits. geological field trips 2016 - 8(1.2) excursion notes 27 Fig. 15 - Quaternary geology of the C-C’ is shown in Fig. 61. C-C’ middle Aterno Valley (modified after Valley middle Aterno 2015). Geological section Pucci et al., topography of the pre-Quaternary topography with a ~350 m deep substratum, depocenter in the Bazzano sub- they evidenced basin. Moreover, heterogeneities and strong lateral (NE of Mt. steps in the substratum Bazzano), suggesting the presence of buried synthetic and antithetic bedrock and involving fault splays basin infill deposits within the sub-basin. Paganica etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) excursion notes 28 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Structural setting - middle Aterno Valley 2013) highlighted 2012; Blumetti et al., 2011; Giaccio et al., 2010; Cinti et al., studies (Galli et al., Several which extends well is only a small segment of the PSDFS, that the fault responsible for 2009 earthquake between 12 and 30 km. sector and shows different potential rupture length, ranging the Paganica beyond been built up by surface rupturing scarps have they pointed out that the PSDFS cumulative Moreover, Such outcome indicates a affecting either its whole length or smaller sections (2009-like). earthquakes & model (Schwartz be better described by a variable-slip of the seismic source which may complex behaviour 2015) highlighted the existence of a 2015; Civico et al., Coppersmith, 1984). More recent works (Pucci et al., 1-5 km fault splays, parallel by several setting of the PSDFS at surface, characterized complex structural where the net extension is mostly size, in synthetic and antithetic pairs of variable long, frequently arranged structures. This style is found from the outcrop scale (a few meters) up to accommodated by SW-dipping (2015). The PSDFS by Civico et al., entire basin scale (some km-scale) and it is therefore said “quasi-fractal” and a small by a narrow deformation zone characterized sector to the NW, comprises: (1) the Paganica splays Quaternary basin; (2) the San Demetrio sector to SE, with a set of kilometer-spaced hangingwall that exhume and dissect a wider Quaternary basin (Fig 16). The longest fault segments are NW-trending, whereas some minor E- and N-trending faults are present. These latter partly belong to an older system faults mostly activated during Early Pleistocene with complex kinematics, whereas the NW-trending active Civico et under the NE-extensional regime still affecting chain. Notwithstanding this internal complexity, (2015) on the basis of morphological throw distribution, defined PSDFS asal., a ~19 km-long structure in the long-term as a single individual normal fault. which behaves geological field trips 2016 - 8(1.2) excursion notes 29 nt . etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 16 – Map of the Paganica-San Demetrio Fault System (PSDFS) showing its geometrical arrangement at the surface and exte (PSDFS) showing its geometrical arrangement System Demetrio Fault Fig. 16 – Map of the Paganica-San and age of outcropping pre-Quaternary basement, and Plio-Pleistocene and Holocene deposits (modified after Civico et al., 2015) and age of outcropping pre-Quaternary basement, Plio-Pleistocene Holocene deposits (modified after Civico et al., DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Geological setting – L’Aquila city city (about 70,000 inhabitants), settled in a tectonic basin delimited by prominent is a moderate-sized L’Aquila becoming soon the most important centre of founded at the half of XIII century, It was mountain ranges. historic heritage. by a large and valuable the area characterized geological field trips 2016 - 8(1.2) excursion notes 30 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 17 - Geological map of L’Aquila city centre Fig. 17 - Geological map of L’Aquila (MS–AQ WORKING GROUP, 2010). WORKING GROUP, (MS–AQ DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. The city centre is placed on a flat terraced hill The city centre is placed on a flat terraced whose schematic geological setting consists, from the top to bottom, of Middle Pleistocene 80- 100 m-thick calcareous breccias, (“brecce onto a 250-270 m- - MBR), which lay dell’Aquila” thick homogeneous Early Pleistocene fluvial- lacustrine pelites and sands, as shown in Figs 17 are the “brecce dell’Aquila” and 18. In particular, composed of fine to coarse calcareous fragments (mostly of some cm) embedded in size of variable by highly sandy or silty matrix, characterized cementation degree and mechanical variable 2013), while the fluvial- properties (Monaco et al., lacustrine deposits consist of fine- to medium- silts. The latter ones are placed onto the grained carbonate bedrock, whose depth Meso-Cenozoic the NE, as testified by deep decreases toward boreholes, and seismic reflection gravimetric 2010; Del Monaco (Amoroso et al., investigations 2010; Tallini Group, Working 2013; MS–AQ et al., thickness 2011). The “brecce dell’Aquila” et al., sector decreases from about 100 m in the central of the historical centre (i.e. Piazza Duomo) to 0- hill, where 10 m in the southern slope of L’Aquila replaced by sands, pelites and they are laterally geological field trips 2016 - 8(1.2) excursion notes 31 calcareous gravels and breccia calcareous gravels (Del Monaco et al., layers at places, some 2013). Further, (empty or underground caves filled with 1-10 m thick residual epikarst fine-grained soils named “terre rosse”) are present in the “brecce (Del Monaco et al., dell’Aquila” 2013). the city is Unfortunately, located within a highly seismic region (Fig. 19), whose activity is well documented by old historical sources since the etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 18 - Schematic geological section across L'Aquila city centre (Monaco et al., 2013 - modified city centre (Monaco et al., Fig. 18 - Schematic geological section across L'Aquila after MS–AQ WORKING GROUP, 2010), also showing the position of deep investigations. WORKING GROUP, after MS–AQ L’Aquila, before 2009. L’Aquila, Fig. 19 - Seismic history of L’Aquila, produced the most severe damage in produced the most severe In table the list of the earthquakes that In table the list of earthquakes before 2009. (DBMI - Locati et al., 2011). before 2009. (DBMI - Locati et al., DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) excursion notes 32 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. (modified after Fig. 20 - Map of 1703 earthquake Colapietra, 1978). Colapietra, damage due to the the distribution of Quaternary geology and paleoseismology in the Fucino L’Aquila basins DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. early XIV century. The first event that was reported that was The first event early XIV century. occurred on 1315. Since to cause damage in L’Aquila strong has experienced several then, L’Aquila destroyed heavily which was The city, earthquakes. has been restored each time. after all these events, is considered, by the 1461 event In particular, historians and city planners, responsible of the housing in L’Aquila disappearing of the medieval (Clementi and Piroddi, 1986), while the 1703 the birth of present urban marked earthquake a major disaster in the was plan (Fig. 20). This event and occurred during a long period history of L’Aquila of political and economic decline, in which further (occurred in 1639, 1646, and minor earthquakes After the 1703 earthquake 1672) damaged the city. established, in search of “antiseismic” techniques such as wooden beams to improve a new building planning was buttresses and reduction of floor height. and connections between roofs walls, the connection of walls after the almost ten years years: difficult and took many very the reconstruction of city was However, less than 15% of buildings had been rebuilt (De Matteis, 1973). earthquake, the area inside ancient Wars, and in the period between two World earthquake After the 1915 Avezzano for expanding into the open spaces that during ancient times had been reserved further urbanized, was walls gardens, pastures and cattle fairs. vegetable buildings located downtown are mainly two to four storeys, built variable: The present building stock is very in simple stone masonry, to corresponding respectively often with tie-rod connections among walls, according to EMS98 (Grunthal, 1998). class A and B, vulnerability stones or bricks were used only for Massive and important edifices: among them there are more recent buildings, built during the last some strategic class C). In the suburban area, recently in brick masonry and reinforced concrete (RC) (vulnerability century, structures with masonry infill modern reinforced concrete frame most buildings are relatively developed, 2011; 2012). et al., class C and D) (see for details: Tertulliani (vulnerability geological field trips 2016 - 8(1.2) excursion notes 33 (Tertulliani et al., 2011). et al., (Tertulliani earthquake April 2009 after the 6 downtown, L’Aquila grades in grades the damage Distribution of Fig. 21 - etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. The 2009 earthquake in L’Aquila city hit a Mw=6.1 earthquake On 6 April 2009, at 01:32 GMT, severe effects and causing very with devastating L’Aquila social damage also in tens of villages nearby with a grievous city), 47% of impact: 309 casualties (2/3 of them in L’Aquila the housing partially damaged, 20% of heavily damaged and more than 40,000 people left homeless. The disastrous. impact on religious and monumental heritage was 8-9 was The assessed macroseismic intensity for L’Aquila downtown has been subject EMS98. The damage in L’Aquila the first because it was studies after the earthquake, of many Calabria time in Italy that, after the 1908 Messina-Reggio The struck by a seismic event. severely a city was earthquake, performed soon after the earthquake macroseismic survey (Fig. 21) highlighted that about 70% of the buildings, mainly represented in classes B and C, suffered substantial to very damage. In particular: heavy buildings (class A) were all damaged; · the most vulnerable destruction; heavy about 50% of them suffered very damage, of severe · classes B and C suffered a high rate to partial structure failure cracks from large and extensive elements in in masonry buildings and damage to structural RC buildings; · more than 90% of the monumental buildings suffered to total collapse; damage from severe quite distinct within the city: The spatial distribution of the damage was in the western sector of city (red circle Fig. 21), mainly concentrated damage was · the heaviest in San Pietro a Coppito quarter; particular the 39% of total collapses were observed border of the historical centre. · about 80% of collapses in RC buildings occurred along the south-western geological field trips 2016 - 8(1.2) excursion notes 34 of the XIX century (Stokel, 1981; Centofanti, areas until the end 1984; Piroddi et al., 1984; Figs 22a and gardens and green 22b), except few 22b), except buildings detected in Via Campo di Fossa since 1753 Campo di Fossa dedicated to vegetable (Fig. 22a). At the end of 1800s, this part At the city acquired building interests (Fig. 22c) due to the construction of Via XX Settembre to connect the city to railway station, and because of the 1915 Avezzano earthquake, after which a earthquake, Avezzano parcelling plan was introduced (and parcelling plan was never realized) that caused a chaotic realized) never construction (Stokel, 1981). During the construction (Stokel, years the urban expansion continued until years saturation was reached (Figs 22d and 22e). was saturation etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins 1958; 1858; (d) (a) (b) 1983. The red 1931; DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Fig. 22 - Historical urban maps of L’Aquila city centre (Centofanti, 1984): 1753; (c) (e) line delineates the southern part of the city within the anciet walls. South L’Aquila damage RC buildings collapsed or suffered severe several in South L’Aquila As introduced in the previous paragraph, due to the main shock causing 135 victims. centre (including most of Differently from the ancient part of L’Aquila with red line in Fig. 22) old masonry buildings), the southern part (marked the historical heritage and several buildings, mostly 5-7 storey high, built between 1950 and 1965. Itfeatures reinforced concrete frame mainly was geological field trips 2016 - 8(1.2) itinerary 35 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins DAY 1 Fucino basin Quaternary geology and palaeosismology in the DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) itinerary 36 ste etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Wallace, 1978) that divides Mt. Magnola from Mt. Velino, the Late-Glacial 1978) that divides Mt. Magnola from Velino, Wallace, sensu Fig. 23 - In the background the panoramic view of Mt Magnola, Tre Monti and Serra di Celano fault escarpments. The Monti and Serra view of Mt Magnola, Tre Fig. 23 - In the background panoramic deposits, at the base of the Tre Monti fault escarpment. In the foreground city of Avezzano. deposits, at the base of Tre Majelama “wine glass valley” is also indicated. The inset drawing locates the “scarplet” (fault scarp) in Late Glacial slope-wa is also indicated. The inset drawing Majelama “wine glass valley” DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. STOP 1.1 – Landscape view of the Fucino basin from Mt. Salviano and general introduction view on the fault escarpment of Velino a panoramic looking north, it is possible to have From Mt. Salviano, a with a spectacular Holocene normal fault scarp at its base. From the Majelama Valley, - Magnola Massif, ( typical “wine glass valley” geological field trips 2016 - 8(1.2) itinerary 37 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Majelama alluvial fan gently slopes toward the Fucino basin. The city of Avezzano, partly built on the edge of the Fucino basin. The city of Avezzano, Majelama alluvial fan gently slopes toward seen standing after the main on January 13, 1915. Only one building was totally destroyed the alluvial fan, was occurred in this town (94,9 % of the population). shock; most of the 30,000 casualties due to earthquake Monti fault escarpment also shows a prominent bedrock scarp (“nastrino” or Looking NE, the Tre slope Monti fault cuts the Late Glacial stratified ribbon); it is to notice that the SW termination of Tre deposits, where it shows an about 2 m high fault scarp. uplifted along the Cerchio-Pescina the east, in background, are Quaternary continental terraces To surfaces of Late Pliocene (?) - Early Pleistocene age. The include two main terrace fault. The «upper terraces» as highest one culminates at 1050 m a.s.l. and represents the top of most ancient lacustrine cycle, by a in the bedrock. The second one is faulted and reworked terraces also by wave-cut demonstrated intersecting NW-SE depositional surface of the Alto di Cacchia unit culminating at 950 m a.s.l. (Fig. 11). Two fault scarps up to 100 m high. and generate and SE-NW trending normal faults border the «upper terraces» for the artificial drainage 1870. Except filling the wide basin until year was In the middle, Fucino Lake hydrologically the Fucino basin was by Alessandro Torlonia, times first and eventually in Roman of the lake closed (endorheic) throughout the whole Quaternary. STOP 1.2 – Paleoseismology and long-term activity along the Magnola fault (Fonte Capo La Maina, Forme) Figs 24-26), a prominent westnorthwest- view of the Magnola fault (MF, The Stop allows a panorama front. The fault mountain range eastsoutheast normal fault on the southern slopes of Magnola-Velino of Late Miocene age, possibly sense of slip a thrust ramp with reversed appears to represent the reactivation dip angle (30-50°). The MF length is estimated by Galli et al. (2012) in moderate reflected in the relatively fault, while to the east, trending Velino of 13 km, bounded to the west by northwest-southeast excess continuation in the Fucino fault system (the it has a natural abruptly, disappears rather despite its trace 2012). fault of Galli et al., Marsicana Highway 2012). (Galli et al., confirmed this fault is capable of major earthquakes studies have Recent studies documenting the recent activity of MF are those Piccardi et al. key In addition to the latter, et al. (2004), Gori (2007), Schlagenhauf (2010, 2011). The works of Piccardi (1999), Palumbo features of the fault zone (1999) and Gori et al. (2007) focus on the major geomorphological stratigraphic and 0.54- of 0.7 mm/a after the Last Glacial Maximum (LGM) respectively front, assessing slip rates and range geological field trips 2016 - 8(1.2) itinerary 38 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 24 - Panorama of the Magnola range with some key elements indicated. BB - Bisegna breccias. DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) itinerary 39 : view from Stop 1.2. The Bisegna below : view from west (Stop 1.2 is at the far right edge etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Above . Galli et al. (2012) have recalculated the Holocene . Galli et al. (2012) have Quaternary geology and paleoseismology in the Fucino L’Aquila basins Cl) dating of the exposed limestone fault slickenside has Cl) dating of the exposed limestone fault slickenside 36 earthquake supercycles period (started ca. 4.5 ka ago) before the Roman period, followed by two historical earthquakes, period (started ca. 4.5 ka ago) before the Roman Fig. 25 - Panorama of the Magnola range-front fault escarpment. of the Magnola range-front Fig. 25 - Panorama breccias crop out on the right side of photograph. of the photograph). The Bisegna breccias crop out to the left of Valle Majelama; The Bisegna breccias crop out to the left of Valle of the photograph). DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. evidenced a number of rejuvenation events after the LGM (5 according to Palumbo et al., 2007, and 9 et al., (5 according to Palumbo after the LGM events evidenced a number of rejuvenation in the latter paper were all to be events 2010, 2011). If the rejuvenation according to Schlagenhauf et al., between would be 1.5 ka, but largely uneven recurrence interval then the average attributed to coseismic slip, possibly representing events, occurred during the so-called inferred an event obtaining 0.9 ± 0.1 mm/a. They have slip-rate, vertical Neoglacial documented in most of their trenches the Fucino basin, which they interpret as an early Middle Age event (see discussion in Stop 1.6), and the 1915 event. the 508 CE earthquake 0.81 mm/a for the last million years. Cosmogenic ( 0.81 mm/a for the last million years. geological field trips 2016 - 8(1.2) itinerary 40 : detail of the Right etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins : general aspect of the fault scarp around location studies cited in text. : general Left Fig. 26 - fault slickenside (looking east from near the trench site). fault slickenside DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. The fault slickenside can be approached with a hike of at least 30 minutes. Standing near the fountain on can be approached with a hike The fault slickenside shelf in Mesozoic the denudated slope carved by a line separating is seen marked pass, the fault trace limestone from late Quaternary scree deposits and Early Pleistocene cemented breccias (Bisegna fm.). The that often marks the on these sediments allows the growth of vegetation presence of Holocene soil developed meters high (vertical here several details of the fault scarp, fault contact (Fig. 25). Figures 26 and 27 provide ca. 7 m). separation the Bisegna breccias (after Bosi & Messina, 1991; named brecce Mortadella in Demangeot, 1965) the Stop, At they are a rather can be seen on the right side of slope (Fig. 25, below). With a typical light reddish color, (early Pleistocene). Cropping out both on the well cemented alluvial fan deposit dated at around 1 million year in the limestone bedrock at ca. 1900 m a.s.l.) and hangingwall, (on the upper flat surface carved footwall of the fault. In origin, they had to slope to estimate the long-term slip rate they represent a reference marker geological field trips 2016 - 8(1.2) itinerary 41 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 27 - Oblique view lookink east and log of the Montagnola paleoseismological trench (after Galli et al., 2012). Fig. 27 - Oblique view lookink east and log of the Montagnola paleoseismological trench (after Galli et al., DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. several degrees southward, i.e. conformably to the slope, while they are found now dip up 10° counter- degrees southward, several reflecting either the natural Their thickness is much higher in the hangingwall, slope in the hangingwall. all this into account, Galli et al. and the stronger erosion higher in slope. Taking thickening downward offset of 550 m. measured a net vertical (2012) have geological field trips 2016 - 8(1.2) itinerary 42 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Equus have been found is also shown. Fig. 28 - Oblique view of the Fucino «intermediate cf. altidens terraces». The trace of the 1915 surface faulting is indicated by the red line and across it Trench site 1 is indicated (site 1 in Fig. 9). The site where remains of DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. STOP 1.3 – Cerchio-Collarmele tectonic terraces: long-term activity along the Cerchio-Pescina fault the landscape of «intermediate terraces» viewpoint (Fig. 28) it is possible to observe From this panoramic in the top surface at about 850-870 m a.s.l.. They are mostly carved that culminate with a well preserved that used the same course belonging to a river formation (Messina, 1996), made up of fluvial gravel, Pescina This formation is about 40 meter thick. River. of the present Giovenco geological field trips 2016 - 8(1.2) itinerary 43 5) Equus cf. Late Pleistocene to 2) remains back to c.a. 1 Pliocene?- Early Pleistocene? breccias; 4) Equus cf. altidens Surface faulting occurred during the January 13, 1915 SF) etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Holocene deposits of the Fucino Lake; Holocene deposits of the Fucino Lake; 1) Quaternary geology and paleoseismology in the Fucino L’Aquila basins Dated tephra layer; layer; Dated tephra 6) Middle Pleistocene fluvial and lake deposits; Middle Pleistocene fluvial and lake 3) Ar across the section A-A’ the long term slip rate 1991) constrains et al., age; Follieri 40 Ar/ 39 . This species characterizes the Italian fauna from end of Early Pleistocene and is no longer . This species characterizes Fig. 29 - Schematic geologic profile across the Quaternary terraces at the NE border of Fucino basin (location in Fig. Fig. 29 - Schematic geologic profile across the Quaternary terraces earthquake (modified after Serva et al., 2002). et al., (modified after Serva earthquake 11). The «intermediate» and «lower terraces» deposits are shown, whereas the «upper terrace» is here represented by an deposits are shown, whereas the «upper terrace» 11). The «intermediate» and «lower terraces» of deposits. Legend: erosional surface with only a thin layer Holocene alluvial fan deposits; Meso-Cenozoic pelagic limestone sequence; Meso-Cenozoic DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. altidens are limited to the SW by a major fault documented during the Late-middle Pleistocene. Both these terraces fault (B in Fig. 9). scarp up to 100 m high (Fig. 29), related the activity of Cerchio-Pescina-Parasano dated with the The correlation of the top surface these terraces, found at a depth of 100 m in the centre basin, dated Ma to 0.45 Ma, together with the age of a tephra to ca. 540 ka BP ( Slightly entrenched in this terrace, in the Giovenco River valley and in the surrounding of villages Pescina valley River in the Giovenco Slightly entrenched in this terrace, that culminates at about 800-830 m a.s.l.. This is also made up of fluvial gravel there is a terrace and Cerchio, about at the Valley, In a reddish paleosoil outcropping inside the Giovenco river. belonging to a paleo-Giovenco maxillary found a fragmentary site, 830 m a.s.l.; Fig. 28), it was della Mandra top of this sequence (at Ponte bone with a tooth of an equid. The paleontological determination ascribes this fossil remain to of Fig. 29 to 0.3 - 0.6 mm/yr. geological field trips 2016 - 8(1.2) itinerary 44 is (b) . Small stars indicate the event Fig. 30 - Geological cross- (after Galadini & Galli, 1999). located 35 m to the west of section (a) the triangle represents horizons; dating; sampling site for radiocarbon unit 1 is a colluvium that buries an archaeological settlement close to this area, dated back to 2500 B.C. sections of the gas pipeline trench at Section site 1 (southern wall). etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. In the ‘90s, the excavation of a long gas pipeline trench that crossed the Cerchio-Pescina fault (site 1 in Fig. of a long gas pipeline trench that crossed the Cerchio-Pescina In the ‘90s, excavation 1), allowed to collect the paleoseismological data shown in Fig. 30 (Galadini & Galli, 1999). 9 and Table affecting Late Pleistocene–Holocene deposits up fault planes, at a distance of about 35 m, were observed Two of the ploughed soil (Fig. 30). to the level 1); (Table at least four displacement events revealed According to Galadini & Galli (1999), the trench stratigraphy offset of about 1 m. it had a vertical the 1915 event; most likely was the latest, occurred after 2500 B.C., geological field trips 2016 - 8(1.2) itinerary 45 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins The Filippone Hotel is located at the base of the Serrone Mt. normal fault scarp (Fig. 31). We have The Filippone Hotel is located at the base of Serrone Mt. normal fault scarp (Fig. 31). We Fig. 31 - Panoramic view of the southwestern flank Mt. serrone fault escarpment. The Holocene scarp is visible Fig. 31 - Panoramic about half-way up the slope. This scarp was likely reactivated during the 1915 earthquake. reactivated likely up the slope. This scarp was about half-way DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. STOP 1.4 – The Serrone fault escarpment Overview: the opportunity to have a close-up view of landscape feature that is nearly identical to the Magnola, Velino the opportunity to have during the previous stops. From swimming pool it is possible to see Monti fault scarps observed and Tre one of the most spectacular fault planes belonging to San Benedetto-Gioia dei Marsi fault. This bedrock according to eye-witnesses. during the 1915 earthquake, been reactivated fault mirror is thought to have of the Serrone Mt. fault scarp can be used as a model for understanding Therefore, the geomorphic characters of similar landforms throughout the Apennines, which appear to be controlled by repeated the evolution occurrence of strong recent earthquakes. The Serrone fault scarp is close to the SE tip of that controls NE border Fucino Lake along- for total throw, value basin (Fig. 32). Compared to the centre of fault we expect a relatively-low of thinning of the basin-fill sediments, a reduction relief across fault escarpment, low values strike and oblique-slip kinematics. slip per earthquake geological field trips 2016 - 8(1.2) itinerary 46 Cl 36 , so the faulting is ° The fault length is 35 km towards 222 towards The slip vector across the fault The slip vector ° Fig. 32 - Map and cross-section along Line A-B showing Fig. 32 - Map and cross-section along Line A-B Sample site is SE of Gioia dei Marsi. etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. the geometry of basin-bounding fault on NE side 2002). Slip- et al., basin (modified, from Cavinato Fucino Lake & Michetti (2004). on the fault are from Roberts vectors almost pure dip-slip with a small right-lateral component, as expected from the location near to & Michetti, 2004). the SE fault tip (Roberts sediments, dating from Pliocene and Pleistocene that the fault in a classic half-graben towards thicken from decrease in thickness along strike geometry, ~900 m where the throw is 1600 to 100-200 at 2002). et al., Gioia dei Marsi (Cavinato Expected slip per event: in length (modified from Roberts & Michetti 2004 in length (modified from Roberts 2010). Using empirical et al., Walker and Faure & Coppersmith (1994) we relationships in Wells expect ~1.5 m maximum slip at the centre of fault, but only ~0.2 m slip at the site chosen for dating because we are within a few kilometres of the SE fault tip. Kinematics: plunges at 54 Quaternary geology and paleoseismology in the Fucino L’Aquila basins The total throw across the fault is defined by geological cross-sections showing DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Total throw and basin fill: offset of the base of the Miocene strata. The total throw is 250-300m (Roberts & Michetti, 2004), compared to a The total throw is 250-300m (Roberts offset of the base Miocene strata. et al., throw of 1600 m ~3km NW San Benedetto dei Marsi near the centre fault (Fig. 32 from Cavinato Basin-filling lacustrine and alluvial along strike. the displacement gradient 2002). This difference reveals geological field trips 2016 - 8(1.2) itinerary 47 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins The fault displays the classic geomorphology of upper slope, free-face and lower slope The fault displays Fig. 33 - Hillshade of the Serrone scarp kinematic data from structural mapping. kinematic data from structural Cl dating is indicated in green. Insets show from terrestrial LiDAR data. The site chosen for 36 DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Geomorphology: revealed by LiDAR data (Figs 33 and 34). This morphology forms when a preserved last glacial maximum (LGM) by LiDAR data (Figs 33 and 34). This morphology forms when a preserved revealed faulting uplifted the normal fault. During the LGM, landscape is offset by Holocene surface slip across an active of the coldest The cold climate (-12°C mean temperature faulting events. bedrock limestone in meter-scale that outpaced scarp growth 1999) promoted free-thaw action and high erosion rates month; Allen et al., scarp could form. Sediments accumulated eroded, so no cumulative through faulting. The emerging scarp was a smoothed landscape with continuous slopes The result was as scree sheets on the down-faulted hangingwall. (0 to 4°C mean increased after the demise of LGM normal faults. When temperatures across the active scarp decreased. This allowed a cumulative 1999), erosion rates of the coldest month; Allen et al., temperature to accumulate through surface faulting. On the nearby Magnola fault, study of pitting fault surfaces and upper fault plane angles slope versus imply Holocene erosion rates perpendicular to slopes of 0.001 of erosion rates mm/yr with LGM et al., 0.2-0.4 mm/yr (Tucker 2011). The timing of the demise is 12-18 ka, defined by a the LGM most number of climate proxies, notably the change in dominance of coniferous to deciduous pollen in 1999). sediments (Allen et al., lake Thus, the change in climate for the a time marker provides faulting. The free-face formed in 12-18 kyrs. geological field trips 2016 - 8(1.2) itinerary 48 Cl 36 A tripod-based LiDAR Cl site: data set has been processed to and to produce vegetation remove a hillshade map and scarp profiles (Figs 33 and 34). The scarp profiles are used to define the throw and and define the slip after the LGM for the upper-slope, dip values and free-face. These lower-slope are needed to model the values data. emphasise that geomorphology We so of the scarp differs along strike, site selection is essential to exclude as a fault plane mass-wasting exhumation process. Along the NW portion of the Serrone scarp (Fig. 33), the lower slope has been modified by Holocene mass wasting LiDAR data set and detailed geomorphology of the chosen 36 Cl. The hangingwall cut-off must be cut-off Cl. The hangingwall 36 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Cl dating is conducted otherwise part of the exhumation will be due to 36 Fig. 34 - Scarp profile of the Serrone scarp from terrestrial LiDAR data, showing confirmed by exhumation of a trench. the classic geomorphology of upper slope, free-face and lower slope developed climate across the demise of Last from cold to warmer during the transition in the sub-surface, GPR data show the geometry of strata Glacial Maximum (LGM). DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. to produce deeply-incised debris-flow channels cut into the formerly-planar lower slope. Along the SE portion debris-flow channels cut into the formerly-planar to produce deeply-incised of the Serrone scarp (Fig. 33), lower slope is less-modified by incised debris-flow channels. In places This hanging is preserved. at the time of demise LGM cut-off hangingwall formed when cut-off wall during the demise of last glacial maximum (LGM), decreased as the climate warmed sedimentation rates and is horizontal cut-off The hangingwall surface faulting event. offset by the first post LGM and the slope was sampled for where we have continuous for tens of metres along strike preserved in this way at sites where in this way preserved mass wasting and not slip in earthquakes. mass wasting geological field trips 2016 - 8(1.2) itinerary 49 Cl. 36 Cl (Fig. 35). However, the upper Cl (Fig. 35). However, ~10 metres of the fault plane (measured in the plane of fault) been eroded by a few have decimetres to a few metres (termed free face; see Fig. 34). the degraded not sampled this for have We in millimetre-scale frictional-wear striae. The frictional wear striae plunge to the crests of corrugations parallel The free-face is defining the slip vector. almost free of erosion, with millimetres scale frictional wear striae preserved for the lowermost ~5 metres (measured in the plane of fault). sampled this fault plane for have We 36 This erosion has also removed the This erosion has also removed lowest portion of the upper slope upper slope). (termed degraded the Thus, this erosion has removed but we are able to cut-off, footwall reconstruct it by projecting the un- etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. towards the basin. The similarity in dip between these towards ° Quaternary geology and paleoseismology in the Fucino L’Aquila basins trench along the Serrone scarp showing site (b) (Fig. 34). The lower slope, formed of breccia/conglomerate colluvium derived from the upper slope colluvium derived (Fig. 34). The lower slope, formed of breccia/conglomerate ° free-face and (a) Cl. The upper slope, which is cut into bedrock limestone, is relatively smooth and planar, dipping towards the dipping towards smooth and planar, Cl. The upper slope, which is cut into bedrock limestone, relatively Cl dating. 36 36 Fig. 35 - for DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Where the fault scarp has not been modified by Holocene mass wasting (SE portion), we have chosen a site to date (SE portion), we have Where the fault scarp has not been modified by Holocene mass wasting with slopes cut on different materials suggests they were formerly the same slope in the LGM that has become offset by slopes cut on different materials suggests they were formerly the same slope in LGM carbonate fault gouge that is The free-face is a carbonate fault plane that formed in indurated surface fault slip. tens of metres, and is covered is corrugated on a decimetre scale and over 20-30 cm thick. The free-face slickenside (scree), is also very smooth and planar, dipping at 37-38 smooth and planar, (scree), is also very basin at 39-40 geological field trips 2016 - 8(1.2) itinerary 50 Cl accumulation in 36 Cl concentration (Fig. 36a), Cl concentration 36 To check that the lower slope has not To The throw measured between the footwall cut- The throw measured between the footwall etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins We have sampled the lowermost 5 m of free-face, plus 1.95 fault plane exposed have We Cl approach: DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. in the trench (all measured in the plane of the fault). We collected a continuous sample in 5 cm sections, and in the trench (all measured plane of fault). We 56 determinations of have analysed a subset of the samples collected. We have been modified by mass-wasting or formation of channels before later re-surfacing we collected a ground- been modified by mass-wasting measured in the plane of fault; Fig. 34). dataset and dug a shallow trench (1.95 m deep, radar penetrating sediment. The data reveal of at least 5 metres through the hangingwall penetration The GPR achieved we found ~10 cm of organic ground surface. In the trench excavation the present-day reflectors that parallel scree deposits that are free of organic indurated rich soil (probably Holocene) before entering light-coloured, ground surface, the present-day colluvium parallels in this LGM sediments). Layering material (probably LGM lower slope(s) had similar dips to the upper slope cut into confirming the findings from GPR, and that LGM offset by to be former ground surfaces that became progressively interpret the layers bedrock limestones. We at the top of cut-off correctly identified the hangingwall This confirms we have faulting during the LGM. or formation of channels before sediments, and that the site has not been disturbed by mass-wasting LGM determine the density of colluvial wedge as this also influences later re-surfacing. We eroded free-face upwards and the un-eroded upper slope downwards until they intersect. This line of and the un-eroded upper slope downwards eroded free-face upwards A Holocene <1m thick colluvial for tens of metres along strike. is horizontal cut-off, intersection, the footwall been able to project the lower slope beneath this define ground surface at wedge exists, but we have Fig. 34). cut-off; the time of demise last glacial maximum (hangingwall Ground Penetrating Radar (GPR) and shallow trench excavation: 36 with supporting elemental analyses with ICPMS and ICPOES, plus blanks and spiked samples. The surface plus blanks and spiked with supporting elemental analyses ICPMS and ICPOES, the subsurface portion of fault plane. Throw after the Last Glacial Maximum and throw-rate: is continuous for tens plane defined by the slip-vector, measured in the vertical cut-off, off and the hangingwall and is 15.5 ± 1 metre. This implies 20.9 –of metres along strike 18.4 metres slip in the plane of fault since the demise of last glacial maximum. If we assume age slopes is between 12 and 18 ka, 1999; 15 ± 3 ka), the implied throw- from climate data (Allen et al., the known age of demise LGM is 1.35 ± 0.4 mm/yr. is 1.06 ± 0.3 mm/yr and the slip-rate rate geological field trips 2016 - 8(1.2) itinerary 51 5 Cl 36 Cl site. Instead, 36 atoms per gram. Thus, atoms per gram. 5 Cl in the 56 samples whilst Cl increase from ~0.5 x 10 36 36 Cl profile from a hypothetical time Cl profile from a hypothetical 36 Concentrations of Concentrations etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Cl concentrations above the hangingwall cut-off. the hangingwall above Cl concentrations 36 atoms/gram measured 5 metres above the hangingwall cut-off of the cut-off the hangingwall measured 5 metres above atoms/gram 5 Cl since exhumation above the ground by surface slip, and during their the ground by surface slip, Cl since exhumation above 36 We modelled the data (black points in Fig. 36a) using code of Schlagenhauf et al., We Cl data and expected resolution of time versus slip: Cl interpretation: Cl as a function of height up the fault plane at this site if has been slipping constant Holocene DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. concentration profile. Furthermore, we have calculated a hypothetical calculated a hypothetical profile. Furthermore, we have concentration 2010 with the site geometry parameters (fault dip, upper and lower/hangingwall slope dips, total scarp height) upper and lower/hangingwall (fault dip, 2010 with the site geometry parameters of of this site. The red dashed lines on Fig. 36b show the expected variation obtained from our LiDAR survey residence in the sub-surface. Thus, the rate of exhumation the uppermost free-face that is now eroded and residence in the sub-surface. Thus, rate not amenable to sampling must be factored in calculate the accumulation of rate based on 15 ± 3 ka as the beginning of the Holocene. Clearly, the fault has not been slipping at a constant based on 15 ± 3 ka as the beginning of Holocene. Clearly, rate exhuming low slip has been rapid, Recent rate. we have concentrated on resolving slip-rate variation through time. variation on resolving slip-rate concentrated we have LGM slope. Error bars associated with accelerator mass spectrometry are ± ~0.1 x 10 slope. Error bars associated with accelerator LGM samples will have accumulated samples will have 36 in the trench to ~2 x 10 atoms/gram 36 36 although we have rock samples from between the heights of our 56 analyses, we have not analysed these rock samples from between the heights of our 56 analyses, we have although we have because analytical error bars would not allow further resolution of details the height versus versus slip dataset that includes slip magnitudes of <50 cm. We have found that it is not possible to recover have slip dataset that includes magnitudes of <50 cm. We versus time data using model fitting with certainty - that we know are in the input slip versus < 50 cm slip events analytical uncertainty shows that as described above, unless samples spaced <~ 5 cm are analysed. However, conclude that it will if samples spaced this closely are analysed. We no increase in resolution can be achieved expected at our the 0.2 m slip events like individual earthquakes be challenging to recover they were in the sub-surface. We do this by including exhumation faulting for the full extent of free- they were in the sub-surface. We Our approach is possible than specifying a so-called “pre-exposure” value. face in the modelling, rather of the LGM cut-offs and hangingwall because the scarp profile from LiDAR, with reconstructed footwall the can iterate of faulting since 12-18 ka. We rate slope (Fig. 35), defines the offset and time-averaged information slope (12-18 ka) as extra of faulting to model the 56 samples using age LGM actual rate not considered. This approach is similar if the entire extent of free-face was that would not be available to that termed “seismic pre-exposure” 2010. by Schlagenhauf et al., geological field trips 2016 - 8(1.2) itinerary 52 (d) (a) time versus slip. The slip. time versus (c) Cl data at this site would 36 Cl results for the Serrone scarp. Cl results for the Serrone scarp. (b). 36 interpretation; (b) Fig. 36 - close-up of best fit to the data shows a pulse of rapid slip that best fit to the data shows a pulse of rapid identified in coincides with palaeo-earthquakes 1996). (see Michetti et al., trenches along strike Data; earthquake surface slip at this site was most surface slip at this site was earthquake slip) zero much smaller (or even likely compared to our sampling and thus is not slip that we The period of rapid resolved. infer from the coincide with the timing of the earthquake of coincide with the timing of earthquake which produced strong shaking in 801 A.D., between and an additional event Rome, inferred that was and 1349 A.D. 1000 A.D. 1996 for from trenching (see Michetti et al., This is the first discussion of these events). time that cosmogenic dating of a bedrock to fault scarp has been explicitly linked paleoseismic trench results along strike along the same fault. etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Cl concentrations (Fig. 36c) through multiple model runs. Two model runs are shown (Fig. 36c) through multiple model runs. Two Cl concentrations 36 DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. (blue and green circles) in which the recent slip rate on the fault has been higher than Holocene average (blue and green circles) in which the recent slip rate Although both of these models fit the data better than a model that assumes ago. since ~1500 years rate the lowest RMS is obtained when we include a long elapsed time since significant slip rate, Holocene-averaged ago; green circles in Fig. 36d). Note that the 1915 Fucino accumulated at this site (800 ± 200 years To fit a model to the data we have used an optimisation approach that seeks to minimise misfit between fit a model to the data we have To measured and modelled geological field trips 2016 - 8(1.2) itinerary 53 Cl concentrations to resolve a history of fault to resolve Cl concentrations 36 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins It is possible to use Fig. 37 - Panoramic view of the Venere Fig. 37 - Panoramic the geological profiles in Figs 39 and 40. quarries nowadays. Red line shows the trace of line shows the trace Red quarries nowadays. the 1915 surface faulting along San stars Benedetto-Gioia dei Marsi fault. Yellow of lines indicate the trace locate pictures. Yellow DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Conclusions from this site and implications: STOP 1.5 – The Venere quarries: surface faulting of the 1915 earthquake and paleoseismic evidence The Stop focuses on the surface faulting of along the San the 1915 Fucino earthquake Benedetto-Gioia dei Marsi fault section (Figs of evolution 37 and 38) on the post-LGM this sector of the Fucino basin. slip despite concerns that climate changes and mass wasting might dominate exhumation of samples. However, we might dominate exhumation of samples. However, slip despite concerns that climate changes and mass wasting and to mass wasting carefully to exclude that this is only possible where the site chosen very strongly-emphasise also emphasise that the geometry of scarp and knowledge We exhumation purely through fault slip. resolve that allow constraints extra age of the climate change that formed geometry scarp (15 ± 3 ka) gives than simple pre-exposure. Although we doubt that modelling to include so-called seismic pre-exposure rather constant through time. Our was we are able to test whether the slip-rate can be resolved, individual earthquakes in traditional resolved slip that corresponds with the timing of palaeoearthquakes results show a phase of rapid slip indicates to the NW and historical record. The rapid palaeoseismic trenches a few kilometres along strike clustering must be included in calculations be strongly clustered in time. Temporal recurrence may that earthquake elapsed time since the last probabilities that combine mean recurrence intervals, that attempt to define earthquake produced by and clock-advance earthquake, Coulomb stress transfer. geological field trips 2016 - 8(1.2) itinerary 54 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. We follow a 500 m long segment of the 1915 fault, We 83 Santilli, at km 13.1 of SS starting from Cave Marsicana (starting point; Fig. 38) up to a point by eye- observed was where the fault reactivation allows a witnesses (Fig. 41). The quarry excavation of the geologic and geomorphic 3D observation features that are the effect of repeated Late Quaternary coseismic surface faulting events. Quaternary geology and paleoseismology in the Fucino L’Aquila basins : Left : exposure Right Fig. 38 - Exposure in the Cave Santilli of the San Fig. 38 - Exposure in the Cave of the fault inside quarry and detail faulted debris. picture taken in the ‘80s northern part of picture taken Santilli (location in Fig. 37). present Cave Benedetto-Gioia dei Marsi fault ruptured in 1915. DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Particularly, one of the quarry walls (location in Fig. 37) exposes a limestone wave cut terrace (Fig. 39 left; cut terrace (location in Fig. 37) exposes a limestone wave one of the quarry walls Particularly, and the overlying terrace WT in Fig. 39 right) buried by the Late Glacial and Holocene talus. Both wave-cut fan delta metres high. Just upon this erosional surface, LGM debris are affected by a fault scarp several in other ancient quarries, some hundred meters to the east, near San Veneziano deposits were observed platform to about 20 ka. Its present position abrasion the age of lake Village (Fig. 40 left), constraining metres along the San Benedetto-Gioia dei Marsi fault section (Radmilli, uplifted by several indicates that it was 1995). 1970; Giraudi, 1956; 1981; Raffy, geological field trips 2016 - 8(1.2) itinerary 55 al., 1993). al., rock wave- Late Glacial stratified slope- Late Glacial stratified 2) etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Surface faulting. The profile trace is shown as C-C’ in Figs 11 and 37. is shown as C-C’ Surface faulting. The profile trace SF) Holocene talus with a level containing Neolithic pottery; Holocene talus with a level 1) wave-cut terrace; terrace; wave-cut WT) , the Riparo di Venere site (Radmilli, 1956), few hundreds of meters north of Cave Santilli 1956), few hundreds of meters north Cave site (Radmilli, , the Riparo di Venere bedrock; e.g. 3) Fig. 39 - Left: Exposure of the limestone wave-cut terrace in the Cave Santilli quarry. Right: Geological profile showing a bed Santilli quarry. in the Cave terrace Fig. 39 - Left: Exposure of the limestone wave-cut waste deposit; waste cut terrace associated to the LGM high-stand of the Fucino Lake, displaced several times during the Holocene (after Blumetti et displaced several high-stand of the Fucino Lake, associated to the LGM cut terrace 50 to 100 cm. Legend: The 1915 offset was DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. (Fig. 37). The latter shows LGM high-stand lakeshore gravel deposits covered by fire places with charcoal and deposits covered gravel high-stand lakeshore (Fig. 37). The latter shows LGM are presently buried terrace and the wave-cut The caves other archaeological remains dated at 19 to 12 ka BP. debris are affected by a and the overlying terrace by the Late Glacial and Holocene talus. Both wave-cut clearly reactivated metres high, locally subdivided into subsidiary segments. This scarp was fault scarp several displacement of 50-100 cm. with an average also during the 1915 earthquake Some Paleolithic sites are located in the caves at the inner edge of the wave-cut terrace, at the base of terrace, at the inner edge of wave-cut sites are located in the caves Some Paleolithic bedrock cliff, geological field trips 2016 - 8(1.2) itinerary 56 WT) Fan delta Fan 2) bedrock; 4) Lacustrine sediments; 1) Surface faulting. SF) Late Glacial to Holocene talus; 3) etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 40 - Up: fan delta deposits affected by a listric normal fault, Wave-cut terrace; terrace; Wave-cut antithetic to the Fucino master fault, in an ancient quarry located Santilli, near San Veneziano. some hundred meters east of Cave Based on this and other exposures in the surrounding of San Village (near Gioia dei Marsi), the cross section down Veneziano (modified, after Blumetti et al., showing the “lower terraces” drawn listric 1993; see location in Figs 11 and 37). It shows several to the slope, ca. 20 parallel normal faults, defining a little graben down-throw of m wide and more than 100 long, with an overall a few metres. Legend: deposits; Inside the ancient quarries of San Veneziano, it was possible it was Inside the ancient quarries of San Veneziano, listric normal faults, defining a little graben to detect several to the slope, c. 20 m wide and more than 100 parallel down-faulting of a few metres (Fig. 40). long, with an overall soil. In fact, the These faults do not displace the present-day the structure is truncated by an erosion surface that levels top of the alluvial sequence. Instead, a few metres downslope, the same erosion surface is affected by some fault scarps that produce a series of topographically to the running parallel depressed and uplifted belts, always a maximum height of few metres, slope. They have length of a few hundreds meters and width tens of metres, and were formed prior to the 1915 earthquake. Santilli following the fault scarp to ESE. Another Cave leave We of on the wall exposure of recent faulted deposits is preserved described log was an old quarry (Fig. 41). Here, a stratigraphic 2008 (Fig. 41), allowing to identify at least by Saroli et al., occurred after 14-15 ka BP. three displacement events DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) itinerary 57 2 4 It : The Left : The same outcrop represents the result 5 Fig. 42 - Leonello’s hair. Leonello’s 1915 coseismic slip was by two eye- observed witnesses (Alfonso Di and Antonio De Salvatore Angelis) here with Leonello 1988). et al., (Serva Serva Right The ageing later. 30 years is clearly visible on etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. gravels indicate deposition along the shoreline, while unit gravels vineyard. Here, two eye-witnesses of the 1915 Here, two eye-witnesses vineyard. (Fig. 42) reported that here the earthquake about 70 cm. coseismic offset was 3 Quaternary geology and paleoseismology in the Fucino L’Aquila basins ). The characteristics of unit ). The characteristics 1 Fig. 41 - Recent faulted deposits on the wall of an inactive quarry. The stratigraphic log is described in Saroli et al., 2008. log is described in Saroli et al., The stratigraphic quarry. of an inactive faulted deposits on the wall Fig. 41 - Recent of the re-organisation of alluvial gravel along the lacustrine shoreline. of the re-organisation alluvial gravel (gravels in sandy matrix) is interpreted as a colluvial wedge deposited from a coseismic scarp. Finally, unit Finally, in sandy matrix) is interpreted as a colluvial wedge deposited from coseismic scarp. (gravels shows a pit-fire containing fragments of Eneolithic (Copper Age) and Bronze Age pottery shards (3000-1500 B.C.) inside unit Age pottery shards (3000-1500 B.C.) of Eneolithic (Copper Age) and Bronze containing fragments shows a pit-fire (just below the present soil, unit DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. About 150 m towards east, the limestone fault plane is very well exposed at the edge of an abandoned east, the limestone fault plane is very About 150 m towards geological field trips 2016 - 8(1.2) itinerary 58 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 43 - Reproduction of the original photographs in the paper of Oddone (1915). of the original photographs Fig. 43 - Reproduction DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. STOP 1.6 – 1915 coseismic rupture in the lake sediments and trench logs the a ground rupture, directed toward dei Marsi, Oddone (1915) observed of San Benedetto and Venere West sediments with an offset of 30 to 90 cm (Oddone, northern edge of the Fucino basin, dislocating recent lake similar to those commonly paper) indicate a complex scarp, 1915). The images in Fig. 43 (from Oddone’s bed had been it must be recalled that the lake soft sediments; actually, in ruptures involving observed close to table is still very (1875) and the water definitely reclaimed only a few decades before the earthquake the surface, especially in winter. still evident in the ’90s (Fig. 44). After farming activities since then, a subdued scarp was Despite the intensive but the fault can still be discerned and actually seen the scarp is now almost vanished, nearly 20 more years, ditches bordering the farmed fields cutting across shallow as the water very even excavations, in vertical located between the 1996 trenches of Michetti et al. orthogonally to it. A clear example is shown in this Stop, (summary in Galadini & Galli, 1999). (1996) and those of Galadini & Galli near Venere geological field trips 2016 - 8(1.2) itinerary 59 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 44 - Scarp of the 1915 coseismic rupture in southern outskirts of San Benedetto dei Marsi, where the paleoseismological trenches of Michetti (location 1996 were excavated et al., and log in Fig. 48). DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. The first two paleoseismological trenches in the Fucino basin were dug across this scarp 1996 (Michetti et al., 1996), just in the southwestern outskirts of San Benedetto (location Fig. 48), soon followed by a number dei Marsi in Fig. 48). trenches across different fault segments by Galadini & Galli (1999) (trenches near Venere The planned Stop is located close to the trench site # 4 in Galadini & Galli (1999) and less than 2 kilometers to one of shallow takes from the trenches of Michetti et al. (1996) (Fig. 44). From parking lot, a short walk ditches cutting across the fault (Fig. 45) where, on its western face, can be clearly seen (2016). sediments (Fig. 46). More details are reported in Galli et al., most recent lake geological field trips 2016 - 8(1.2) itinerary 60 th Fig. 46 - Close-up view of the fault rupture at Stop 1.6. etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. The exposed section is ca. 90 cm high and shows, lacustrine light grey-blue below the ploughed level, silts (early Holocene; right side in Fig. 46) clayey rich of faulted against grey silts, and sandy gravels pottery shards. The latter are mantled by Roman silt deposited during the last high- light-grey (Middle Age-19 of the Fucino Lake standing levels this section likely century). Beside the 1915 event, records the previous 508 AD earthquake. evidence of The schematic logs in Fig. 48 give to the 1915 comparable historical faulting events without being able to precisely earthquake, their occurrence time, because of the constraining ages. large uncertainties in radiocarbon Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 45 - The 1915 rupture at Stop 1.6 (see Fig. 46 for close-up view). DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Based on stratigraphic and archaeological Based on stratigraphic evidence, Michetti et al. (1996) have since the VI century, inferred two events i.e. after the obstruction of Emperor Claudius’ for lack of system, likely drainage return to flood maintenance, and the lake (B) is constrained the area. An event between 550 and 885 CE, possibly referable that caused to the 801 or 847 earthquakes (Galli & Molin, 2014). damages in Rome geological field trips 2016 - 8(1.2) itinerary 61 : M96 : trenches GG Fig. 47 - Panorama Galli (1999). view of the 1915 ruptures between San Benedetto and Gioia. There is no general consensus regarding the rupture along the fault. Parasano trenches of Michetti et (1996), al., described in Galadini & in Galli & Molin (2014). etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. A more recent event (A) might have occurred afterwards, still in the Middle Age but before 1349 occurred afterwards, (A) might have A more recent event of such a because since then the historical seismic catalogue is deemed complete for events earthquake, in historical times occurred magnitude. Instead, Galadini & Galli (1999) infer only one penultimate event at 426-782 CE). They between the II and XV centuries (only in their trench # 5 age is better constrained responsible of significant damages to the strongly felt in Rome, to the 508 earthquake attribute this event A of Michetti et al., aside the more obscure event leaving Colosseum (Galli & Molin, 2014). In summary, to the 1915 one, comparable earthquake (1996), the paleoseismological evidence points to a post-Roman corresponding to the 508 or 801 –most likely left historical and archaeological traces which have 847 events, by Galadini & Galli (1999) because are excluded the 801 and 847 events Actually, of partial collapses in Rome. as summarized basin, Aquae Juliae fault near Venafro), attributed to other capable faults (L’Aquila tentatively geological field trips 2016 - 8(1.2) itinerary 62 : M96 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins : Galadini & Galli, 1999). GG Fig. 48 - Location of Stop 1.6 and trench logs across the 1915 rupture in the San Benedetto-Venere dei Marsi area ( Fig. 48 - Location of Stop 1.6 and trench logs across the 1915 rupture in San Benedetto-Venere Michetti et al., 1996; Michetti et al., DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) itinerary 63 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins DAY 2 L’Aquila basin field trip (afternoon) inside L’Aquila city. field trip (afternoon) inside L’Aquila Quaternary geology and palaeosismology in the Field trip stops in the middle Aterno Valley. The black box encloses the area covered by Part 2 of the by Part encloses the area covered The black box Valley. Field trip stops in the middle Aterno DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) itinerary 64 in etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 49 - Panoramic view of the middle Aterno Valley from San Martino d’Ocre. From NW (to the left) to SE right) ma Valley view of the middle Aterno Fig. 49 - Panoramic villages close to L’Aquila town are clearly visible. The Gran Sasso range (with its main peaks) is in the background. Sasso range town are clearly visible. The Gran villages close to L’Aquila DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. STOP 2.1 - Panoramic view from San Martino d'Ocre to the north and south correspond some major highs bounding the valley The main topographic (PSDFS). In the System - San Demetrio Fault Quaternary normal fault scarps belonging to the Paganica source and the earthquake fault scarp of the 2009 L’Aquila it is possible to see the cumulative sector, Paganica dots) surface coseismc breaks were sites where continuous (red dots) and discontinuous (yellow fault scarp is visible (Stop 2.2). In the San Demetrio sector another Quaternary cumulative observed. is filled with a complex sequence of continental deposits. Among the oldest sediments, Early The valley (Stop 2.4) are found. The south-eastern part Pleistocene lacustrine silts (Stop 2.3) and fan-delta conglomerates uplift of the PSDFS. exhumed and dissected by the long-term activity footwall progressively of the basin was geological field trips 2016 - 8(1.2) itinerary 65 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. range between 0.2 and 0.4 mm/yr (Fig. 51). range preliminary stratigraphic sketch of the fault zone sketch preliminary stratigraphic c) Quaternary geology and paleoseismology in the Fucino L’Aquila basins for the investigated portion of the fault are consistent, and for the investigated estimated that the late Holocene and Pleistocene dip-slip rates close-up view of a fault splay close to the San Demetrio Ne’ close-up view of a fault splay view and a) to the rupture of the whole PSDFS. Moreover, Cinti et al., (2011) Cinti et al., Moreover, to the rupture of whole PSDFS. b) aternary composite fault scarps and paleoseismological investigations for earthquakes in the past larger than the April 6, 2009 event, likely related likely in the past larger than April 6, 2009 event, for earthquakes - Qu Fig. 50 - Village. The red stripe shows the location of paleoseismological Vestini trench.; exposed in the eastern trench wall (after Blumetti et al., 2015). (after Blumetti et al., exposed in the eastern trench wall DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. STOP 2.2 - San Demetrio Ne' Vestini along the PSDFS were performed in order to reconstruct its Late investigations Paleoseismological Pleistocene–Holocene rupture history. Here, the fault displaces Early- sector. of the San Demetrio Ne’ Vestini a splay Blumetti et al. (2015) investigated Middle Pleistocene alluvial fan deposits (VIC), Middle-Late sediments (SMA) and, in the fault zone, (2011), Galli Holocene colluvial deposits and presents a ca. 25 m-high composite fault scarps (Fig. 50). Cinti et al., sector. fault at the Paganica causative the 2009 earthquake (2013) excavated (2010; 2011) and Moro et al., et al., distinct (2011) conclude that 1) five record at four different sites, Cinti et al., By interpreting the paleoearthquake and 2) there are indications occurred since 2900-760 B.C. (including the 2009 event) surface faulting earthquakes geological field trips 2016 - 8(1.2) itinerary 66 view of the main fault zones. At this site, the At view of the main fault zones. e) and d) etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. excavation along the Paganica sector crossing the 20 m-high along the Paganica excavation Quaternary geology and paleoseismology in the Fucino L’Aquila basins a) detailed log of the NW wall of the trench; detailed log of the NW wall c) and b) Fig. 51 - Aqueduct site trench (after Cinti et al., 2011). Fig. 51 - Aqueduct site trench (after Cinti et al., zone 2 (FZ2) the 2009 ruptures produced diffuse deformation accompanied both by cracking and warping. 2 (FZ2) the 2009 ruptures produced diffuse deformation accompanied both by cracking zone 2009 ruptures occurred at the base of scarp on fields and tarmac road adjacent to pipeline. In coincidence fault cumulative scarp. cumulative DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) itinerary 67 This formation testifies the late Fig. 54 - Small conjugate normal faults affecting laminated for scale on bottom left). silts and fine sands (scraper etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins STOP 2.3 - Poggio Picenze Early Pleistocene lacustrine deposits This outcrop shows Early Pleistocene lacustrine deposits (limi di San Nicandro fm. - SNL), composed of laminated, calcareous silts and sands with thin whitish, fine-grained silts, containing at places small leaves of clayey layers (Figs 52-54). fragments basin opening when the stage of the middle Aterno depocenter probably reached its maximum depth. The formation has a maximum thickness > 100 m. In the more intercalations due to facies it shows sparse gravelly proximal of the fan-delta deposits (Stop 2.4). the progradation Fig. 52 - Location map and geology of Stop 2.3 Fig. 53 - outcrop of lacustrine deposits. The considerable dip of Fig. 53 - outcrop of lacustrine deposits. The considerable (after Pucci et al., 2015). (after Pucci et al., the bedding (~20° to W) is mostly due tectonic tilting. DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) itinerary 68 which consists of The general dip to The general , . Fig. 57 - High-angle conjugate normal faults affecting the Fig. 57 - High-angle conglomerates. Vall’Orsa etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins STOP 2.4 - Le Macchie Early Pleistocene Gilbert fan delta conglomerates fm. (VOC) This outcrop shows the Vall’Orsa Early Pleistocene thick and polygenic beds of carbonatic with sparse, thin and with sandy matrix mixed conglomerates (Fig. 55). Clinoforms, cross-bedding layers whitish clayey-silt and pinch-out structures are visible, together with some sets of conjugate normal faults (Figs 56, 57). This formation the limi di San Nicandro fm. (SNL) overlies the SE of the foresets testifies the progradation of a huge fan- the SE of foresets testifies progradation an early flow towards delta system and a consistent drainage basin. south-eastern depocenter in the middle Aterno Fig. 55 - Location map and geology of Stop 2.4 Fig. 56 - Carbonatic conglomerates showing foreset beds Fig. 56 - Carbonatic conglomerates (after Pucci et al., 2015). (after Pucci et al., the Limi di San Nicandro Fm. related to a Gilbert fan delta. This unit is partially heteropic with DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) itinerary 69 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 59 - Panoramic view from the NE of the Valle dell’Inferno right flank. view from the NE of Valle Fig. 59 - Panoramic This Stop dell’Inferno showing view of the Valle is a panoramic the relationship between normal faults, continental deposits and (Fig. 58). evolution drainage Here a fault scarp truncates two wide surfaces: higher erosional on Cretaceous limestones and a lower depositional surface carved surface corresponding to the top of Early Pleistocene alluvial fm. - VOC). This fault succession (Vall’Orsa fan conglomerate belongs to an E-trending system that acted mostly during Early by the more recent lately deactivated Pleistocene times and was This kinematic change is faults of the PSDFS. NW-trending dell’Inferno gorge, which denotes a dramatic testified by the Valle network, with a new SW-flowing reorganization of the river completely different from the Early Pleistocene SE- drainage, flowing one (Fig. 59). Fig. 58 - Geological map of the Valle Inferno area (after Pucci et al., 2015). Inferno area (after Pucci et al., DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. STOP 2.5 - Valle dell’Inferno The syntectonic deposition and drainage evolution geological field trips 2016 - 8(1.2) itinerary 70 Fig. 61 - Simplified NE-trending Fig. 60. Trace location in Fig. 15. Fig. 60. Trace geological section showing the main Quaternary fault pattern and the continental depositional units (yellow, the pale green and blue) over undifferenitated carbonate pre- Quaternary bedrock (dark green) 2015). The black (after Pucci et al., rectangle encloses the area shown in Along the Valle dell'Inferno is visible Along the Valle the close alternance of synthetic with the and anthitetic fault splays, ones accommodating SW-dipping most of the displacement, that influence the thickness of Quaternary depocenters (Figs 60 and 61). etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Fig. 60 - View to the west showing details of Valle dell'Inferno right flank with the top of Early Pleistocene conglomerate succession (Vall’Orsa fm.) abutting against the N-dipping normal fault in Cretaceous limestones geological field trips 2016 - 8(1.2) itinerary 71 s Location of site a) Stratigraphic cross sections and V Stratigraphic Fig. 62 - et al., 2015). et al., investigations in the area under study; investigations b) profiles from down-hole, surface wave and seismic dilatometer test (Amoroso (Milana et al., 2011; Tertulliani et al., 2011; Tertulliani (Milana et al., 2012; Amoroso et al., 2012; Totani 2014; 2015). In particular, et al., locally well underground caves, in known and commonly recognized are more the “brecce dell’Aquila”, frequent than in other parts of the city centre. Fig. 62a shows the location of the site investigations, and RC buildings underground caves collapsed due to the 2009 within the area of earthquake, etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. STOP 2.6 - South L’Aquila damage due to the main shock causing several RC buildings collapsed or suffered severe several In South L’Aquila, in the collapse of 11 report that 135 victims were concentrated forensic surveys tens of victims. Post-earthquake of damage buildings located in this area (i.e. about 44% of the total number casualties). The huge concentration within this area created speculation for both poor design and construction techniques, also related to inadequate by the Italian building code in use at time of their construction. Indeed, of the seismic action provided evaluation complex and can cause significant amplification effects. In the area site effects the local subsoil condition is very soils amplification due fine-grained be related to: lithostratigraphic (“terre rosse”) interposed within, or placed breccias the coarse-grained above, effects topographic man-made fills; underground caves; (“brecce dell’Aquila”); geological field trips 2016 - 8(1.2) itinerary 72 S in the 400-700 m/s values of the subsoil values S S ≈ 400 m/s, man-made fills of maximum S etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Fig. 64 - Example of RC building collapsed in Via Campo di Fossa during the April 6, 2009 main shock. di Fossa Quaternary geology and paleoseismology in the Fucino L’Aquila basins (≈ 200-300 m/s). Examples of collapsed buildings are shown in Figs 63 S Fig. 63 - Example of RC building suffered severe damage in Fig. 63 - Example of RC building suffered severe Via Cola dell’Amatrice during the April 6, 2009 main shock. Via Cola dell’Amatrice DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. thickness ≈ 8-10 m with lower V layers. The upper portion of the subsoil is constituted by the “brecce dell’Aquila”, with shear wave velocity V velocity with shear wave The upper portion of the subsoil is constituted by “brecce dell’Aquila”, layers. field trip. In addition, Fig. 62a includes the line of the section named “A-A’”, while Fig. 62b shows the In addition, Fig. 62a includes the line of section named “A-A’”, field trip. V velocity profile of this cross section and the shear wave and stratigraphic topographic ≈ The breccias are superimposed to lacustrine deposits, with V 600-1000 m/s or higher. and 64. Figs 65 and 66 shows two caves, located respectively in Via Campo di Fossa and Via De in Via Campo di Fossa located respectively and 64. Figs 65 66 shows two caves, sinkholes during the April 6, 2009 main shock. In this respect Bartholomaeis, that originated impressive were performed, and still ongoing, related to and geotechnical investigations geological, geophysical many studies and research activities for supporting the reconstruction planning Seismic Microzonation et al., 2014; 2015; Totani (Amoroso et al., 2012). range, and laying on the bedrock. The upper portion of subsoil is irregularly affected by peculiar local and laying range, “terre rosse” with V conditions (Fig. 62b): underground caves, geological field trips 2016 - 8(1.2) itinerary 73 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Fig. 66 - Example of cave (areal extension ≈ 60 m Fig. 66 - Example of cave Working Group, 2010). Group, Working originated with a maximum depth of 14 m) in Via De Bartholomaeis during the April 6, 2009 main shock (MS–AQ Quaternary geology and paleoseismology in the Fucino L’Aquila basins was built in 1257 and repeatedly restored during times for was , is the biggest square of the city and the market place since 1303. The square has always , is the biggest square of city and market Cathedral of Santi Massimo e Giorgio Fig. 65 - Example of cave originated in Via Campo di Fossa Fig. 65 - Example of cave during the April 6, 2009 main shock. DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. damage causeed by earthquakes. Historical chronicles report that this church, reconstructed after the 1315 damage causeed by earthquakes. Also the 1915 damaged this church. During 1703 event. totally collapsed during the destructive earthquake, and part of the apse the transept damaged. In particular, severely was the cathedral the 2009 earthquake damaged. severely ceiling was collapsed, and the vaulted STOP 2.7 - Piazza Duomo Piazza Duomo represented the cultural centre of the city.represented the cultural The top surface of the bedrock in Piazza Duomo is located below 300 m depth, as shown in the deep borehole of Fig. 67. The geological field trips 2016 - 8(1.2) itinerary 74 Fig. 68 - S. Maria del Fig. 68 - S. earthquake. Suffragio church after L’Aquila Suffragio by the earthquake. The by the earthquake. damaged severely church was in by the 2009 earthquake, particular the superb dome the (attributed to G. Valadier), lantern and the spires collapsed. The and transept roofing were in danger of collapse. etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins church (better known as Anime Sante Church – Fig. 68) was S. Maria del Suffragio Fig. 67 - On the left a stratigraphic column reconstructed from a 300 m deep core-destructive Fig. 67 - On the left a stratigraphic medium-grained, mostly silty lacustrine deposits, more than 220 m thick. medium-grained, borehole executed in Piazza Duomo, L'Aquila (Monaco et al., 2013, after Amoroso et al., 2010): the top 2013, after Amoroso et al., (Monaco et al., L'Aquila in Piazza Duomo, borehole executed surface of the bedrock in city centre is located below 300 m depth. The upper portion subsoil, size of variable fine to coarse calcareous fragments 80 m thick, is constituted by “brecce dell'Aquila” by highly variable (mostly of some centimetres) embedded in sandy or silty matrix, characterized residual soils, locally known as "terre rosse", are cementation and mechanical properties. Fine-grained encountered in the upper 8 m, at top of breccias. The breccias are superimposed to fine-to The starting to be built soon after the 1703 earthquake in place of a small church that was destroyed in place of a small church that was starting to be built soon after the 1703 earthquake DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. geological field trips 2016 - 8(1.2) itinerary 75 Fig. 71 - Particular of the Fig. 71 - Particular collapsing. Biblioteca Tommasi. The building Biblioteca Tommasi. damaged: the severely very was in danger of main facade was Dander & Moretti 1974). s s ≈ 600- s etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins April 2009. The Palace was built in 1294 for the establishment was April 2009. The Palace ≈ 200-300 m/s) are found in shallow fill s th Fig. 70 - Profiles of shear wave velocity V velocity Fig. 70 - Profiles of shear wave materials (0-2 m deep). originally ≈ reduced as a consequence of the 1703 70 m, was et al. 1997, and then modified in the upper part (Colapietra earthquake, measured by seismic dilatometer tests (SDMT) in column at 2 backfilled boreholes and stratigraphic (Monaco et Margherita, L'Aquila the site of Palazzo 2013). The upper portion of the subsoil belongs al., formation (V to the "brecce dell'Aquila" size, in grain possibly reflects some variability cementation and/or mechanical properties. Lower (V values 1000 m/s or higher), and corresponds roughly to The dispersion of the V the upper 80 m deep. Fig. 69 - Upper panel: Palazzo Margherita after the 2009 earthquake. Lower panel: glimpse of the square. DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. STOP 2.8 - Piazza Palazzo Margherita represented the political centre of city due to presence Palazzo This square has always (Fig. 69), seat of the municipality until 6 of the “Capitano” seat, the main local representative of the royal authority during the Middle Age. In 1572- of the royal of the “Capitano” seat, main local representative held by Queen Margherita deeply restored to become the set of Abruzzi Government was 1577 the Palace damage to Palazzo caused severe the name to building. The 1703 earthquake that gave d’Austria, the height of tower, In particular, Margherita, as testified by the historical documentation on its restoration. geological field trips 2016 - 8(1.2) itinerary 76 seismic s measured in the breccias are ≈ 200-300 m/s) have been ≈ 200-300 m/s) have S s Fig. 74 - Profiles of V (0-4 m deep). locally measured in shallow fill materials dilatometer tests (SDMT) measured in 2 backfilled boreholes and schematic soil - profile at the site of Piazza del Teatro 2013). Scuola De Amicis (Monaco et al., The upper portion of the subsoil belongs to formation, and the "brecce dell'Aquila" corresponds roughly to the upper 80 m The V deep. mostly ≈ 600-1000 m/s or higher, increasing with depth. Lower generally (V values etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 73 - Scuola De Amicis after L’Aquila earthquake. L’Aquila and was damaged by the 1461 and was In and the 1703 earthquakes. 1875 the building became a military infirmary and finally in 1909 it turned in a school 1992). (Centofanti et al., April 2009. It was built during the XV century for the establishment of San Salvatore Hospital built during the XV century for establishment of San Salvatore April 2009. It was th DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. collapsed. tower that part of the bell especially the upper damaged the church earthquake severely earthquake cathedral: the 2009 cathedral: Fig. 72 - San Bernardino STOP 2.9 - Via San Bernardino built in XV The church was is one of the most important monument L’Aquila. San Bernardino cathedral damaged the The 1461 earthquake century and the superb façade dates back to first half of XVI century. collapsed almost entirely the cathedral recently built. During the 1703 earthquake dome of the cathedral the façade. excluding De Amicis primary school, strongly damaged by the 2009 earthquake, one of the main school in city was centre until the 6 geological field trips 2016 - 8(1.2) itinerary 77 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 76 - Main workings during the repair and consolidation of damaged and collapsed masonry vaults. STOP 2.10 - Palazzo Ardinghelli Ardinghelli is located in the heart of historical center Palazzo The ground floor The building is on two main levels. of L’Aquila. hall with the is dominated by the presence of passing entrance This floor stairs on the left, and by a colonnaded courtyard. building phases that led its realization. the various reveals Fig. 75 - Reconstruction of the wall completely of the wall Fig. 75 - Reconstruction collapsed in a room on the main floor. DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Conversely, the main floor, at least in the the main floor, Conversely, completely body facing the square, was of 1703, with rebuilt after the earthquake halls and the the creation of large vaulted insertion of a small chapel surmounted by with the facade, dome. Together is the element that characterizes courtyard termination the building. Its exedra differentiates it from almost all of the coherence to and gives buildings in L’Aquila complex. Under the the architectural geological field trips 2016 - 8(1.2) itinerary 78 etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Fig. 77 - Reconstruction of the wooden roofs conserving original configuration. Fig. 77 - Reconstruction DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. stylistic unity provided to the palace by the eighteenth-century intervention, it is hidden an intense layering to the palace by eighteenth-century intervention, stylistic unity provided building of the factory. readable through the structure and character of the principles and it is aimed to the restoration restoration is based on the traditional The intervention and to the re-use of building. The to the seismic improvement damage caused by the 2009 earthquake, able to effectively the Palace plant that makes goal of the project is to equip building with a structural finishing of surfaces and decorations, the restoration it is provided respond to the seismic action. Moreover, repaired with damage was works and the building installations necessary for its future reuse. The earthquake been repaired and have techniques and modern technologies. The damaged masonry vaults mixing traditional The connections between walls been rebuilt with similar technology. consolidated while the collapsed ones have with a systematic shackling at the height of ceilings. A bead reinforced masonry has been realized have and the elements of cover. giving a better connection between the walls on top of the walls, been realized The roofs were reconstructed with wooden the textures masonry. The insertion of artificial diatones improved substantially preserving the original plant but regularizing mesh of main elements. warping, geological field trips 2016 - 8(1.2) itinerary 79 Fig. 79 - Castello earthquake. Cinquecentesco after the 2009 L’Aquila damaged, as well as the offices of INGV seated in the of the upper level castle. etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins The 2009 earthquake caused the partial collapse of upper The 2009 earthquake in the cracks large and extensive and the roof, part of the walls of the building. The historic and artistic heritage walls inside the castle, were seriously Museo Nazionale d’Abruzzo, Fig. 78 - Castello Cinquecentesco after the 2009 L’Aquila earthquake. after the 2009 L’Aquila CKNOWLEDGEMENTS DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. STOP 2.11 - Castello Cinquecentesco started was Located in the highest part of city, building is also known as Spanish Fortress. This massive bastions to be built in 1534 under the Spanish domination. The fortress has a square plan with four massive Historical not supposed to be filled with water. at the corners. The castle is surrounded by a moat that was damaged during the 1703 and 1762 earthquakes. that the castle was accounts revealed in the person of Eng. archeoRes, A special thanks for the generous support offered by company wish to thanks also Americo Santilli, owner Ardinghelli. We Gianluca Olivieri, for permitting our visit to Palazzo permitted our visit. for having of the quarries Stop 1.5, and owners “Le Macchie” shooting-range A Quaternary geology and paleoseismology in the Fucino and L’Aquila basins S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Michetti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori g e o l o g i c a l

f i e l d

t r i p s

2 0 1 6

8 ( 1 . 2 )

80 m e m o r a n d u m

DOI: 10.3301/GFT.2016.02 geological field trips 2016 - 8(1.2) references 81 , M. taly. i & F. ondaggi etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins International INQUA Meeting on Paleoseismology, Active Tectonics Active International INQUA Meeting on Paleoseismology, th and Archaeoseismology 19 - 24 April 2015, Pescina, Fucino Basin, Italy (Blumetti A.M., Cinti F.R., De Martini P.M., Galadini F. De Martini P.M., Cinti F.R., Fucino Basin, Italy (Blumetti A.M., and Archaeoseismology 19 - 24 April 2015, Pescina, Guerrieri L., Michetti A.M., Pantosti D., Vittori E. Eds.), Miscellanea INGV, 27, 511-513, ISSN: 2039-6651. 27, 511-513, ISSN: Vittori E. Eds.), Miscellanea INGV, D., Pantosti Michetti A.M., Guerrieri L., Nowaczyk N., Oberhansli H., Watts W., Wulf S. & Zolitschka B. (1999) - Rapid environmental changes in southern Europe during environmental (1999) - Rapid B. & Zolitschka S. Wulf W., Watts Oberhansli H., N., Nowaczyk the last glacial period. Nature, 400, 740-743. dei s la stratigrafia geologiche, geotecniche e geofisiche per lo studio della risposta sismica locale città dell’Aquila: giugno-agosto 2010. Report CERFIS 1/10. University of L’Aquila. www.cerfis.it/en/download/cat_view/67-pubblicazioni- of L’Aquila. CERFIS 1/10. University 2010. Report giugno-agosto cerfis/68-reports.html (in Italian). 2014, 25-27 November Solida (GNGTS), Proceedings of 32nd Conference Gruppo Nazionale di Geofisica della Terra terrace. ISBN : 978-88-940442-0-1 (raccolta). 2, 122-128, ISBN: 978-88-940442-2-5 (volume), Bologna (Italy), Vol. Sustainable Planning and Landscape Exploitation, - Urban Geology, Engineering Geology for Society and Territory L’Aquila. XVIII, 1097-1100, DOI 10.1007/978-3-319-09048-1_208, Print ISBN 978-3- 5, Part Springer International Publishing, Vol. 319-09047-4, Online ISBN 978-3-319-09048-1. (2011) - Deep geophysical electromagnetic section across the middle Aterno Valley (central Italy): preliminary results after (central Valley electromagnetic section across the middle Aterno (2011) - Deep geophysical doi: 10.4430/bgta0028. Appl., Boll. Geofis. Teor. earthquake. the April 6, 2009 L’Aquila 35, 257–310. Mem. Soc. Geol. Ital., 58, 77-104. Boll. Soc. Geol. It., (Appennino abruzzese). geomorphological features and seismotectonic implications. Earth Surface Processes Landforms, 18, 203-223. on IV Int. Conf. Guide for the excursion, Italy”, of central “Geomorphology and Quaternary evolution Eds., Dramis, Fisica e Dinamica Quaternaria, suppl. III, 2, 1997, 79-103. Italy 1997, Supplementi di Geografia Geomorphology, 288, 183–194. Doi: 10.1016/j.quaint.2012.04.040. Apennines). Quat. Int., basin (Central Valley landscape of the Middle Aterno Italy). Basin, Central fault (L’Aquila 6 Volume Abstracts DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. References Negendank J., J., Mingram A., Mackensen M., Kraml J., Keller Huntley B., Hubbertens H-W., A., Brauer U., Brandte Allen J., G. (2010) - Campagna di indagini & Totani F. Totani M., Tallini B., Taddei Monaco P., Di Eusebio F., Del Monaco F., Amoroso S., Amoroso S., Di Naccio D., Di Giulio G., Vassallo M. & Milana G. (2014) - Site effects along the southern flank of L’Aquila Vassallo Di Giulio G., Di Naccio D., Amoroso S., (2015) - Local seismic response in the Southern part of historic centre P. G. & Monaco, Totani F., Totani Amoroso S., Siniscalchi & Votta A., Romano G., Rizzo Piscitelli E., S., Perrone Lapenna A., Gueguen V., Giocoli E., Galli A., Balasco M.P. Bally A.W., Burbi L., Cooper C. & Ghelardoni R. (1986) - Balanced sections and seismic reflection profiles across the Central I Cooper C. & Ghelardoni R. (1986) - Balanced sections and seismic reflection profiles across the Central Burbi L., Bally A.W., con i fenomeni orogenetici nella Marsica quaternarie della regione fucense ed i loro rapporti Beneo E. (1939) - Le terrazze 6, 293-314. Il Quaternario, (L’Aquila). & Bosi C. (1993) - La tettonica quaternaria della conca di Fossa Bertini T. Italy); Apennines (Central moun-tain fronts in Central & Michetti A.M. (1993) - Fault-generated F. Dramis Blumetti A.M., Gentil & Sardella R. (1997) - Fucino Basin. In: B. J. Raffy C., Petronio Michetti A.M., L., Ferreli Coltorti M., Blumetti A.M., Demetrio fault system in the seismic Guerrieri L. & Vittori E. (2013) - The primary role of the Paganica–San Blumetti A.M., & Guerrieri L. Comerci V. Vittori E., data on the San Demetrio ne’ Di Manna P., (2015) - Paleoseismicity Blumetti A.M., Vestini geological field trips 2016 - 8(1.2) references 82 7. ly: lini nal De ene sins 2009 4. ocene of the 6 F., Tortorici F., , 36, L18308. Doi: Geophys. Res. Lett. etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins L. (1990) - Palinspastic restoration and paleogeographic reconstruction of the peri-Tyrrhenian area during the Neogene. reconstruction of the peri-Tyrrhenian and paleogeographic restoration L. (1990) - Palinspastic 77, 42–50. Doi: 10.1016/0031-0182(90)90097-Q Paleoecol., Paleoclimatol. Paleogeogr. 37, L06308. http://dx.doi.org/10. 1029/2010GL04280 Lett., Res. Mw 6.3). Geophys. Italy, (Central earthquake April 2009 L’Aquila 36, paper 8, 2010. 1441-8142, Vol. Electronic Edition, ISSN of the Virtual Explorer, 579, 173–192. Doi:10.1016/j.tecto.2012.01.026. Tectonophysics, igneous petrology constraints. 27, 955–958. motion, Geology, a subducting slab in retrograde to corner flow above Response Apennines: The correlation of geological events across different intermountane basins. Il Quaternario 16 (1bis), 55-76. Apennines: The correlation of geological events Studi Geol. Camerti, 1991, 257-263. laziale-abruzzese. 198, 233–253. Apennines (Italy): Insights from facies and backstripping analyses. Sediment. Geol., the Central Jour Conticelli & C. Doglioni, The Geology of Italy, M. Mattei, S. A. Peccerillo, and what we imagine. In: (Eds.) M. Beltrando, and correlation with the volcanotectonic activity in Central Italy. Mem. Descr. Carta. Geol. d’It. Mem. Descr. Italy. activity in Central and correlation with the volcanotectonic 49, 63-76. Italy). Sedimentary Geology 148, 29-59. lacustrine deposits of Fucino Basin (Central Italy). Sedimentary Geology 148, 29–59. alluvial and lacustrine deposits of the Fucino Basin (central Miche Mele F., Margheriti L., Marchetti A., Lucente F.P., Improta L., A., Govoni L., Faenza Di Stefano R., Di Bona M., Luca G., L. (2009) - The & Valoroso Seccia D. P., Roselli Piccinini D., Piana Agostinetti N., M., Pastori Moretti M., Monachesi G., A., main shock and aftershocks. Italy) Mw 6.3 earthquake: (central L’Aquila 10.1029/2009GL039627 42, 2–18. http://dx.doi.org/10.1016/j.jsg.2012.06.007. Struct. Geol., Apennines, Italy). J. (central earthquake DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Boccaletti M., Ciaranfi N., Cosentino D., Deiana D., Gelati R., Lentini F., Massari F., Moratti G., Pescatore T., Ricci Lucchi T., Pescatore G., Moratti Massari F., Lentini F., Gelati R., Deiana D., Cosentino D., N., Ciaranfi Boccaletti M., Boncio P., Pizzi A., Brozzetti F., Pomposo G., Lavecchia G., Di Naccio D. & Ferrarini F. (2010) - Coseismic ground deformation F. & Ferrarini Di Naccio D. G., Lavecchia G., Pomposo F., Brozzetti Pizzi A., Boncio P., vs. Tectonics and western mediterranean: of the central Lustrino M. & Doglioni C. (2012) - Geodynamic evolution Carminati E., ba of intrapenninic sedimentary evolution M. (1994) - Tectonic Funiciello R. & Parotto De Rita D., Cosentino D., G.P., Cavinato of Pio-Pleistoc (2002) - Sedimentary and tectonic evolution Miccadei E. & Piacentini T. M., Dall’Asta Carusi C., G.P., Cavinato Bosi C., Galadini, F. & Messina, P. (1995) - Stratigrafia Plio-Pleistocenica della Conca del Fucino. Il Quaternario 8 (1). 83-9 Plio-Pleistocenica della Conca del Fucino. (1995) - Stratigrafia & Messina, P. Galadini, F. Bosi C., & Sposato A. (2003) - Plio-Quaternary continental deposits in the Latium-Abruzzi Messina P. Giaccio B., Galadini, F., Bosi C., Bosi C. & Messina P. (1991) - Ipotesi di correlazione fra successioni morfolitostratigrafiche pliopleistoceniche nell’Appennino successioni morfolitostratigrafiche (1991) - Ipotesi di correlazione fra Bosi C. & Messina P. 135-146. Elsevier, of Geology. Geodynamics: Encyclopedia Carminati E. & Doglioni C. (2005) - Mediterranean in control on the architecture of a Miocene carbonate ramp M. (2007) - Tectonic Mariotti G. & Brandano Corda L., Carminati E., magmatism and geodynamics of Italy: What we know Cuffaro M. & Doglioni, C. (2010) - Tectonics, Lustrino M., Carminati E., Cavinato G.P. & De Celles P. G. (1999) - Extensional basins in the tectonically bimodal central Apennines fold-thrust belt, Ita G. (1999) - Extensional basins in the tectonically bimodal central & De Celles P. G.P. Cavinato of Plio-Pleist (2002) - Sedimentary and tectonic evolution Miccadei E. & Piacentini, T. M., Dall’Asta Carusi C., G.P., Cavinato Centofanti M. (1984) – 1753 – L’Aquila 1983. Il restauro della città. Edizioni Libreria Colacchi, L’Aquila. L. (1992) – & Zordan Properzi P. Conforti C., Edizioni. CARSA città di Piazze. R., Colapietra Centofanti M., L’Aquila De Gori P., Ciaccio M.G., L., Chiaraluce Cecere G., Cattaneo M., Bianchi I., Baccheschi P., Anselmi M., Amato A., C., Chiarabba Chiaraluce L. (2012) - Unraveling the complexity of Apenninic extensional fault systems: a review 2009 L’Aquila L. (2012) - Unraveling Chiaraluce geological field trips 2016 - 8(1.2) references 83 l. ec., Explor., tudi per (2011) - 457-468. -carbonate etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins 36, paper 12. doi:10.3809/jvirtex.2010.00223. detritalmodes in foreland basin system: An example from Upper Miocene arenites of the central Apennines, Italy. Geol. Soc. Apennines, Italy. detritalmodes in foreland basin system: An example from Upper Miocene arenites of the central 420, 107–133. Am. Spec. Pap., 158, 34-47. doi: 10.1016/j.enggeo.2013.03.008. resonance properties vs. subsoil model. Engineering Geology, 403 pp. France, et Documentation, Paris, data and tectonic Apennines (Italy) along the CROP 11 seismic profile: indications from geologic, seismologic and gravity implications. Earth & Planet. Sci. Letters, 280, 1-12. 3 (4), 423-434. Nova, Apennines system. Terra Geophys. Geosyst., 5, Q11003, doi:10.1029/2004GC000724. Geosyst., Geophys. Evidence for surface faulting events along the Paganica fault prior to the 6 April 2009 L’Aquila Earthquake Central Italy. J. Italy. Central Earthquake fault prior to the 6 April 2009 L’Aquila along the Paganica Evidence for surface faulting events 116, B07308. http://dx.doi.org/10.1029/2010jb007988. Res., Geophys. vo Stud. Geol. Camerti, Spec., cinematica. In: Studi Preliminari All’acquisizione Dati del Profilo CROP 11 Civitavecchia-Vasto, Italy. 143–149, Camerino, & M. Parotto, Cavinato G.P. 1991/2, edited by M. Tozzi, Italy. 135–143, Camerino, 1995/2, pp. vol. 644-645, 108-121, . Italy) using airborne LiDAR data. Tectonophysics, fault (Central earthquake 2009 L’Aquila 124, 611–643. Boll. Soc. Geol. Ital., piattaforma carbonatica Laziale-Abruzzese. 66–72. Italy, Nella Sede della Deputazione, Rome, il bicentenario della morte di A.L. Antinori, L’Aquila. DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Critelli S., La Pera E., Galluzzo F., Milli S., Moscatelli M., Perrotta S. & Santantonio M. (2007) - Interpreting siliciclastic S. Perrotta Moscatelli M., Milli S., F., Galluzzo E., La Pera Critelli S., Dander M. & Moretti (1974) – Japadre Editore, L’Aquila. civile Aquilana. Dal XIV al XIX secolo. Architettura Napoli. Giannini ed., e ﬁscalità (secoli XV-XVIII). e il contado: demograﬁa De Matteis A. (1973) - L’Aquila Italy): site (central in historical downtown L’Aquila (2013) - HVNSR survey F. C. & Durante De Rose M., Tallini Del Monaco F., Mémoires et Documents, Centre Recherche adriatiques. Cartographiques (1965) - Géomorphologie des Abruzzes Demangeot J. M. (2009). Deepening of the Adriatic Moho beneath central Tiberti M.M. & Parotto G.P., Cavinato Mele G., Di Luzio E., Doglioni C. (1991) – subductions – A proposal of kinematic modellig for W-dipping – applications to the Tyrrhenian Possible Doglioni C. & Flores G. (1995) – 1-95. Ed. Il Salice, Potenza, An introduction to the Italian Geology. (1998) – & Pialli G.P. 52, Mongelli F. Mem. Soc. Geol. It., Boudinage of the Alpine Belt in Apenninic Back-arc. Doglioni C., Cinti F.R., Faenza L., Marzocchi W. and Montone P. (2004) - Probability map of the next M 5.5 earthquakes in Italy, Geochem. in Italy, (2004) - Probability map of the next M 5.5 earthquakes and Montone P. W. Marzocchi L., Faenza Cinti F.R., A. and Patera Pinzi S. Brunori C.A., Cucci L., Pierdominici S., Civico R., Pucci S., De Martini P.M., D., Pantosti Cinti F.R., Cipollari P. and Cosentino D. (1991) - La linea Olevano-Antrodoco: Contributo della biostratigrafia alla sua caratterizzazione Contributo della biostratigrafia (1991) - La linea Olevano-Antrodoco: and Cosentino D. Cipollari P. Stud. Geol. Camerti, Sp dell’Italia Centrale, M. (1995) - Modello Cinematico-Strutturale and Parotto Cosentino D. Cipollari P., (2015). Morphotectonic analysis of the long-term surface expression and De Martini P.M. D. Pantosti Pucci S., Civico R., e Litotamni nella delle litofacies e modello deposizionale dei Calcari a Briozoi (2005) - Atlante Civitelli G. and M. Brandano 214 pp. Laterza, Bari, Italy, Clementi A. and Piroddi E. (1986). L’Aquila, Antinoriana III: S Strutture sociali ed urbane della città nel Sei e Settecento, dell’Antinori. R. (1978) - L’Aquila Colapietra (1997) – Bartolomucci C. and Amedoro T. Centofanti M., – i Palazzi R., Colapietra L’Aquila: Ediarte, L’Aquila. Virtual J. Apennines: A regional review. (2010) - Geology of the Central and Scrocca D. Marsili P. Cipollari P., Cosentino D., geological field trips 2016 - 8(1.2) references 84 , 0 l. 9, na tà. the fault trale). taggio 1997, 27-64. etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins years, evidenced by new palaeoseismic results. Terra Nova. evidenced by new palaeoseismic results. Terra years, 187/3, 1119-1134, Int., J. fault linkage. Geophys. implications for active Mw 6.3 earthquake): http://dx.doi.org/10.1111/j.1365-246X.2011.05233.x. (Fucino fault system, Central Italy). Bollettino di Geofisica Teorica ed Applicata, 53 (4), 435-458. Italy). Bollettino di Geofisica Teorica (Fucino fault system, Central 1306. Doi: 10.1007/s10518-012-9409-0. Boll. Soc. Geol. It., 115. Boll. Soc. Geol. It., Fucino Plain (Central Italy). Journal of Geodynamics, 24, 87-103. Fucino Plain (Central Implications for active tectonics in Central Apennines. Tectonophysics, 308, 143-170. Apennines. Tectonophysics, tectonics in Central Implications for active 29, 3768–3789, http://dx.doi.org/10.1016/j.quascirev.2010.08.018. faults system. Quat. Sci. Rev., L’Aquila 2009 (Central Italy). Terra Nova, 22/1, 43–51, http://dx.doi.org/10.1111/j.1365-3121.2009.00915.x. Nova, Italy). Terra 2009 (Central M., Galli P. & Galadini F. (2009) - The Paganica Fault and surface coseismic ruptures caused by the 6 April 2009 earthquake Fault (2009) - The Paganica & Galadini F. Galli P. M., 80/6, 940–950. Lett., Italy). Seismol. Res. Central (L’Aquila, Vo Research, Journal of Geophysical Apennines, Italy. in the central in the seismic cycle timescales: insights into variability 115, B10418. doi:10.1029/2009JB006462. con il magmatismo Plio-Quaternario nell’area dei bacini neogenici e loro rapporti evoluzione Workshop del Fucino (Abruzzo). tosco-laziale. Pisa, 12-13 Giugno 1991, 90-92. 5 (1), 33-50. Il Quaternario, - Abruzzo). Majelama (Massiccio del Velino Sintesi delle ricerche geologiche multidisciplinari dell’ENEA sul “Lazio meridionale”. In Serie di Studi e Ricerche, monografia Ed. Dipartimento Ambiente, Claudio Carrara DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Galli P., Giaccio B., Messina P., Peronace E. & Zuppi G.M. (2011) - Palaeoseismology of the L’Aquila faults (Central Italy, 200 Italy, faults (Central of the L’Aquila E. & Zuppi G.M. (2011) - Palaeoseismology Peronace Messina P., Giaccio B., Galli P., (2012) - Early Pleistocene to late Holocene activity of the Magnola E. & Quadrio B. Peronace Giaccio B., Messina P., Galli P., Galli P. & Molin D. (2014) - Beyond the damage threshold: the historic earthquakes of Rome. Bull. Earthquake Eng., 12, 1277- Eng., Bull. Earthquake of Rome. the damage threshold: historic earthquakes (2014) - Beyond & Molin D. Galli P. Galadini F., Galli P. & Giraudi C. (1997a) - Geological investigations of Italian earthquakes: new paleoseismological data from of Italian earthquakes: C. (1997a) - Geological investigations & Giraudi Galli P. Galadini F., Galadini F., Galli P. & Giraudi C. (1997b) - Paleosismologia della Piana del Fucino (Italia Centrale), Il Quaternario, 10 (1), Il Quaternario, della Piana del Fucino (Italia Centrale), C. (1997b) - Paleosismologia & Giraudi Galli P. Galadini F., Galadini F. & Galli P. (1999) - The Holocene paleoearthquakes on the 1915 Avezzano earthquake faults (central Italy): faults (central earthquake on the 1915 Avezzano (1999) - The Holocene paleoearthquakes & Galli P. Galadini F. Galli P., Giaccio B. & Messina P. (2010) - The 2009 Central Italy earthquake seen through 0.5 Myr-long tectonic history of the seen through 0.5 Myr-long Italy earthquake (2010) - The 2009 Central & Messina P. Giaccio B. Galli P., Italy in 140 on a single fault in central E. (2016) - Three magnitude 7 earthquakes & Peronace Messina P. Giaccio B., Galli P., EMERGEO Working Group (2010) - Evidence for surface rupture associated with the Mw 6.3 L’Aquila earthquake sequence of April earthquake Group (2010) - Evidence for surface rupture associated with the Mw 6.3 L’Aquila EMERGEO Working Vol Sposato A., Scardia G., Naso G., Messina P., Giaccio B., Saroli M., Moro M., Fubelli G., E., Peronace Gori S., E., Falcucci Faure Walker, J.P., Roberts G.P., Sammonds P. & Cowie P.A. (2010) - Comparison of earthquakes strains over 102 and 104 year over strains (2010) - Comparison of earthquakes & Cowie P.A. Sammonds P. G.P., Roberts J.P., Walker, Faure 39Ar/40Ar di un sondaggio nella pia e datazione radiometrica Sadori L. & Villa I.M. (1991) - Palinologia Magri D., M., Follieri geologica tardopleistocenica ed olocenica del conoide complesso della Valle C. (1992) - Evoluzione M. & Giraudi Frezzotti di tettonica e paleosismici C. (1995) - I depositi del Pleistocene superiore e dell’Olocene; evidenze M. & Giraudi Frezzotti (1995) - Il terremoto del 1915 e la sismicità della piana Fucino (Italia Cen C. and Molin D. Giraudi Galli P., Galadini F., geological field trips 2016 - 8(1.2) references 85 r s 6. 9. patto Aquila l Salto - Fault 393-298. l Convegno educed from Berlusconi A. etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins antropico. Il Quaternario, 8 (1), 203-210. Il Quaternario, antropico. 126, 365-374. Apennines. Boll. Soc. Geol. It., examples from the central kinematic evaluations: 101 pp. de Geodynamique et Seismologie, Luxembourg, of the Seismological Society America, 101/3, 975–993. and basin depocentre migration over the last 2 Ma in the L’Aquila 2009 earthquake region, central Italian Apennines. Quat. region, central 2009 earthquake the last 2 Ma in L’Aquila over and basin depocentre migration 56, 69–88, http://dx.doi.org/10.1016/j.quascirev.2012.08.016. Sci. Rev., basin in the epicentral across the Middle Aterno & Giacomuzzi G. (2012) - High-resolution controlled-source seismic tomography Apennines, Italy). Italian Journal of Geosciences, 131/3, 373-388. (central earthquake area of the 2009, Mw 6.3, L’Aquila Progress on (Ed.), Recent Italy) seismic sequence (Mw 6.3): a preliminary seismotectonic picture. In: Guarnieri P. (Central 1-17. Publishers, ISBN 978-1-60876- 47-0, pp. Nova Geology. Earthquake an analysis of the Neogene to present deformations and related stress fields. Bull. Geol. Soc. America, 106, 9, 1107-1120. Bologna. Accessed 18 Mar 2015. di archeologia “Il Fucino e le aree limitrofe nell’antichità”. Avezzano 10-11 Novembre 1989, 45-53. 10-11 Novembre Avezzano di archeologia “Il Fucino e le aree limitrofe nell’antichità”. Eng. 9, 741-759. DOI 10.1007/s10518-011-9246-6. Bull. Earthquake for downtown L’Aquila. Apennines). Giornale di Geologia, 62, 57–77. (central di Varri and Val 0557-1405. Pàtron Editore, Bologna, Italy. n. 3, 8-22. ISSN Rivista Italiana di Geotecnica, Anno XLVII, city of L’Aquila. 22, 1027–1047. Geology, Journal of Structural Italy. central segment boundary, (Abruzzo, Central Italy): Geological evidence of large historical events. Journal of Geophysical Research, 101 No. B3, 5921-593 101 No. Research, Journal of Geophysical Italy): Geological evidence of large historical events. Central (Abruzzo, studie & Riccio G. (2011) - The contribution of seismic data in microzonation Régnier J. Pucillo S., Marcucci S., A., Fodarella nthal G. (Editor) (1998) - The European Macroseismic Scale EMS-98, Vol. 15, Conseil de l’Europe, Cahiers du Centre Europeén G. (Editor) (1998) - The European Macroseismic Scale EMS-98, Vol. nthal DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Gori S., Dramis F., Galadini F. and Messina P. (2007) - The use of geomorphological markers in the footwall of active faults fo of active in the footwall (2007) - The use of geomorphological markers and Messina P. Galadini F. F., Dramis Gori S., Gru sequence. Bulletin earthquake moment tensors of the 2009 L’Aquila Malagnini L. & Munafò I. (2011) - Regional Herrmann R.B., Pierdominici S., Civico R., Brunori C.A., M., Punzo F., Varriale D., De Rosa Castiello A., Bruno P.P., Villani F., Improta L., Giaccio B., Galli P., Messina P., Peronace E., Scardia G., Sottili G., Sposato A., Chiarini E., Jicha B. & Silvestri S. (2012) S. & Silvestri Jicha B. Chiarini E., Sposato A., Sottili G., Scardia G., E., Peronace Messina P., Galli P., Giaccio B., Giraudi C. (1988) - Evoluzione geologica della Piana del Fucino (Abruzzo) negli ultimi 30.000 anni. Il Quaternario 1(2), 131-15 geologica della Piana del Fucino (Abruzzo) C. (1988) - Evoluzione Giraudi G. (2010) - The April 2009 Pizzi A. & Pomposo F., Ferrarini Di Naccio D., De Nardis R., F., Brozzetti Boncio P., G., Lavecchia Italy d in east-central A. (1994) - seismotectonic zoning Joao V. Menichetti M. & Keller Barchi M., F., Brozzetti G., Lavecchia of the Italian Macroseismic Database. Milano, Camassi R. & Stucchi M. (eds) (2011) - DBMI11, the 2011 version Locati M., de Atti M. (1989) - Primi risultati delle analisi polliniche dei sedimenti lacustri della piana del Fucino. & Follieri Magri D. Giraudi C. (1995) - I detriti di versante ai margini della Piana del Fucino (Italia Centrale): significato paleoclimatico ed im ai margini della Piana del Fucino (Italia Centrale): C. (1995) - I detriti di versante Giraudi Messina P. (1996) - Tettonica mesopleistocenica dei terrazzi nord-orientali del Fucino (Italia centrale). Il Quaternario, 9(1), Il Quaternario, nord-orientali del Fucino (Italia centrale). mesopleistocenica dei terrazzi (1996) - Tettonica Messina P. de of the Messinian turbiditic complex in Valle stratigraphy analysis and physical (2000) - Facies & Moscatelli S. Milli S. by seismic dilatometer (SDMT) in the (2013) - Site characterization & Marchetti D. F. Totani Amoroso S., G., Totani Monaco P., of deformation within an en chelon normal fault kinematics and rates (2000) - The geometry, G.P. Morewood N.C. & Roberts Michetti A.M., Brunamonte F. Serva L. & Vittori E. (1996) - Trench investigations of the 1915 Fucino earthquake fault scarps of the 1915 Fucino earthquake investigations L. & Vittori E. (1996) - Trench Serva Brunamonte F. Michetti A.M., A.M., Duval Di Giulio G., G., Cultrera Cogliano R., F., Cara Bordoni P., E., Bertrand Bergamaschi F., R.M., Azzara Milana G., geological field trips 2016 - 8(1.2) references 86 y) ur 216. ence della nale e aternary ei, Roma. lithosphere etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Cl surface exposure dating: Evidence for strong earthquake over Holocene. Earth Planet. Sci. Lett., 225, 163-176. Holocene. Earth Planet. Sci. Lett., over Cl surface exposure dating: Evidence for strong earthquake 36 piana del Fucino (Italia Centrale). Rend. Fis. Acc. Lincei, S. 9, 5(2), 115-123. Fis. Acc. Lincei, S. Rend. piana del Fucino (Italia Centrale). 74, n. 2. S.B., Weten, Ned. Ak. Von subsequent dilatatation and collapse. Koninkl. from of the 2009 L’Aquila seismic event (Central Italy) causative fault, revealed by paleoseismological investigations. fault, revealed Italy) causative (Central seismic event of the 2009 L’Aquila 583, 131–144. http://dx.doi.org/10.1016/j.tecto.2012.10.036. Tectonophysics, 35, 177-202. Soc. Geol. It., (in Italian). and CD-Rom, 3 vol. Civile, L’Aquila, 6, 87-92. Quaternario, slab, in The Lithosphere in Italy. Advances in Earth Science Research, edited by A. Boriani et al., pp. 157–176, Acc. Naz. Linc pp. edited by A. Boriani et al., in Earth Science Research, Advances in The Lithosphere Italy. slab, l’arco appenninico meridionale nell’Abruzzo e nel Molise. Stud. Geol. Camerti, Spec. Vol. 1991/2, pp. 417–441, Camerino, Italy. 417–441, Camerino, 1991/2, pp. e nel Molise. Stud. Geol. Camerti, Spec. Vol. l’arco appenninico meridionale nell’Abruzzo & I.P. Vai Basin, edited by G.B. of an Orogen: The Apennines and Adjacent Mediterranean Southern Apennines. In Anatomy Academic Publishers, Dordrecht, Netherlands. 401–440, Kuwler Martini, pp. 139, 499-530. Int., J. from the Fucino region. Geophys. 1-5 settembre 1984. Braga, Association of Urbanists “Les Acteur de la mise en oeuvre l’urbanisme dans les villes Moyennes”, area (Abruzzi Apennines, Italy). Journal of Maps, 11-5, 689- earthquake 2009 L’Aquila Valley, geology of the Middle Aterno 1744-5647. Doi: 10.1080/17445647.2014.927128. 697, ISSN: 94-116. Bollettino Società Geologia Italiana, LXXV: including a large, previously unrecorded earthquake in the Middle Ages (860-1300 A.D.). J. Geoph. Res. 101, 5937-5960. Geoph. Res. J. in the Middle Ages (860-1300 A.D.). including a large, previously unrecorded earthquake 408 (1-4), 147-176. and GPS data. Tectonophysics, comparison between geological fault slip-rate DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Nijman W. (1971) - Tectonics of the Velino-Sirente Area, Abruzzi, Central Italy: modification of compressional structures by Area, Abruzzi, Central of the Velino-Sirente (1971) - Tectonics Nijman W. terremoto marsicano-fucense del 13 gennaio 1915. Boll. Soc. Sism. It. 19, 71- Oddone E. (1915) - Gli elementi fisici del grande Palumbo L., Benedetti L., Bourlès D., Cinque A. & Finkel R. (2004) - Slip history of the Magnola fault (Apennines, Central Ital R. (2004) - Slip history of the Magnola fault (Apennines, Central Cinque A. & Finkel Bourlès D., Benedetti L., L., Palumbo Mostardini F. & Merlini S. (1988) - Appennino centro-meridionale: Sezioni geologiche e proposta di modello strutturale. Mem. (1988) - Appennino centro-meridionale: Sezioni geologiche e proposta di modello strutturale. & Merlini S. Mostardini F. – Abruzzo sismica per la ricostruzione dell’area aquilana. Regione Group (2010) - Microzonazione Working MS–AQ Prot. Dip. Il etnea nell’area del Fucino (Italia Centrale). piroclastico di provenienza (1993) - Segnalazione di un livello Narcisi B. piroclastici nei sedimenti del Pleistocene superiore di due livelli e possibile provenienza (1994) - Caratteristiche Narcisi B. Moro M., Gori S., Falcucci E., Saroli M., Galadini F. & Salvi S. (2013) - Historical earthquakes and variable kinematic behavio and variable (2013) - Historical earthquakes & Salvi S. Galadini F. Saroli M., E., Falcucci Gori S., Moro M., Patacca E., Scandone P., Bellatalla M., Perilli N. & Santini U. (1991) - La zona di giunzione tra l’arco appenninico settentrio di giunzione tra (1991) - La zona N. & Santini U. Perilli Bellatalla M., Scandone P., E., Patacca Patacca E. & Scandone P. (2001) - Late thrust propagation and sedimentary response in the thrust belt-foredeep system of the (2001) - Late thrust propagation and sedimentary response in the belt-foredeep E. & Scandone P. Patacca Apennines (Italy): evid oblique extension in the central & Boccaletti M. (1999) - Active P. Tapponier Gaudemer Y., Piccardi L., (1984) – & Tironi F. Properzi P. Mattogno C., Piroddi E., una piccola città media. Proceedings of the International L’Aquila: E. & Gueli A. (2015) - Qu Pons-Branchu De Martini P.M., Smedile A., Del Carlo P., D., Pantosti Civico R., Villani F., Pucci S., del Fucino. dei Marsi, Territorio presso Venere Superiore nella Grotta Clemente Tronci A.M. (1956) - Il Paleolitico Radmilli Pantosti D., D’Addezio G. & F. Cinti (1996) - Paleoseismicity of the Ovindoli-Pezza fault, central Apennines, Italy: a history fault, central of the Ovindoli-Pezza Cinti (1996) - Paleoseismicity G. & F. D’Addezio D., Pantosti Papanikolaou I., Roberts G. & Michetti A.M. (2005) - Fault scarps and deformation rates in Lazio–Abruzzo, Central Italy: Central in Lazio–Abruzzo, scarps and deformation rates G. & Michetti A.M. (2005) - Fault Roberts I., Papanikolaou sinking of a relic mountain building in the Apennines. The role of passive (1989) - Post-Tortonian E. & Scandone P. Patacca geological field trips 2016 - 8(1.2) references 87 - o cr. 11) - Eng. le del etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Conference Gruppo Nazionale di Geofisica della Terra Solida (GNGTS), Trieste 14-17 novembre Trieste Solida (GNGTS), Conference Gruppo Nazionale di Geofisica della Terra th bacino del Fucino (Italia Centrale). Il Quaternario, Italian Journal of Quaternary Sciences, 21(1B), 2008 - 383-394. Il Quaternario, bacino del Fucino (Italia Centrale). of methodology and histories on limestone normal fault scarps: a reappraisal past earthquake 36 cosmonuclide to recover 182, 36-72. Doi:10.1111/j.1365246X.2010.04622.x. Int., J. interpretations. Geophys. 307, 487-500, doi:10.1016/j.epsl.2011.05.022. inferred from 36Cl exposure dating. Earth Planet. Sci. Lett., Italy, in Central 89 (B7), 5681–5698, http://dx.doi.org/10.1029/JB089iB07p05681. Res., Geophys. J. Zones. Andreas Fault 15-46. Carta Geol. It., tettonica recente di alcune strutture. Mem. Soc. Geol. It. 35, 893-907. interpretazione della evoluzione Geologica e Geodinamica Proceedings of the Conference “Evoluzione a geological time interval. over earthquakes Spec. n°1 (2001), 939-946. Vol. Boll. Soc. Geol. It., Pialli”. in memoria del Prof. dell’Appennino Sismica a riflessione ad alta risoluzione per il modello del sottosuolo e la stima della pericolosità sismica centro storic Proceedings of 30 dell’Aquila. Geol., Special Publication No. 6 “Perspectives in Paleoseismology”, 101-113. in Paleoseismology”, 6 “Perspectives Special Publication No. Geol., Italy). Journal of Maps. Doi: 10.1080/17445647.2013.867545. Central (Abruzzo, valley River middle Aterno Dinam. et Geogr. Phys., 23(1), 55-72. Phys., Dinam. et Geogr. 26, 339-376. Geology, Journal of Structural Italy. central example from Lazio-Abruzzo, DOI: 10.6092/INGV.IT-CPTI11 Bologna, http://emidius.mi.ingv.it/CPTI. Italiani. Milano, Terremoti 2011 (In Italian). DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Schlagenhauf A., Gaudemer Y., Manighetti I., Palumbo L., Schimmelpfennig I., Finkel R. & Pou K. (2010) - Using in situ Chlorine R. & Pou Finkel Schimmelpfennig I., L., Palumbo Manighetti I., Gaudemer Y., Schlagenhauf A., supercycles K. (2011) - Earthquake and Pou J. Malavieille R., Finkel Gaudemer Y., Benedetti L., Manighetti I., Schlagenhauf A., and San examples from the wasatch earthquakes: and characteristic behavior (1984) - Fault & Coppersmith K.J. D.P. Schwartz Mem. Des for an interpretation of the italian geodynamics: a review. (2003) - Contraints Doglioni C. & Innocenti F. Scrocca D., di Blumetti A.M. & Michetti (1988) - Gli effetti sul terreno del terremoto Fucino (13/1/1915); tentativo L., Serva Guerrieri L. & Michetti A.M. (2002) - The Apennine intermountain basins: the result of repeated strong Blumetti A.M., L., Serva N. (20 G. & Pelosi Cavuoto D., Tarallo G. (1981) –Stokel Del Monaco F., il 1860 e 1960. Edizioni del Gallo Cedrone, L’Aquila. F., Il centro storico tra Varriale La città dell’Aquila. M., Punzo Castiello A., Bruno P.P., Di Fiore V., M., Tallini Santo A., Ascione A., Di Crescenzo G., Miccadei E., Piacentini T. & Valente E. (2013) - Tectonic-geomorphological map of the E. (2013) - Tectonic-geomorphological & Valente Piacentini T. Miccadei E., G., Di Crescenzo Ascione A., Santo A., dati paleosismologici dal settore orienta (2008) - Nuovi & Galli P. Galadini F. D., Dell’Acqua Borghesi H., Moro M., Saroli M., Radmilli A.M. (1981) - Storia dell’Abruzzo dalle Origini all’età del Bronzo. Ed. Giardini, Pisa, 451pp. dalle Origini all’età del Bronzo. A.M. (1981) - Storia dell’Abruzzo Radmilli 1, 3-18. Mediterranee, (Italie central). (1970) - Étude géomorphologique sur le Bassin d’Avezzano J. Raffy étude géomorphologique. Thèse inédite, 705 pp. central: tyrrhénien de l’Apennin (1979) - Le versant J. Raffy Geol. Rev. (Italie central). tyrrhénien des Abruzzes (1981-82) - Orogenése et dislocations quaternaires du versant J. Raffy 8, 105–139. (1986) - The Oligocene to recent foreland basins of the Northern Apennines. IAS Spec. Publ., Ricci Lucchi F. an normal fault Systems: along active in growth rates variations & Michetti A.M. (2004) - Spatial and temporal G. P. Roberts dei 2011 del Catalogo Parametrico di) (2011). CPTI11, la versione & Stucchi M. (a cura Gasperini P. Camassi R., A., Rovida Bull. Ass. Abruzzi, Italy, in Central fault zone active & Nardi A. (1995) - The Ovindoli fault: a segment of longer, Salvi S. geological field trips 2016 - 8(1.2) references 88 il 6 6 he es) G.P., iutta I., etti-F. Potenza-S. Pucci-G. Roberts-L. Serva-A. Smedile-L. Smeraglia-A. Tertulliani-G. Tironi-F. Villani-E. Vittori Tironi-F. Tertulliani-G. Smedile-L. Smeraglia-A. Serva-A. Pucci-G. Roberts-L. Potenza-S. etti-F. Quaternary geology and paleoseismology in the Fucino L’Aquila basins Earthquake. Bulletin of the Seismological Society of America, 102/4, 1543–1553, Bulletin of the Seismological Society Earthquake. Mw 6.3 L’Aquila earthquake in Central Italy. Bull. Seismol. Soc. Am., 101/4, 1507–1530. Bull. Seismol. Soc. Am., Italy. in Central earthquake Mw 6.3 L’Aquila following the 6 April 2009 L’Aquila earthquake (Mw 6.3). Ital. J. Geosci., 131/ 3, 309–329, Geosci., (Mw 6.3). Ital. J. earthquake following the 6 April 2009 L’Aquila http://dx.doi.org/10.3301/IJG.2012.03. (2011) - Surface faulting of the & Cowie P.A. Phillips R.J. Mccaffrey K.J.W., Wilkinson M., Sileo G., Livio F., Berlusconi A., April 2009 http://dx.doi.org/10.1785/0120100140. 84, 974–1002. area and surface displacement, Bull. Seismol. Soc. Am., http://dx.doi.org/10.1785/0120110205. April 2009 Rossi A. & Vecchi M. (2011). An application of EMS98 in a medium-sized city: The case of L’Aquila (Central Italy) after the Apr (Central city: The case of L’Aquila M. (2011). An application of EMS98 in a medium-sized A. & Vecchi Rossi Bull. Earthq. Eng. 9,6, 2009 Mw 6.3 earthquake. 67–80. Doi10.1007/s10518-010-9188-4. on Performance- In: M. Maugeri and C. Soccodato (eds), Proc. 2nd Int. Conf. Southern part of the historic centre L’Aquila. 2.13, 315-328. Pàtron Editore, Bologna (CD- No. Paper Italy, Geotechnical Engineering, Taormina, Based Design in Earthquake ROM). 2011. Earth Surface, 116, F01022, 14 PP., Journal Geoph. Res., glacial bedrock scarps on normal fault footwalls. Doi:10.1029/2010JF001861 DOI: 10.3301/GFT.2016.02 S. Amoroso-F. Bernardini-A.M. Blumetti-R. Civico-C. Doglioni-F. Galadini-P. Galli-L. Graziani-L. Guerrieri-P. Messina-A.M. Mich Messina-A.M. Guerrieri-P. Galli-L. Graziani-L. Galadini-P. Blumetti-R. Civico-C. Doglioni-F. Bernardini-A.M. Amoroso-F. S. Vittori E., Di Manna P., Blumetti A.M., Comerci V., Guerrieri L., Esposito E., Michetti A.M., Porfido S., Piccardi L., Roberts Roberts Piccardi L., S., Porfido Michetti A.M., Esposito E., Guerrieri L., Comerci V., Blumetti A.M., Di Manna P., Vittori E., Bull. Geol. Soc. Am. 88 (1977) 1267–1281. Nevada, fault scarps, north-central R.E. (1978) - Profiles and ages of young Wallace (1994) - New empirical relationships among magnitude, rupture length, width, & Coppersmith K.J. D.L. Wells Tertulliani A., Arcoraci L., Berardi M., Bernardini F., Camassi R., Castellano C., Del Mese S., Ercolani E., Graziani L., Lesch L., Graziani Ercolani E., Del Mese S., Castellano C., Camassi R., Bernardini F., M., Berardi L., Arcoraci A., Tertulliani Tertulliani A., Leschiutta I., Bordoni P. & Milana G. (2012) - Damage Distribution in L’Aquila City (Central Italy) during the City (Central & Milana G. (2012) - Damage Distribution in L’Aquila Bordoni P. Leschiutta I., A., Tertulliani Totani G., Totani F., Monaco P., Tallini M., Del Monaco F. & Zia G. (2012) - Site investigations and geotechnical problems in t & Zia G. (2012) - Site investigations Del Monaco F. M., Tallini Monaco P., F., Totani G., Totani & Phillips R. (2011) - Geomorphic significance of post- Lancaster S.T. G.P., Roberts A.C., Whittaker S.W., McCoy G.E., Tucker Apennin G. (2012) - A fresh look at the seismotectonics of Abruzzi (Central & Valensise U. Fracassi P., Burrato P., Vannoli