Geological Field Trips

Società Geologica Italiana

2009 Vol. 1 (1) 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

The Laga basin: Stratigraphic and Structural Setting 70th EAGE Conference & Exhibition - Rome 2008

DOI: 10.3301/GFT.2009.01 geological field trips 2009 - 1(1)

2 publishing group ons and sse e delle .it 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome (3) [email protected] [email protected] [email protected] salv The Laga basin: Stratigraphic and Structural Setting massimiliano , Salvatore Milli (2) Editorial Board M. Balini, G. Barrocu, C. Bartolini, D. Bernoulli, F. Calamita, B. Capaccioni, W. Cavazza, F.L. Chiocci, R. Compagnoni, D. Cosentino, S. Critelli, G.V. Dal Piaz, C. D'Ambrogi, P. Di Stefano, Doglioni, E. Erba, R. Fantoni, P. Gianolla, L. Guerrieri, M. Mellini, S. Milli, M. Pantaloni, V. Pascucci, L. Passeri, A. Peccerillo, L. Pomar, P. Ronchi (Eni), B.C. Schreiber, Simone, I. Spalla, L.H. Tanner, C. Venturini, G. Zuffa. ISSN: 2038-4947 [online] ISSN: No.1 (2009), pp. 50, 27 figs. (DOI 10.3301/GFT.2009.01) (2009), pp. No.1 , Massimiliano Moscatelli 1 (1) EAGE Conference & Exhibition - Rome 2008 th 70 (ISPRA-Roma) Geol.F.Trips, Vol. Geol.F.Trips, Sabina Bigi The Laga basin: Stratigraphic and Structural Setting and Structural The Laga basin: Stratigraphic (SGI-Roma) (ISPRA-Roma) Periodico semestrale del Servizio Geologico d'Italia - ISPRA e della Società Geologica Italiana semestrale Periodico (SGI-Perugia) (ISPRA-Roma) (ISPRA-Roma) Dipartimento di Scienze della Terra, SAPIENZA Università di Roma, Roma, Italy. Italy. Roma, di Roma, Università SAPIENZA della Terra, Dipartimento di Scienze Dipartimento di Scienze della Terra, SAPIENZA Università di Roma, Roma, Italy. Italy. Roma, di Roma, Università SAPIENZA della Terra, Dipartimento di Scienze Geological Field Trips (1) http://www.isprambiente.it/site/it-IT/Pubblicazioni/Periodici_tecnici/Geological_Field_Trips CNR - IGAG, Istituto di Geologia Ambientale e Geoingegneria, Roma, Italy. Italy. CNR - IGAG, Istituto di Geologia Ambientale e Geoingegneria, Roma, (3) - (2) GFT contents of the guides published; Authors each paper are responsible for ideas, opinions and published. Il Servizio Geologico d’Italia, la Società Geologica Italiana e il Gruppo editoriale non sono responsabili delle opinioni espre affermazioni pubblicate nella guida; l’Autore/i è/sono il/i solo/i responsabile/i. Responsible Director Responsible Leonello Serva Editor in Chief Gloria Ciarapica Editorial Responsible Maria Letizia Pampaloni Editorial Manager Mauro Roma Responsible Convention Anna Rosa Scalise Alessandro Zuccari The Geological Survey of Italy, the Società Geologica Italiana and Editorial group are not responsible for ideas, opini geological field trips 2009 - 1(1)

3 index ...... 28 ...... 25 ...... 35 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome Basin plain deposits of the Laga 1 and - The Laga basin: Stratigraphic and Structural Setting The upper Messinian-lower Pliocene piggy The boundaries of the Laga basin - - References...... 43 Second day Laga 2 units near the frontal and lateral slope of basin. The Montagna dei Fiori-Montagnone fault-related fold Third day back deposits of Monte Coppe and Rigopiano conglomerates. The Campo Imperatore Quaternary basin Itinerary First day 20 24 ...... 9 ...... 13 ...... 19 ...... 5 ...... 9 ...... 7 ...... 8 Geological and stratigraphic setting of the Laga basin and surrounding regions data ...... 14 and structural Stratigraphic The Laga Depositional Sequence Architectural elements and depositional setting ...... Interaction with the confining slopes ...... INDEX Informations Safety ...... 4 Hospital...... 4 Accommodation ...... 4 Program Summary ...... 5 First day ...... 5 Second day ...... 6 Third day Riassunto Abstract Excursion notes Introduction Geological setting of the central Apennines geological field trips 2009 - 1(1)

4 informations . d nce is a c.). 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting - number: +39 0861 95105 Telephone - number: + 39 0861 598416 Telephone : Hotel “Vomano” Viale Risorgimento 2/16, Montorio al Vomano, 64046 Teramo. Tel. 0861 598498; Tel. 64046 Teramo. Viale Risorgimento 2/16, Montorio al Vomano, : Hotel “Vomano” - Presidio Ospedaliero “G. Mazzini” The emergency telephone number for ambulance is 118. The emergency telephone numbers for police is 112 and 113. - personal responsibility and all participants should be aware of the following issues. personal responsibility and all participants should be aware low altitude (less than 1000 meters). Most of the outcrops are along road and we place at relatively takes - The excursion long walks. will not make sinuous roads. along very are goods although to reach outcrops will be necessary drive - Roads or running shoes are unsuitable footwear in the field. boots. Trainers - All participants require comfortable walking are possible stable although changes with rain the weather is relatively is essential. In September, coat/jacket - A waterproof be useful. may over-trousers Waterproof (an a spare T-shirt waterproofs, - A small rucksack is needed for daily use. This needs to be at least big enough carry your and small snacks. a fleece/sweater), bottle of water maybe are useful. - Sun protection can be useful; hats or headscarves affect performa or mental condition, which may physical leaders (in confidence) of any should inform the excursion Participants lung disease, allergies et heart condition, back problem, ear disorder, vertigo, in the field (e.g. asthma, diabetes, epilepsy, etc.). on request (vegetarian, - Special diets are available will carry one basic first aid kit. - Each vehicle is good although in some places it can be absent. - Mobile/cellular phone coverage - Safety of potential difficulties, fitness and use appropriate equipment. Safety Safety in the field is closely related to awareness Hospitals - Teramo number: + 39 0861 4291 Telephone Address: Piazza Italia, 1 64100 Teramo. First-aid station: - Montorio al Vomano - Pietracamela, Fano Adriano, Crognaleto Accommodation - Montorio al Vomano 0861 592736 Fax geological field trips 2009 - 1(1)

5 informations 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Program Summary First day to Laga basin passing will move Participants through Lazio and Abruzzi (2 - 3 hours). time, participants will be Depending on the arrival terminations of the Laga introduced in the lateral to the hotel in basin, directly on the field. Arrive After a brief rest, before dinner, the evening. participants will be introduced to the geology of and in particular to the Italy, the Central and stratigraphic, depositional, paleogeographic, setting of the Laga basin. structural Dinner and night at Montorio al Vomano: Hotel “Vomano” Viale Risorgimento 2/16, Montorio al Vomano, 64046 Teramo. Tel. + 39 0861 598498; Fax 592736. Second day to the analysis of will be devoted The second day the Laga 1 and 2 lobe deposits: depositional architecture of the lobes, their geometries and facies will be discussed. During the afternoon two stops will be dedicated to the Montagna dei Fiori structure, a regional fold, in order to scale recumbent fault-related style of the the typical stuctural illustrate belt structures. Apennines fold-and-thrust Dinner and night at Montorio al Vomano: Hotel “Vomano” Viale Risorgimento 2/16, Montorio al Vomano, 64046 Teramo. Tel. + 39 0861 598498; Fax 592736. geological field trips 2009 - 1(1)

6 informations 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Third day to piggy-back will be devoted The third day deposits of the Monte Coppe (upper Messinian) (lower Pliocene) and and Rigopiano conglomerates to their significance in the tectono-stratigraphic will have of the Laga basin. Participants evolution Sasso view of the Gran also a panoramic normal faults structures and Campo Imperatore between system, and of the interaction conpressional structures and the youger by 1 P.M. to Rome extensional tectonic. Return geological field trips 2009 - 1(1)

7 informations EAGE Conference & th 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting EAGE 2008, guida all'escursione, bacino della Laga, Gran Sasso, Appennino centrale Exhibition, tenutasi Roma nel 2008. L'escursione sul terreno, della durata di tre giorni, ha avuto per oggetto di tre giorni, ha avuto della durata sul terreno, nel 2008. L'escursione Exhibition, tenutasi Roma il Bacino della Laga, uno dei più importanti e meglio conosciuti bacini sin-orogenici messiniani dell'Appennino. la porzione interna della catena a pieghe e faglie, tra l'elemento di cerniera infatti, rappresenta bacino, Tale quella esterna, più a est, sepolta sotto una spessa coltre di depositi clastici sin-orogenici del Plio-Pleistocene. e in particolare l'assetto Il primo giorno di escursione è dedicato a introdurre la geologia dell'Italia centrale, l'as- stratigrafica, del bacino della Laga. L'architettura deposizionale e paleogeografico stratigrafico-strutturale, il secondo giorno di setto deposizionale e le facies dei depositi torbiditici della Laga sono analizzati durante e discusso l'as- Lo stesso giorno è osservato chiave. di alcuni affioramenti l'osservazione escursione, attraverso setto geometrico dei depositi della Laga rispetto alle anticlinali in deformazione, alla monoclinale regionale e che attra- infine, l'escursione si conclude con un transetto giorno, Il terzo Sasso. del Gran al sovrascorrimento includendo: 1) i depositi pliocenici che seguono la deformazione principale Sasso, del Gran la struttura versa e le più recen- le strutture compressive che intercorrono tra di questo thrust regionale; 2) l'analisi dei rapporti ti faglie estensionali. chiave: Parole Riassunto viene presentata la guida geologica all'escursione n.2 della 70 In questo lavoro geological field trips 2009 - 1(1)

8 informations 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting EAGE Conference & Exhibition, that was held in EAGE Conference & Exhibition, that was th EAGE 2008, excursion guidebook, Laga basin, Gran Sasso, central Apennines Abstract present here the guidebook of field trip n.2 70 We Rome in 2008. The focus of the 3-days field trip is upon the structural and stratigraphic setting of the Messinian and stratigraphic field trip is upon the structural in 2008. The focus of the 3-days Rome Laga basin, one of the most studied syn-orogenic basins Apennines. Due to period its geological of the Apennines in it represents a link between the internal, Lower Miocene fold-and-thrust-belt evolution, the west and external more recent part of chain buried below a thick pile syn-orogenic, Plio- Pleistocene clastic deposits, in the east. and in particular to the depositional, Italy, to introduce the geology of central is devoted The first day the setting of the Laga basin. During second day, and structural stratigraphic, paleogeographic, outcrops, where is through some key architecture of the Laga turbidite deposits is analyzed stratigraphic The possible to see the main sedimentological features of different depositional environments. geometric setting of the Laga deposits with respect to growing anticlines, regional monocline and a tour following attendees is given the third day southward, Sasso thrust is also shown. Moving the Gran the main Sasso thrust, which includes: i) the Pliocene deposits that post-dated section across the Gran structure and the younger deformation of this regional thrust; ii) the relationships between contractional extensional normal faults. Keywords: geological field trips 2009 - 1(1)

9 excursion notes 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Introduction thrust Most of the ancient turbidite systems are known being deposited in foredeep basins at front active located in the more internal portion of these basins, belt. Differently from fluvio-deltaic systems generally turbidite systems occur at different depth in the more deeper portions of these basins (foredeep shallower tectonically confined depressions occurring on top of the thrust belt systems) or in the relatively turbidite systems (wedge-top turbidite systems) (see discussion in Mutti et al. 2002, 2003). Foredeep and represent the classical sedimentation in a broad and flat basin plain, showing thick to thin parallel turbidite systems are continuous sandstone beds with the Bouma-type depositional division. Wedge-top directly fed by fluvio-deltaic systems and more clearly record both climate changes affecting the source areas and tectonic activity of the orogenic wedge. indicating characters Apennines show many Messinian turbidite deposits of the northern and central in relation to the segmentation of sedimentation in confined basins, formed since the upper Tortonian Ricci foredeep basin (inner stage of the Marnoso-Arenacea, Marnoso-Arenacea Langhian-lower Tortonian analyses as a well structural stratigraphic detailed facies and physical Lucchi, 1986). In these last years, Apennines), demonstrate fms. (central and thermal analyses, conducted on the Laga Argilloso-Arenacea of the Messinian as these basins were located at the hinge between foredeep and wedge-top depozones 2004; 2003; Moscatelli, Milli et al., Apennine thrust belt (Milli and Moscatelli, 2000, 2001; Bigi et al., 2007; 2006; Critelli et al., 2006; Casero and Bigi, Aldega et al., 2006; Stanzione et al., et al., Falcini deeply controlled the onset 2007). Anisotropy of the subducted plate and thrust propagation rate Milli et al., 2006). The resulting of complex basins at the top orogenic wedge (Casero and Bigi 2006; et al., a strong control on turbidite of these basins and the concomitant climate changes exerted topography organization of these deposits. sedimentation and on the stratigraphic Geological setting of the central Apennines since the upper fold and thrust belt, developed Apennines are part of an eastward-migrating The central 1986; and Ryan, subduction of the Adria plate (Malinverno westward Oligocene, in relation to the passive 1990; Doglioni, 1991; Argnani and Ricci Lucchi, 1990; Boccaletti et al., et al., Ricci Lucchi, 1986; Patacca geological field trips 2009 - 1(1) excursion notes 10 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting eastern part of central Fig. 1 - Structural map of Apennines and Tyrrhenian Sea. map of Apennines and Tyrrhenian Fig. 1 - Structural shown in fig. 3. Modified after Patacca et al. (1993). shown in fig. 3. Modified after Patacca Legend: 1) base of Pliocene/Quaternary isobaths (in kilometres); 2) front of thrust belt; 3) major post-Tortonian faults; 6) antiforms; 7) thrusts; 4) normal faults; 5) strike-slip bodies. OR line: Ortona- 9) intrusive synforms; 8) volcanoes; Apennines area line. Square indicates central Roccamonfina 2001) (Fig. 1).more The successions Meso-Cenozoic Apennines involves southern deposited on the Jurassic-Cretaceous Ocean (Kligfield, margin of the Tethys passive by the characterised 1979). This paleomargin was starting from the Middle Liassic, of development, domains: and paleogeographic two main structural the Sabina-Umbria-Marche pelagic domain to carbonate and North, the Lazio-Abruzzi West platform to the East and South (see Centamore et 1971; Cooper and Burbi, 1986; Accordi al., Carboni, 1988 and references therein), which were main normal fault named by a Jurassic separated 1978, 1982). line" (Castellarin et al., "Ancona-Anzio the Sabina-Umbria-Marche the present day, At pelagic domain is tectonically placed onto the Lazio- Abruzzi carbonate platform along the Olevano- and Praturlon, Antrodoco line (Fig. 2) (Parotto et al., 1975; Salvini and Vittori, 1982; Cavinato 1991; 1987; Bigi et al., 1986; Calamita et al., 1995) that 1991; Corrado, Cipollari and Cosentino, of the Sibillini Thrust. ramp is considered the lateral geological field trips 2009 - 1(1) excursion notes 11 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 2 - Schematic stratigraphic column (left) for the Umbria–Marche basin succession, and (right) stratigraphic Fig. 2 - Schematic stratigraphic (from Mazzoli et al., 2005). et al., (from Mazzoli relationships between Latium–Abruzzi carbonate platform and slope-to-basin Sabina (Gran Sasso) transitional successions Sasso) transitional carbonate platform and slope-to-basin Sabina (Gran relationships between Latium–Abruzzi The Sabina-Umbria-Marche pelagic succession is about 3000 m thick and is represented by a multilayer of The Sabina-Umbria-Marche pelagic succession is about 3000 m thick and represented by a multilayer carbonate platform is made up of about 5000 pelagic limestones, marls, and siliceous rocks. The Lazio-Abruzzi to the upper on a subsiding platform from the upper Triassic carbonates, developed m of shallow water (Fig. 2) respectively Miocene, with evidences of sinking and emersion during the Cretaceous Paleocene 1988). (Accordi et al., of the Apennine chain migration During the Neogene accretionary process (Oligocene to Present), eastward 1997; Argnani and Ricci Lucchi, 1990; Gueguen et al., et al., 1990; Patacca (Ricci Lucchi, 1986; Boccaletti et al., 2001) genereted a complex foreland basin system, essentially filled by thick successions of siliciclastic turbidites (Langhian- (Burdigalian-Langhian), and Marnosa-arenacea of the Macigno (Chattian-Burdigalian), Cervarola crop out along the Marche Plain and, southward, lower Messinian) fms. Plio-Pleistocene deposits filled the Po coastal sector. and Abruzzo geological field trips 2009 - 1(1) excursion notes 12 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome Fig. 3 - Geological sketch of the central Fig. 3 - Geological sketch Apennines. Starting from the Late Tortonian 1978) (Centamore et al., tectonic event of the characters the physiographic Apennine foreland basin system changed as well the main features of the turbidite systems. In Lazio- Abruzzi carbonate platform, small, elongated and confined turbidite basins 1984; Milli and (Bellotti et al., 2003) Moscatelli, 2000; Bigi et al., bordered by pre-thrusting normal faults were formed (Fig. 3). These faults dissected the foreland during time (Compagnoni Tortonian-Messinian 1998, 1991; Calamita et al., et al., 2001, 2002; Bigi 2002; Scisciani et al., & Costa Pisani 2002, 2005; Tavernelli 1998), and are exumated at et al., present, along the margins of turbidite basins. These elements of evolution controlled the structural the chain, as well nature and architecture of the stratigraphic turbidite depositional systems (e.g., Milli & Moscatelli, 2000; Moscatelli 2003; Bigi et al, 2003, 2004, 2009; 2004; 2007, 2009). Milli et al., The Laga basin: Stratigraphic and Structural Setting geological field trips 2009 - 1(1) excursion notes 13 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 4 - Geological map of Laga basin. Centamore et al. (1991). Black square indicates the field trip area. of correlation panels Black lines are traces of figs. 7 and 8; dashed line indicates the of the geological cross-section fig. trace 6. White numbers indicate measured sections of figs. 7 and 8. T1: stratigraphic thrust of fig. 6. Modified after Teramo Geological and stratigraphic setting of the Laga basin and surrounding regions Laga basin has a The present-day triangular shape (Fig. 4) due to its inherited physiography. distinguish a northern sector of We the basin (Northern Laga basin, NLB), from the southern one (Southern Laga basin, SLB), being this latter more subsiding and wide compared to the first one. the Laga basin is Southward Sasso thrust, bounded by the Gran is constituted by whose hanging wall carbonate platform Triassic-Miocene 1980, deposits (Cantalamessa et al., the Laga 1983, 1986). Westwards basin is bounded by the Sibillini is made up of thrust; its hanging wall geological field trips 2009 - 1(1) excursion notes 14 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting pelagic Meso-Cenozoic carbonates (Centamore et al., 1991; Calamita et al., 1994; Artoni & Casero, 1997; Bigi 1994; Artoni & Casero, 1991; Calamita et al., carbonates (Centamore et al., pelagic Meso-Cenozoic the back limb of Montagna dei Fiori-Montagnone anticline constitutes foreland 1999). Eastward, et al., where part of the Laga Messinian turbidite deposits onlap (Fig. 4). ramp when regional tectonic phase delineated the Laga turbidite basin from upper Tortonian, The infra-Messinian the passage to marked this sector from the Marnoso Arenacea basin. This event thrust activity separated 2002, 2003; et al., upper Messinian to Present foreland basin system (Ricci Lucchi, 1986; Roveri successive 2009). The Laga turbidite succession 2007, 2009; Bigi et al., 2006; Milli et al., 2005; Bigi et al., Manzi et al., of the closing phase phase being the lower Messinian portion representative recorded this transitional of the onset Marnoso Arenacea foreland basin system and the upper Messinian portion representative foreland basin system. present-day Stratigraphic and structural data area to by numerous authors in the past, because it represents a key The Laga basin has been investigated of the deformational phases of the Neogene-Quaternary evolution understand and reconstruct the youger 1991; Artoni et al., 1991; Patacca 1991; Ghisetti & Vezzani, belt (Centamore et al., Apennine fold-and-thrust 2005; Artoni, 2003, 2007; Moscatelli, et al., 2002; Tozer et al., 1998; Mazzoli et al., 1997; Tavarnelli & Casero, 2004; Scisciani & Montefalcone, 2005). More recently new data from seismic lines 2003; Moscatelli et al., interpretation and balanced geological cross-sections, thermal history analyses, facies physical of this portion the Apennine analyses allowed to better define the time-space evolution stratigraphic 2006, 2009; 2004; Casero & Bigi, 2006; Bigi et al., foreland basin system (Moscatelli, 2003; Moscatelli et al., 2007, 2009). 2007; Milli et al., 2006; Aldega et al., Stanzione et al., subdivision of the Messinian Laga fm. has been proposed since 80's (Cantalamessa et al., Stratigraphic Tortonian-lower 1991, 1992, 1993). This unit lies above 1980, 1981-82, 1982, 1986; Centamore et al., Messinian pelagic and hemipelagic deposits (marne a Pteropodi marne Orbulina fms.) was analysis conducted by Facies and post-evaporitic. evaporitic subdivided into three members: pre-evaporitic, 1981) allowed interpreting the Laga fm. as 1978; Mutti & Sonnino, the previous authors (see also Mutti et al., a classical deep-sea fan turbidite succession (Mutti & Ricci Lucchi, 1972). 1991) authors (Chiocchini & Cipriani 1989, 1991, 1992; Civitelli al., several From a compositional point of view, by igneous being the sediments derived indicate for the turbidite deposits of Laga fm. a western provenance, geological field trips 2009 - 1(1) excursion notes 15 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 5 - Main stratigraphic units recognized in the units recognized Fig. 5 - Main stratigraphic Laga basin (Modified from Milli et al., 2007). Laga basin (Modified from Milli et al., Messinian Laga basin. Pre-ev = pre-evaporitic unit; Messinian Laga basin. Pre-ev = pre-evaporitic p- stage; res-ev = resedimented evaporites; ev = evaporitic units. U1, U2, U3, U4, and ev1 and p-ev2 = post-evaporitic I1, I2, I3 are unconformity surfaces. The dotted line ash layer indicates the position and age of a volcanic in the level constituting an important chronostratigraphic and metamorphic rocks of Alpine origin. Morelli three (1994) and Corda Morelli (1996) recognized main petrofacies in the Laga fm. that, from evidence an increase of chert and bottom to the top, More in detail, the lower carbonate lithic fragments. from turbidite flows unit derived petrostratigraphic along coming from the northern sectors, and moving the axis of basin. The upper petrostratigraphic had the main source from unit, instead, would have smaller catchment area with transversal relatively located on the Apennine orogenic belt. collector, scheme of The recent Messinian chronostratigraphic by a the Apennine foreland basin system, derived data and methodologies, of several close integration allowed the identification of allounits bounded by been correlated to unconformity surfaces that have 1994; (Bassetti et al., the main Messinian events 1998, 2001; Krijgsman et et al., 1997; Roveri Vai, 2002; 1999; Bassetti, 2000; Ricci Lucchi et al., al., 2002; Artoni, 2003; Moscatelli, et al., Rossi 2005; Roveri 2004; Manzi et al., Moscatelli et al., 2007, 2009). Although and Manzi, 2006; Milli et al., and Marche area, these in Romagna recognized units has been also individuate in the Southern Laga 2007, basin (SLB) (Artoni, 2003, 2007; Milli et al., 2009) (Fig. 5). based on the analysis of 45 measured stratigraphic- on the SLB, The study conducted in the last years and re- 7000 m) and on the integration sedimentological sections (total thickness of approximately geological field trips 2009 - 1(1) excursion notes 16 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting interpretation of numerous literature data (see Cantalamessa et al., 1980; Centamore et al., 1991; 1992, 1980; Centamore et al., data (see Cantalamessa et al., interpretation of numerous literature 2003) substantially confirmed the stratigraphic 2000; Albouy et al., 1993; Morelli, 1994; Bigazzi et al., units. It schemes proposed by Artoni (2003) and Moscatelli et al. (2004) as far the main recognized interpretation and for differentiates from the previous schemes instead for new sequence stratigraphic between climatic and the detail on internal organization of units, which reflects a close interaction tectonic processes (Stanzione, 2007; Milli et al. 2007, 2009). Based on these new data, Laga 1, 2, and in the SLB; these units are bounded were recognized to the main Messinian events, Laga 3 units constrained (Fig. 5). Adopting the Messinian by three unconformity surfaces called I1, I2, I3, respectively scheme proposed by Krijgsman et al. (1999), and taking into account the basin-wide chronostratigraphic relationships between the unconformities as well the stratigraphic correlations of the recognized Messinian and the lower Pliocene deposits, Laga 1 unit is proposed to be deposited during pre- stage (ev) (5.96-5.61 Ma), and the stage (7.251-5.96 Ma), the Laga 2 unit during evaporitic evaporitic stage (p-ev1 and p-ev2) partially during the basal portion of Laga 3 unit during the post-evaporitic lower Pliocene (5.61-5.3 Ma) (Fig. 5). in the more western and proximal characters In the studied area I1, I2, and I3 surfaces show erosive conformities in the more distal and sectors of the basin (near Sibillini thrust) and turn into correlative eastern sectors, where the passage from Laga 1 to 2 and 3 is commonly transitional. the external margin of basin, where of angular unconformities towards These surfaces show the characters In the sector between Sibillini thrust and turbidite deposits onlapped onto the deforming external ramp. the Montagna dei Fiori-Montagnone alignment (Fig. 4) Laga 1 and 2 units reach their maximum Eastward East where these units onlapped onto an external regional ramp. thickness, which decreases towards of the Montagna dei Fiori-Montagnone alignment Laga 1 and 2 units are present in subsurface relationships are also evident in the interpreted seismic These stratigraphic while Laga 3 occurs in outcrop. wedging of the Laga 2006, 2009) showing the eastward section of Fig. 6 (Casero and Bigi, 2006; Bigi et al., In the same area Laga 3 unit is about 4000 m thick (Fig. 6) and 1 and Laga 2 units onto the substrate. turbidite deposits of the marls fm. and to the coeval pass to the slope sediments of Vomano transitionally to form a succession with clear both of lower Pliocene age. The three units are stacked Cellino fm., propagation of the Apennine thrust belt. forestepping pattern, reflecting the eastward geological field trips 2009 - 1(1) excursion notes 17 - 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 6 - Geological cross-section derived by the interpretation of seismic lines. Note the Eastwards wedging of the Laga 1 by the interpretation of seismic lines. Note Eastwards Fig. 6 - Geological cross-section derived section see fig. 4. Modified from Casero & Bigi, 2006. and Laga 2 units onto the substrate represented by the Cerrogns marls and Orbulina formations. In same area and Laga 2 units onto the substrate the position of cross marls and Cellino formations. For pass to the Vomano Laga 3 unit is 4000 m thick and transitionally Structural data suggest that during the Laga 1 deposition turbidite sedimentation insists on growing anticline Structural high, sedimentation Sasso structural Sasso thrust whereas, in the North of Gran associated to the Gran deposits Turbidite area, corresponding to the axial depozone. filled the deeper part of basin in Tronto on the western limb of Montagna dei onto the deforming monocline, as can be observed onlapped eastward of thrust (Fig. 6). The size of T1-T2 by the development Fiori - Montagnone anticline, folded, at present day, being the the same as nowdays, the basin and its shape during deposition of Laga 1 had to be approximately of Sibillini thrust. Restoration located in correspondence of the present-day zone slope-to-basin transition of T1 thrust, as the extension in the hanging wall geological cross section indicates a reduce shortening value Sasso ridge) and about of the basin could be around 75 km in South (immediately North Gran 30-35 km in the North (around Acquasanta structure). geological field trips 2009 - 1(1) excursion notes 18 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome -order depositional sequences -order depositional sequences. rd th and 4 rd The Laga basin: Stratigraphic and Structural Setting -order sequences were controlled by tectonics, recording increasing thrust propagation rd Basing on this, the Laga succession can be subdivided in two main composite 3 with duration of about 2 Myr. Both these sequences are stacked with a clear forestepping pattern. The first Both these sequences are stacked of about 2 Myr. with duration - lower sequence, informally named Laga Depositional Sequence (LDS), deposited during the upper Tortonian Messinian and includes the Laga 1 2 units. LDS records closing phase of Marnosa-arenacea foreland basin system. The second sequence, informally named Cellino Depositional Sequence (CDS), deposited marls, and Cellino fm. CDS during the upper Messinian - lower Pliocene and includes Laga 3 unit, Vomano records the initial depositional phase of upper Messinian to Present foreland basin system. The surface tectonic phase. related to the intra-Messinian these two sequences is the I3 surface and was separating Both these two 3 followed by a slowdown of their activity. This is testified by: i) basin reorganization producing change of followed by a slowdown of their activity. ii) dispersion of the turbidity currents (change in local paleocurrent and paleotopography; physiography variation directions); iii) external geometry and architecture of the turbidite channel systems, iv) temporal and depositional zones. of transfer of the sediment supply determining migration During deposition of Laga 2, the Acquasanta anticline started to grow and control distribution flows are though to be controlled by the occurrence of growing high sedimentary bodies in the basin. Turbidite Sasso thrust took place: in the in the East and South sectors where differential uplift of Gran at the surface, Borbona area, T2 thrust plane started to propagate as far the associated anticline arrays of the ancient pre-existing rotation and inversion - Monte Camicia sector, whereas in the Corno Grande reduced and the depth of Laga basin was high took place. In this condition, the physiography structural occurred. In this context, I2 surface can be retrogradation followed by a successive and an initial progradation shift of depocentre, controlled by the thrust activity. considered as the expression of a local, intrabasinal, to the East of I3 surface, located between Laga 2 and 3, represents the depocentre shift from West as well uplifted and tectonically transported, Montagna dei Fiori - Montagnone ridge. The western area was of the T1 thrust, which defined new Sasso Ridge, in the South. They represent hanging wall the Gran the internal which separates morphology of the basin. T1 thrust position corresponds to slope-to-basin sector, areas of the basin, site shelf sedimentation, from a deeper part, where turbidite sedimentation occurred Cellino fm.). (Laga 3 unit and successive interpretation of the Laga deposits (see correlation panels Figs. 7 and 8) A more detailed sequence stratigraphic the Laga 1, 2, and 3 units in terms of has allowed framing geological field trips 2009 - 1(1) excursion notes 19 -order th 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting -order LDS up to the gypsum-arenites. The thickness -order LDS up to the gypsum-arenites. rd The Laga Depositional Sequence This field trip will mainly examine the deposits of 3 lowstand sequences set with duration of about 400 kyr and 100 kyr. These units show variable thicknesses These units show variable of about 400 kyr and 100 kyr. lowstand sequences set with duration hundred meters in the depocenter from hundred meters in correspondence of basin margins to several ranging locally erosional surfaces. section, 9 in Fig. 7), and are bounded by sharp, (Vomano only trend with a preservation fining- and thinning upward All the high-frequency sequences show a vertical persistent sandstone beds in the medial-distal basin which are essentially constituted by laterally of the LSTs, portion of the basin. They sand deposits in the proximal channelized floor (lobe deposits) and by the coeval the basin floor fan, which record persistent siltstone and mudstone draping to thin and laterally pass upward a backstepping of the clastic depositional systems supplying fan and prolonged period sediment seem to suggest that during the deposition of LST most sands by- Such considerations starvation. continuous lobes in the medial and distal portion passed the channels and were deposited as thick laterally features (scours), lag deposits, and thin depositional area of the fan, erosive of the fan. In channelized sandstone bodies consisting of 3D bedforms occurred. During the final phase LST most sands were, instead, deposited into the channels; they formed thick trough-bedded sandstone bodies consisting of 3D extension occurred in the rise to composite bars. Lobes of minor thickness and lateral bedforms that give medial and distal basin floor fan. of this unit varies from 1350 m to 2650 m along the basin axis, from the Amandola to Vomano sections from 1350 m to 2650 along the basin axis, Amandola Vomano of this unit varies (Fig. 7). Thickness increases from 685 m to 2650 and then decreases 1229 (Vezzola respectively the eastern margin of basin, perpendicularly to basin axis, from Borbona section, 6' in Fig. 7) towards elements and stacking pattern architectural sections (sections from 1' to 9 in Fig. 7). Facies, to Vomano 2003), which records a phase of slope (sensu Gardner et al., allowed to interpret the LDS as a basinal cycle of the and basin deposition being the slope located in correspondence of present Sibillini thrust. Migration corresponding as related to thrust propagation represents the initial phase of a new cycle slope environment with the initial deposition of CDS. 4 organization of LDS (Figs. 7 and 8) indicate that it is formed by a stack several The stratigraphic geological field trips 2009 - 1(1) excursion notes 20 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 8 - Stratigraphic cross-section of the Laga Fig. 8 - Stratigraphic Depositional Sequence. turbidite deposits. The correlation panel is oriented the location see fig. 4. perpendicularly to basin axis. For LDS: Laga Depositional Sequence; CDS: Cellino Fig. 7 - Stratigraphic cross-section of the Laga Fig. 7 - Stratigraphic Sequence. turbidite deposits. The correlation panel is oriented the location see fig. 4. LDS: Laga to basin axis. For parallel Depositional Sequence; CDS: Cellino Architectural elements and depositional setting allowing reconstruction of the The LDS constitutes the expression of spectacular submarine fan complexes elements of the single fan, from slope to basin floor passing through channels sector. main architectural geological field trips 2009 - 1(1) excursion notes 21 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting The good exposures of the Messinian Laga deposits provide a valuable data set that can be used to study inside a valuable The good exposures of the Messinian Laga deposits provide and non- relationships between facies of channelized turbidite systems, the spatial-temporal the recognized fining and thinning- (lobe deposits) along a depositional profile. All systems show general strata channelized from from up- to downstream (generally trend, as well three main erosional and depositional zones upward where the processes iii) a lobe zone, zone; ii) a channel-lobe transition NW to SE): i) a channel complex zone; Downslope and upslope migration related to the passage of turbidity currents occur with a different intensity. of depositional rise to a generation of these sectors determines, through time, their superimposition and gives simple facies sequence to decametres composite from meter-thick order ranging units of different hierarchical elements as channel, lobe, and channel facies sequence, expression of single and composite architectural 1994, 1999). This mechanism, in turn related to variation (see also discussion in Mutti et al., lobe complexes processes as pulse of tectonic deformation and/or should be controlled by allocyclic in sediment supply, related to the intrinsic growth of submarine processes as avulsion climatic changes, and by autocyclic 2003). channel-lobe system (see also Gardner et al., Biagio section 2 of Fig. 7), wide (Isola S. In the more northern sector of Laga basin a submarine canyon during the initial as bypassing zone active was direction and up to 50-100 m deep, about 5 km in North-South deposition of the LST LDS (Fig. 9). This erosional feature is incised into older slope deposits and was amalgamated sandstones. Thin- thick-bedded, essentially filled during the late LST of LDS with channelized facies are interbedded with the mudstone and sandstones interpreted as overbank bedded fine and very-fine siltstone deposits of the slope environment. the (sector between Fluvione and Scalelle, sections 3 5 of Fig. 7, respectively), the toe-of-slope At basin area, of a broad, multy-story allowed formation, in the proximal decrease of the depositional gradient section during the early lowstand as far the Tronto fan) extending basinward (proximal channel complexes extending as far the passage to lobe zone marked zone sedimentation. Here a channel-lobe transition and frontal slopes of the basin (medial to distal fan). to the lateral of channel bodies reflecting i) the turbidite by a hierarchy are internally characterized Channel complexes and iii) the back-filling by avulsion, driven channel migration sedimentation at different scale, ii) the lateral episodes of cutting and filling related to processes. The single channels and a channel complex record several the passage of turbidity currents giving rise to simple or composite facies sequences that are expression phase. This mechanism is recorded at different of the bypassing phase and following back-filling geological field trips 2009 - 1(1) excursion notes 22 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 9 - Depositional setting of Laga basin during the sedimentation 1 (A), 2 (B), and 3 (C) units. The red box indicates the area of interest of this field trip. indicates the area of interest this field trip. red box hierarchical scales. At the level of the single channels bypassing and back-filling phases give rise to a fining-up phases give of the single channels bypassing and back-filling the level scales. At hierarchical thin deposits constituted by medium- to coarse facies sequences from 5 m to 10 thick. These have sands with rip-up clasts and scour evidences in the basal portion, which are interpreted as lag deposits. Most of the channel deposits are instead constitute by thick sandstone bodies showing internally a complex hierarchy of 3D bedforms; they record multiple episodes channel cutting and filling for prolonged period bypass. of sediment bedload after it has settled out a turbidity bedforms as ripple and dune document the movement currents from suspension and constitute the building block of composite bedforms (bars), some meters high the scale of a turbidite system (high-frequency depositional sequences) channels and hundred meters long. At during the deposition of early as depositional zone and, secondarily, as preferentially bypassing zone served phase). of the late LST (back-filling during the development LST and became essentially a depositional zones geological field trips 2009 - 1(1) excursion notes 23 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting At the channel-lobe transition zone flows velocity diminished because of widening the channels. The passage flows velocity zone the channel-lobe transition At extensive of laterally sedimentation and to generation from confined to unconfined conditions led rapid amalgamated to non- sandstone bodies (lobes). Such constitute 5 m to 10 thick-bedded, sandstones and siltstone deposits. The amalgamated turbidite beds interbedded with thin-bedded very-fine in the and dip sections is strongly marked kilometres), both in strike highly continuity of the beds (several correlation panels showing also lenticular and compensation geometries of the sandstone bodies. The bases show evidences of erosion. Crude to thick and/or fine sharp and rarely are relatively of these lobe complexes escape structure as processes and associated to other water often deformed by dewatering lamination, very of aggradation vertical sandstone beds. These features reflect rapid the thicker characterizes dish and pillar, than "en masse" deposition, as 1995; Baas, 2004), rather sediment during deposition (Kneller and Branney, are typical of flows having been described. Such sedimentological characters often these deposits have for a valid of the basal layer, during sedimentation; such a behavior subcritical condition of their basal layer as net depositional turbidity currents, allow also an analytical formulation for the change in bed elevation 2009) et al., 2006; Falcini et al., ignition condition (see discussion in Falcini function of the hydrodynamic sustained turbidite flows), in turn related to different triggering mechanisms of the flows (surge-type versus 1991; Milliman and Syvitski, floods (Normark and Piper, sediment failures, storms and river as earthquakes, 1996, 2003). 1998; Mutti et al., 1995; Mulder et al., 1992; Mulder and Syvitski, also during the elements developing are architectural and lobe zones Channel, channel-lobe transition change produced a physiographic sedimentation of Laga 2 unit (Fig. 9). During this phase the thrust reactivation connection of the basin and a decrease accommodation space on shelf areas leading to more close physical source points probably represented by sand-rich deltaic systems between deltas and turbidite systems. Several channels (no along the northwestern and western margin of basin. Several on narrow shelves developed seem to be present along the western margin of basin at this time) probably furrowed their prodelta canyons their sediment load. The slopes constituting the flank of contiguous basin through which flows deliver sand-rich turbidite systems by Heller and Dickinson, 1985; dimension of these delta-fed turbidite systems (ramp and by the extension of strongly controlled by the basin topography 2003) was systems by Mutti et al., mixed extension of the channel, channel-lobe the lateral supplying the deltas. Consequently, catchment area of the rivers and a local superimposition of the deposits related to different is highly variable and lobe zones transition source points occurs. geological field trips 2009 - 1(1) excursion notes 24 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Interaction with the confining slopes kilometres) occur in the middle and southeaster thick (5-10 m) lobes of major extension (several Thick to very and frontal near the lateral aggradation vertical portion of the basin (see Fig. 4). Their formation indicates a rapid 1999; slopes of the basin. Similarly to other confined settings (see Haughton, 1994, 2000; Kneller & McCaffrey, of the flows 2004), the interaction 2001; Moscatelli et al., Milli & Moscatelli, 2000, 2001; McCaffrey Kneller, highs leads to a modification of the flow pattern, reflecting high with the basin margins and intrabasinal Sasso of the paleocurrents and resulting facies. Along southern slope basin (the Gran variability of the turbidite flows when they Fig. 4), the great thickness of beds reflects a high sedimentation rate sector, rise to facies and give reflection, and deflection processes are common in this zone approach the slope. Ponding, sequences recording the sedimentation of incident and returning phase for same flow (see descriptions 1994; Grecula et al., et al., 1987; Edwards & Leeder, & Hiscott, 1985; Pantin of the same processes in Pickering 2004). 2003; Moscatelli, Moscatelli et al., These facies sequences show a basal portion (from 1.5 m to 5 thick) with crudely laminated medium fine with climbing ripple lamination. thin interval to a very escape structures, passing upward sandstone and water sharp and marks the passage to homogeneous siltstone-mudstone The top of this basal portion is generally deposits up to 3-4 m thick. Both these divisions are related the incident phase of flow and record impact basal portion of sedimentation of the more concentrated with the frontal slope. They can determine: i) rapid the flow; ii) rising of more dilute and turbulent portion along frontal slope iii) initial expansion sedimentation and rapid 1993) and its successive of the suspended cloud (lofting process; see Sparks et al., down along the slope, it moves When the rising flow depletes its own kinetic energy, before the returning flow. fine sandstone beds, discontinuous fine and very depositing part of the load sediments and giving rise to laterally by an oblique lamination opposite to the occurring in 10-20 cm thick, internally characterized underlying sandstone beds. geological field trips 2009 - 1(1) itinerary 25 E 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting FIRST DAY The boundaries of the Laga basin Fig. 1.1 - Onlap of the Laga 1 unit onto the lower Messinian external ramp. Red line indicates the I1 unconformity surface. Red Fig. 1.1 - Onlap of the Laga 1 unit onto lower Messinian external ramp. about 1 km. W Gradient of the ramp is estimated about 6°-8° (see also Casnedi et al., 2006). The thickness is about 300 m on a length of is estimated about 6°-8° (see also Casnedi et al., of the ramp Gradient Stop 1.1: Main road 80: Fano Adriano village Panoramic view of the Laga 1 unit onlapping onto western limb Montagna dei Fiori-Montagnone anticline. to observe: Features of the lower Messinian foreland ramp. - Geometry and gradient terminations (Fig. 1.1). - Stratal - Stacking pattern of the sandstone lobes. Problems to discuss: and morphology of of the sandstone lobes as expression basin subsidence, sedimentation rate, - Cyclicity the lower Messinian external ramp. geological field trips 2009 - 1(1) itinerary 26 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting ) optional Stop 1.2: Prati di Tivo ( The Gran Sasso thrust and its relationship with the Laga basin deposits. Apennines. The basal thrust, Sasso unit constitutes a complex and spectacular structure of the central The Gran carbonate succession onto the Laga basin deposits. The hanging places the Triassic-to-Miocene trending E-W, The internal is N-S. trend in the footwall to the thrust, whereas main structural main anticline is parallel wall thrust planes that repeat the sedimentary succession Sasso unit is composed by several architecture of the Gran succession is composed The stratigraphic elevation. and topographic it to reach a notable structural and make of the closer carbonate platform by a thick slope-to-basin carbonate succession that records the evolution to be noticed: the occurrence main features have paleodomain to the South. Two system of the Lazio-Abruzzi structure, and the occurrence of basinal deposits Triassic- high as the Corno Grande structural of Jurassic age, cropping out in the eastern sector of unit (bituminous dolostones to spotted limestone; Lower Jurassic 2005). Passeri, to observe: Features Intermesoli (Fig. 1.2). forelimb of the anticline Pizzo Sasso thrust; the overturned - Geometry of the Gran that with the forelimb strata in the Apennines show a similar geometry, Most of the fault-related-fold to the East, same geometry is more In corrispondance of the Corno Grande, overturnes. progressively high. structural complex due to the occurrence of Jurassic of Laga formation unconformity of the strata with the deposits of Laga fm. The progressive - Relationship Sasso unit started during the deposition of Laga 1 and 2 suggests that the tectonic activity of Gran that it constituted the southern border of Laga basin. Problems to discuss: - The southern boundary of the Laga basin. fold. style of fault-related control on structural - Paleogeography geological field trips 2009 - 1(1) itinerary 27 NW 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 1.2 - View from North-East of the E-W Gran Sasso front (road to Prati di Tivo). The overturned forelimb of the anticline The overturned di Tivo). Sasso front (road to Prati Gran Fig. 1.2 - View from North-East of the E-W carbonate multilayer passes upward to the Laga deposits through a progressive unconformity. to the Laga deposits through a progressive passes upward carbonate multilayer of Pizzo Intermesoli - Monte Corvo involves the slope-to-basin pelagic carbonate succession (Triassic to Early Miocene). The the slope-to-basin pelagic carbonate succession (Triassic involves Intermesoli - Monte Corvo of Pizzo SE geological field trips 2009 - 1(1) itinerary 28 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting 2.1 - Thick to very thick sandstone beds Aprati deposited at the base thick sandstone beds Aprati 2.1 - Thick to very sedimentation of the suspended mud. of the Laga basin frontal slope (Gran Sasso paleoslope). The great of the Laga basin frontal slope (Gran of the turbidite flows aggradation thickness of the beds reflects rapid processes are common and when they approach the slope. Reflection rise to facies sequence (double arrow in the figure) recording can give the sedimentation during incident (A, arrow indicate flow direction South) and returning phase (C, arrow indicate flow direction towards B indicates a deposit formed through rapid North) of the flow. towards SECOND DAY fault-related fold. lateral slope of the basin. Basin plain deposits of the Laga 1 The Montagna dei Fiori-Montagnone and Laga 2 units near the frontal Stop 2.1: Aprati The thick to very thick-bedded sandstone lobes of the Laga 1 unit. to observe: Features - The great thickness of the sandstone bodies. - The sharp passage between sandstone and mudstone intervals. - The presence of ripples in the sandstone in opposite directions (Fig. 2.1). beds verging Problems to discuss: - The great thickness of the sandstone beds sedimentation as an expression of a rapid connected to the (aggradation) confinement of the basin. The facies sequences developing - because the ponding effect (reflection processes). of the reflected and deflected - Characters sandstone and mudstone beds. geological field trips 2009 - 1(1) itinerary 29 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 2.2 - The transitional passage between the Laga 1 and 2 units, Monte Bilancere. Fig. 2.2 - The transitional Stop 2.2: Casagreca locality: a panoramic view of the Monte Bilanciere Basin plain sandstone lobes of the Laga 2 allounit. to observe: Features - Change of the depositional trend at passage from Laga 1 to 2 units (Fig. 2.2). of the turbidite succession. - Cyclicity geometry of the sandstone lobes (Fig. 2.3). - Tabular Problems to discuss: depocentre migration. tectonics and eastward - Syn-sedimentary geological field trips 2009 - 1(1) itinerary 30 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 2.4 - Sandstone lobes of the Laga 2 unit, Agnova. Fig. 2.3 - Panoramic view of Monte Bilanciere. Note the tabular geometry sandstone lobes Laga 2 unit and Fig. 2.3 - Panoramic the downward transitional passage to the mudstone and siltstone deposits of Laga 1 unit. transitional the downward Stop 2.3: Agnova village The basin plain sandstone lobes of the Laga 2 allounit. to observe: Features sandstone and architecture of the fine-grained - Facies lobes. - The high thickness of the sandstone lobes as an expression of sustained turbidity currents (Fig. 2.4). Problems to discuss: - The concept of bed and depositional event. bed”. - The significance of the “massive - Analytical approach to the deposition of a turbidity current. geological field trips 2009 - 1(1) itinerary 31 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 2.5 - Photomicrographs of a very-fine grain arenite grain of a very-fine Fig. 2.5 - Photomicrographs of S. Lugli, in Moscatelli et al., 2004). Lugli, in Moscatelli et al., of S. with gypsum cement. The light rounded area in the central part with gypsum cement. The light rounded area in the central of the picture is essentially occupied by a gypsum crystal. plagioclase, fragments Other components are quartz, feldspar, and biotite (courtesy of carbonate rocks (micrite), muscovite, evaporites, formed in semi- evaporites, w-water Stop 2.4: Paranesi village The resedimented gypsum-arenites of the Laga 3 unit. to observe: Features passage between the Laga 2 - The transitional and Laga 3 deposits. - Composition (Fig. 2.5) and sedimentary structures of the gypsarenites. Problems to discuss: - of the gypsum-arenites. Origin and provenance - The in the context significance of the gypsum-arenites and paleogeographic environmental of the Messinian foreland basin. deep-water Gypsarenites constitute relatively by erosion of resedimented deposits derived primary shallo basins in the western sectors enclosed thrust-top of the Miocene Apennine foreland basin (for a 2005). These detailed description see Manzi et al., fine-grained deposits consist of medium to very arenites with gypsum cement. crystals. The gypsum (up to 5 mm of diameter) and include remains anhydrite Gypsum crystals are curved of an original by the diagenetic transformation cement reach about 50-60% of the sandstones; it derives clastic gypsum deposited through resedimentation processes. The original texture has been completely which are related to the diagenetic transformations, gypsum-anhydrite-gypsum by the successive obliterated rocks of diagenetic anhydrite The secondary gypsum formed by hydration sulphate burial-exhumation cycle. 2004). contribution in Moscatelli et al., of clastic gypsum (Lugli S., from the burial-induced dehydration derived geological field trips 2009 - 1(1) itinerary 32 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 2.6 - Regional setting of the Miocene normal fault. View Fig. 2.6 - Regional West to East. West from Monte Girella to Monte Foltrone. The Stop 2.5 is from Monte Girella to Foltrone. places in indicated. The normal fault, dipping westward, deposits of the Corniola Fm. (Sinemurian- contact the Jurassic with the marne con Cerrogna Pliensbachian) in the footwall with a total offset of in the hanging wall, (Tortonian-Langhian) about 1400 m. The black lines indicate the attitude of bedding and the occurrence of folds in Corniola fm. due to syn- rotation of this miocene normal fault (Calamita contractional basinal succession dips eastward 1998). The Jurassic et al., from and is exposed along the road in Salinello Valley, Stop 2.5: Montagna dei Fiori (1) The Miocene normal fault and its relationship with the Montagna dei Fiori anticline. to observe: Features - Mesoscale deformation associated to the normal fault plane. - The normal fault regional setting (Fig. 2.6). Problems to discuss: normal - The occurrences of pre-contractional of Apennines fold and faults in the evolution thrust belt. Stop 2.6: Montagna dei Fiori (2) The Montagna dei Fiori anticline, the folded thrust plane of the Salinello Valley. to observe: Features and Cretaceous view of the Jurassic - Panoramic (Fig. 2.7). formations along the Salinello Valley - The geometry of the anticline, its recumbent forelimb and the associated folded thrust plane (Fig. 2.7, 2.8). - The geometry of the tectonic window. Problems to discuss: of the recumbent anticline and - The evolution the appropriate kinematic models (Di Francesco 2008, 2010). et al., geological field trips 2009 - 1(1) itinerary 33 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome Fig. 2.7 - Geological map of the The Laga basin: Stratigraphic and Structural Setting the stop 2.6. Montagna dei Fiori anticline (extract from Montagna dei Fiori anticline (extract 1992). 1 - Quaternary Centamore et al., deposits; 11,16,17 - Laga 3 8 Gypsum arenites ; 25,24,23,22 - Laga 1 and 2 deposits; 32 - marne con Cerrogna fm. (Miocene); 34,39,45 Scaglia Bianca, Rossa, and Cinerea Fms. (Upper Cretaceous Rosata - Oligocene); 50 marne a Fucoidi fm. (Aptian - Albian); 55,60,61,67 respectively Ammonitico and Rosso Maiolica, Salinello, Corniola fms. (Lower Cretaceous - Middle 68 - Calcare Massiccio fm. Jurassic); (Hettangian - Sinemurian). Note the normal fault that offset the backlimb of anticline to the west and tectonic window in succession The stratigraphic Salinello Valley. is well exposed along the road from stop 2.5 of the Miocene to stop 2.6. In the footwall normal fault the Corniola Fm. crops out, 400m Moving that, here, is dolomitized. the Corniola Fm. passes upward eastward, to a nodular lithofacies. Along the road, after a bend, there is large outcrop of the followed by the Ammonitico fm., Rosso Fm. After Calcari and Marne a Posidonia about 100m, the Salinello fm. crops out, made up of calcarenites and calcirudites. After the second tunnel is possible to and then the Calcari Diasprigni Fm., observe the Maiolica Fm. The cretaceous portion of succession follows, with the stratigraphic the terms of Scaglia Bianca, Rossa, Cinerea Fms. This latter is highly Rosata, deformed and crops out immediately after geological field trips 2009 - 1(1) itinerary 34 l, 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 2.8 - View of Salinello Valley from South. The fault associated to the Montagna dei Fiori anticline crops out in Fig. 2.8 - View of Salinello Valley the Scaglia Rossa formation is overturned and highly folded. formation is overturned the Scaglia Rossa Valley. The hanging wall consists of a recumbent fold having the Calcare Massiccio fm. in core. The forelimb progressively consists of a recumbent fold having The hanging wall Valley. succession. In the footwal the Cretaceous-Miocene terms of stratigraphic at the front of structure involving overturned geological field trips 2009 - 1(1) itinerary 35 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting THIRD DAY The Campo Imperatore Quaternary basin. Fig. 3.1 - The calcarenite di Monte Fiore fm. (on the right). comprises wackestones and grainstone, with strata and grainstone, comprises wackestones of about 60 cm thick, belonging to a carbonate by high energy characterized environment, ramps the top of formation, strata (on the left). To become thinner and show flow slumping tendency structure suggesting a deepening upward The upper Messinian-lower Pliocene piggy back deposits of Monte Coppe and Rigopiano conglomerates. Stop 3.1: Monte Coppe conglomerates (Upper Messinian) The Monte Coppe conglomerates (Upper Messinian) cover with an unconformity the calcareniti di Fiore fm. (Middle Miocene), carbonate ramp deposits belonging to the platform succession of Gran Sasso unit. to observe: Features of calcareniti di Monte Fiore fm. (Fig. 3.1). - Facies - Unconformity relationship between the Monte Fiore and Coppe fms. (Fig. 3.2). composition of Monte Coppe conglomerates. - Polygenic Problems to discuss: of the slope-to-basin carbonate - The evolution Sasso unit. succession of the Gran meaning of the Monte - The palaeogeographic Coppe conglomerates. - The meaning of this unconformity in the of the Laga basin. evolution geological field trips 2009 - 1(1) itinerary 36 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 3.2 - View from North of the unconformity surface between Monte Coppe conglomerates (cp; Upper Messinian) and Fig. 3.2 - View from North of the unconformity surface between Monte Coppe conglomerates the Monte Fiore calcarenites (mf; Middle Miocene). geological field trips 2009 - 1(1) itinerary 37 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 3.3 - Syncline made up by the Rigopiano Fig. 3.3 - Syncline d'Acero (NW). d'Acero conglomerates (Lower Pliocene), unconformably conglomerates placed onto the deformed Laga 3 deposits along Sasso unit. Note the front of the Gran N-S recumbent forelimb of the syncline. View from Forca NE SW View of Rigopiano Stop 3.2: Rifugio Forca d’Acero. conglomerates (Lower Pliocene) The Rigopiano conglomerates (Lower Pliocene) unconformably cover the Gran Sasso thrust. The Sasso unit represents a proximal source area during the deposition of Laga3-Cellino basin (CDS) (see also Fig. 9 - Excursion notes). to observe: Features (Fig. 3.3, setting of Rigopiano conglomerates - Syncline 3.4). Sasso thrust. Starting from with the Gran - Relationship Sasso became the source area Upper Messinian, the Gran deposits (Monte Coppe and Rigopiano for the gravel into the basin. conglomerates) Problems to discuss: meaning of the Rigopiano - The palaeogeographic conglomerates. - The meaning of their basal unconformity in the of the Laga basin. evolution Stop 3.3: Vado di Sole, Fonte Vetica - Campo Imperatore to Assergi. Vetica di Sole-Fonte basin along a road from Vado we cross the Campo Imperatore to Rome, Moving during Late Pliocene- Plain is an extensional basin, filled by continental deposits, developed Campo Imperatore due to the activity of south-dipping normal faults system. These extensional offset main Quaternary, with Sasso thrust. The relationship between these structures can be observed anticline associated to the Gran analysis performed in this areas, documented a seismic the help of Figures 3.4, 3.5, 3.6 and 3.7. Paleoseismic 2003). period (Galadini et al., activity along these normal faults during the Roman geological field trips 2009 - 1(1) itinerary 38 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 3.4 - Geological map of the eastern sector of the Gran Sasso unit (extract from Centamore et al., 1992). 1 - Quaternary from Centamore et al., Sasso unit (extract Fig. 3.4 - Geological map of the eastern sector Gran (Hettangian - Sinemurian); 69, 70 triassic dolostone and bituminous dolostone; 71 Monte Prena (Triassic). deposits; 3,4,5,6 - Cellino fm. (Lower Pliocene); 8 - Rigopiano conglomerate (Lower Pliocene); 11,13 - Laga fm.; 3,9,10 deposits; 3,4,5,6 - Cellino fm. (Lower Pliocene); 8 Rigopiano conglomerate (Upper Messinian); 30,31 - Monte Fiore fm. (Lower 44,49,54,61,64,65,66 Monte Coppe conglomerate 68 - Calcare Massiccio Fm. units belonging to a carbonate slop-to-basin succession (Cretaceous-Jurassic); lithostratigraphic geological field trips 2009 - 1(1) itinerary 39 SW 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 3.5 - View from the top of Monte Camicia (Gran Sasso unit). The stop 3.3 (Vado di Sole) is signed. The Rigopiano Sasso unit). The stop 3.3 (Vado Fig. 3.5 - View from the top of Monte Camicia (Gran Mountain and the N-S thrust-related anticline of the Maiella Mountain. thrust-related Mountain and the N-S NE conglomerates (with pattern in the picture) cover unconformably the N-S thrust of the Gran Sasso unit. The normal fault thrust of the Gran unconformably the N-S (with pattern in the picture) cover conglomerates fold of the Morrone fault-related Plain is evidenced. In the background NW-SE the Campo Imperatore system generating geological field trips 2009 - 1(1) itinerary 40 W 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 3.6 - View from the road crossing through Campo Imperatore Plain to the North. Monte Camicia is eastern peak Fig. 3.6 - View from the road crossing through Campo Imperatore In the foreground, the normal faults bounding the Campo Imperatore Plain are evidenced. In the foreground, normal faults bounding Campo Imperatore E along the E-W front of the Gran Sasso Unit. Here a peculiar Upper Triassic-Cretaceous succession crops out (Passeri, 2005). succession crops out (Passeri, Sasso Unit. Here a peculiar Upper Triassic-Cretaceous front of the Gran along the E-W geological field trips 2009 - 1(1) itinerary 41 NE 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Fig. 3.7 - View from the road crossing through Campo Imperatore Plain to the West. In the background highest crest Plain to the West. Fig. 3.7 - View from the road crossing through Campo Imperatore trending E-W. SW of the Gran Sasso Group (Corno Grande, 2989 m) consisting of Calcare Massiccio Fm. (Hettangian-Sinemurian). The back 2989 m) consisting of Calcare Massiccio Fm. (Hettangian-Sinemurian). Sasso Group (Corno Grande, of the Gran by the evidenced normal fault system, Sasso thrust is offset southward limb of the main anticline associated to Gran The Laga basin: Stratigraphic and Structural Setting 70th EAGE Conference & Exhibition - Rome 2008 g e o l o g i c a l

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42 m e m o r a n d u m geological field trips 2009 - 1(1) references 43 c s e e ion ogy, Bull. aly). artini, aziale- Central outhern nous facies azio-Abruzzo 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Soc. Géol. France, 168, 35-49. Soc. Géol. France, 166, 293-310. 52, 319-349. Italy). Mem. Sc. Geol. Padova, area (Apennines, Central 48, 275-288. Italy). Mem. Soc. Geol. It., Marche area (Apennines, central 155, 327-340. Palaeoecology, Palaeoclimatology, Palaeogeography, basin system, Italy. in Periadriatic ash layers 27, 523-539. Struct. Geol., Apennines (Italy). J. Central Boll. Soc. Geol. It., 122, 447-465. Boll. Soc. Geol. It., 126, 531-556. (Italy). Boll. Soc. Geol. It., 103, 311-326. Boll. Soc. Geol. It., abruzzese”. 110, 87-96. Strat., It. Pal. Apennines). Riv. Central Sasso, (Gran (Eds.), Anatomy of an Orogen: the Apennines and Adjacent Mediterranean Basins. Kluwer Academic Publishers, 327-350. of an Orogen: the Apennines and Adjacent Mediterranean (Eds.), Anatomy Apennines. Abstract, Am. Ass. Petrol. Geol. Annual Convention, 11-14 May, Salt Lake City, Utah. City, Salt Lake 11-14 May, Geol. Annual Convention, Am. Ass. Petrol. Apennines. Abstract, alla Carta delle Litofacies del L (Eds.), Note illustrative G. Mariotti & Sposato A., Kotsakis, T. Esu, R. Funiciello, Rita, D. CNR 114, 11-92. ed aree limitrofe. Quad. Ric. Scient., 55, 504-518. Minerals, and Clay Italy): what do they record? Clay and Hettangian pelagic facies in the Gran Sasso range. Boll. Soc. Geol. It., 109, 219-230. Boll. Soc. Geol. It., Sasso range. and Hettangian pelagic facies in the Gran Baas J.H., 2004 - Conditions for formation of massive turbiditic sandstones by primary depositional processes. Sedimentary Geol 2004 - Conditions for formation of massive Baas J.H., deposits in Marche of upper Messinian (“post-evaporitic”) sedimentology and paleogeography 2000 - Stratigraphy, Bassetti M.A., deposits in Central-S of the Messinian post-evaporitic stratigraphy 1994 - Physical M., & Roveri Ricci Lucchi F. Bassetti M.A., del “complesso torbiditico l generali 1984 - Associazioni di facies e lineamenti evolutivi P., & Valeri Landini B. Bellotti P., 122, 267-276. 2002 - The "pre-thrusting" Fiamignano normal fault. Boll. Soc. Geol. It., & Costa Pisani P., Bigi S. an example from th carbonate platform to a fold-and-thrust-belt: 2005 - From a deformed Peri-Tethyan & Costa Pisani P., Bigi S. Artoni A., 2007 - Growth rates and two-mode accretion in the outer orogenic wedge-foreland basin system of Central Apennine and two-mode accretion in the outer orogenic wedge-foreland basin system of Central 2007 - Growth rates Artoni A., Apennine. example from the Central 1997 - Sequential balancing of growth structures, the late Tertiary Artoni A. & Casero P., in the Monte Camicia success 2004 - Hettangian ammonites and radiolarians F., L. & Venturi Passeri Nannarone C., Bertinelli A., dating of volcani 2000 - New radiometric G., & Zanchetta Nisio S. Mozzi M., Leone G., Centamore E., Bonadonna F.P., Bigazzi G., Artoni A., 2003 - Messinian events within the tectono-stratigraphic evolution of the Southern Laga Basin (Central Apennines, It of the Southern Laga Basin (Central evolution within the tectono-stratigraphic 2003 - Messinian events Artoni A., References modelling in the forward 2003 - Coupled structural/stratigraphic & Sassi W., J.L. Rudkiewicz Eschard R., Casero P., Albouy E., Accordi G. & Carbone F., 1988 - Sequenze carbonatiche meso-cenozoiche. In: G. Accordi, F. Carbone, G. Civitelli, L. Corda, D. D Carbone, G. Civitelli, L. Corda, D. In: G. Accordi, F. carbonatiche meso-cenozoiche. 1988 - Sequenze Accordi G. & Carbone F., bitumi 1990 - Upper Triassic F., & Venturi F. Duranti A., Romano L., Passeri Cirilli S., G., Ciarapica Bigozzi A., Adamoli L., M & I.P. Vai, siliciclastic turbidite systems of the Northern Apennines. In: G.B. 2001 - Tertiary Argnani A. & Ricci Lucchi F., Aldega L., Botti F. & Corrado S., 2007 - Clay mineral assemblages and vitrinite reflectance in the Laga Basin (Central Apennine assemblages and vitrinite reflectance in the Laga Basin (Central mineral 2007 - Clay S., & Corrado Botti F. Aldega L., geological field trips 2009 - 1(1) references 44 o he ro- udi em. erti, ione f the logici s and eale e amerti, on: the nico del 2009 - ing sulla anzini D., 125-140. 981-1982 Messinian F. & Tortorici F. 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting International Geological Congress, Firenze 2004. International Geological Congress, Firenze nd evolution of Central Apennines. Abstract 32 Apennines. Abstract of Central evolution sedimentation within a Messinian foredeep in the Central Apennines, Italy. J. Petr. Geol., 22, 5-18. Geol., Petr. J. Apennines, Italy. sedimentation within a Messinian foredeep in the Central settentrionali). St (Marche meridionali Lazio-Abruzzo le aree umbro-marchigiana e laziale-abruzzese d'incontro" tra della "zona spec. (1991/2), 21-26. Geologici Camerti, vol. Assembly 2006. XY0592, EGU General session Ts7.2 Poster basin analysis. Abstract, for integrated Laga basin: constraints area, Italy). Studi Geologici Cam Apennines (Lazio-Abruzzo, styles and shortening in the Central structural foredeep evolution, num. spec. 2003, 17-37. - Analisi dell'evoluzione tettonico-sedimentaria dei "bacini minori" torbiditici del Miocene medio-superiore nell'Appennino umb tettonico-sedimentaria dei "bacini minori" torbiditici del Miocene medio-superiore nell'Appennino - Analisi dell'evoluzione Fiastrella. Studi Geologici C Fiastrone- T. ed il F. Potenza il F. 9) il Bacino della Laga tra marchigiano e laziale-abruzzese: 7, 17-79. Stratigraphy, structural setting and thermal history of the Messinian Laga Basin in context Apennine foreland basin syst structural Stratigraphy, Med. Earth Sciences, 1, 61-84. J. area during the Neogene. reconstruction of the peri-Tyrrhenian and paleogeographic restoration 1990 - Palinspastic L., 77, 41-50. Paleoecology, Paleoclimatology Paleogeography 13, 873-881. Apennines, Italy). 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The control exerted and Moscatelli, M., Milli, S., Costa Pisani, P., Bigi S., vs flexure migrati thrust front/foredeep depocenter migration 2004 - Active & Moscatelli M., Milli S. Costa Pisani P., Bigi S., Bigi S., Calamita, F., Cello, G., Centamore, E., Deiana, G., Paltrinieri, W., Pierantoni, P.P., and Ridolfi, M., 1999. Tectonic and Ridolfi, M., P.P., Pierantoni, W., Paltrinieri, Deiana, G., Centamore, E., G., Cello, Calamita, F., Bigi S., Cantalamessa G., Centamore E., Chiocchini U., Di Lorito L., Leonelli M., Micarelli A., Pesaresi A., Potetti M., Taddei L. & Ven Taddei M., Potetti A., Pesaresi Micarelli A., Leonelli M., Di Lorito L., Chiocchini U., Centamore E., Cantalamessa G., Boccaletti M., Ciaranfi N., Cosentino D., Deiana G., Gelati R., Lentini F., Massari F., Moratti G., Pescatore T., Ricci Lucchi T., Pescatore G., Moratti Massari F., Lentini F., Gelati R., Deiana G., Cosentino D., N., Ciaranfi Boccaletti M., of deformation, and time-space relationships in t styles, chronology rates 1994 - Structural Cello G. & Deiana G., Calamita F., Cittar Auct. tra della linea Ancona-Anzio 1987 - Analisi strutturale S., C. & Mastrovincenzo Invernizzi Deiana G., Calamita F., di Adria nel sistema oroge del paleomargine mesozoico 2002 - Il ruolo dell'architettura M. & Satolli S., Pelorosso Calamita F., 1998 - Il buttressing delle faglie sinsedimentarie pre-thrust G. & Scisciani V., Rusciadelli Ridolfi M., Pizzi A., Calamita F., 1 M., & Potetti F. Pontoni Micarelli A., Marchetti P., Giardini G., Di Lorito L., Chiocchini U., Centamore E., Cantalamessa G., Bigi S., Milli S., Corrado S., Casero P., Aldega L., Botti F., Moscatelli M., Stanzione O., Falcini F., Marini M. & Cannata D., F., Falcini Stanzione O., Moscatelli M., Botti F., Aldega L., Casero P., S., Corrado Milli S., Bigi S., geological field trips 2009 - 1(1) references 45 i 6. . ica. Soc. stern . Boll. bacini ennino zio" dal aternari Marche. (Central enza dei idolfi M., Camerti, isi di facies 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting Umbro-Marchigiano. Studi Geologici Camerti, 1, 7-89. Umbro-Marchigiano. 63, 83-91. line. Sedimentary Geology, Apennines along the "Ancona-Anzio" of the Central evolution the structural depositi terrigeni neogenici di avanfossa del teramano (Abruzzo settentrionale). Boll. Soc. Geol. It., 112, 63-81. settentrionale). Boll. Soc. Geol. It., (Abruzzo del teramano depositi terrigeni neogenici di avanfossa 5) Risultati degli studi umbro-marchigiano e laziale-abruzzese: minori" torbiditici del Miocene medio-superiore nell'Appennino 18, 135-170. Mem. Soc. Geol. It., in corso. Geol. It., 35, 591-601. Geol. It., num. spec. 2003, 39-48. 1992 - Carta geologica dei bacini della Laga e del Cellino riliev M., Mancinelli A. & Potetti Chiocchini M., Salvucci R., Firenze settentrionale). Scala 1:100.000. S.EL.C.A., carbonatici circostanti (Marche meridionali, Lazio nord-orientale, Abruzzo 111, 437-447. Soc. Geol. It., limitrofe. Studi Geologici e delle zone marchigiano-abruzzese dei depositi del Miocene e Pliocene inferiore dell'avanfossa spec. 1991/2, 125-131. Camerti, vol. Studi Geologici Camerti, vol. spec. "La Geologia delle Marche", 35-55. Studi Geologici Camerti, vol. spec. 1991/2, 375-379. Studi Geologici Camerti, vol. 17, 161-189. Lias medio al Pliocene. Geologica Romana, 24, 325-336. Italy). Mem. Soc. Geol. It., affioranti tra il F. Potenza ed il F. Tronto. Studi Geologici Camerti, num. spec., Riunione Gruppo di Sedimentologia del CNR, Studi Geologici Camerti, num. spec., Tronto. ed il F. Potenza il F. tra affioranti 26-29 Settembre 1983. Benedetto del Tronto, Camerino - S. 24, 221-232. Marche). Mem. Soc. Geol. It., part of Laga basin during the Upper Miocene-Lower Pliocene (central-southern Chiocchini U. & Cipriani N., 1989 - The composition and provenance of the Tortonian and Messinian turbidites in the context of of the Tortonian 1989 - The composition and provenance & Cipriani N., Chiocchini U. Centamore E., Chiocchini U., Cipriani N., Deiana G. & Micarelli A., 1978 - Analisi dell'evoluzione tettonico-sedimentaria dei " 1978 - Analisi dell'evoluzione Deiana G. & Micarelli A., Cipriani N., Chiocchini U., Centamore E., dell'App 1971 - Contributo alla conoscenza del Giurassico Micarelli A. & Pieruccini U., Deiana G., Chiocchini M., Centamore E., Centamore E. & Nisio S., 2003 - Significative events in the periadriatic foredeeps evolution (Abruzzo - Italy). Studi Geologici (Abruzzo in the periadriatic foredeeps evolution events 2003 - Significative Centamore E. & Nisio S., R Micarelli A., Micarelli A., Morelli C., Fumanti F., Cantalamessa G., Casnedi R., Bigi S., Berti D., Adamoli L., Centamore E., e anal 1991 - Stratigrafia Morelli C. & Ridolfi M., Bigi S., Berti D., M., Potetti Micarelli A., Cantalamessa G., Centamore E., 1993 - Contributo alla conosc Cristallini C. & Morelli C., Ridolfi M., M., Potetti Micarelli A., Cantalamessa G., Centamore E., Casnedi R., 1991 - L'avanfossa abruzzese tra i F. Vomano e Pescara nel Pliocene inferiore: rapporti tra sedimentazione e tetton tra nel Pliocene inferiore: rapporti e Pescara Vomano i F. tra abruzzese 1991 - L'avanfossa Casnedi R., del pescarese dati sui depositi neogenici di avanfossa 1992 - Nuovi Micarelli A. & Morelli C., Berti D., Bigi S., Centamore E., Casero P. & Bigi S., 2006 - Deep structure of the Laga Basin. Abstract, Poster session TS7.2 - XY0591, EGU General Assembly 200 - XY0591, EGU General session TS7.2 Poster 2006 - Deep structure of the Laga Basin. Abstract, & Bigi S., Casero P. lungo la "Linea Ancona-An e sovrascorrimenti trascorrenze distensive, 1978 - Fasi A., Colacicchi R. & Praturlon Castellarin A., line Pliocene history of the Ancona-Anzio 1982 - The Jurassic-Lower A. & Cantelli C., Praturlon Colacicchi M., Castellarin A., Mem. della Linea Olevano-Antrodoco. del settore centrale strutturale 1986 - Evoluzione M., & Tozzi Salvini F. G. P., Cavinato Cantalamessa G., Centamore E., Chiocchini U., Micarelli A. & Di Lorito L., 1982 - Tectonic sedimentary evolution of the northwe sedimentary evolution 1982 - Tectonic Micarelli A. & Di Lorito L., Chiocchini U., Centamore E., Cantalamessa G., 1986 - Il Miocene delle con la coll. di Di Lorito L., M., Micarelli A. & Potetti Chiocchini U., Centamore E., Cantalamessa G., Cantalamessa G., Centamore E., Chiocchini U., Di Lorito L., Micarelli A. & Potetti M., 1983 - I depositi terrigeni neogenico-qu M., Micarelli A. & Potetti Di Lorito L., Chiocchini U., Centamore E., Cantalamessa G., geological field trips 2009 - 1(1) references 46 es. afia e Italy). odoco. bstract ematica. ated fold Centrale. deposits: carbonate ni dell'Italia of a turbidite 70th EAGE Conference & Exhibition - Rome 2008 70th EAGE Conference & Exhibition - Rome The Laga basin: Stratigraphic and Structural Setting an example from the Laga formation (central Apennines, Italy). In: Kneller B., Martinsen O.J., McCaffrey B. (Eds.), External McCaffrey B. Martinsen O.J., Apennines, Italy). In: Kneller B., an example from the Laga formation (central depositional systems. SEPM Spec. Publ. 92, 347-362, ISBN: 978-1-56576-136-0. controls on deep-water current as a function of the Richardson number: sedimentological implications for interpretation turbidite facies. A depositional systems, climate, sea- Joint SEPM/Geological Society of London Conference: External controls on deep water volume, Sedimentology, 41, 347-461. Sedimentology, (Central Apennines, Italy), using combined kinematic models. Trabajos de Geologia Journal, special volume YORGSET, 49-60. YORGSET, de Geologia Journal, special volume Apennines, Italy), using combined kinematic models. Trabajos (Central 3, 423-434. Nova, Apennines system. Terra Boll. Soc. Geol. It., 114, 245-276. Boll. Soc. Geol. It., In: Arribas Apennines, Italy. an example from Upper Miocene arenites of the Central Basin Systems: detrital modes in Foreland Geological Society of and Geochemical Perspectives. Petrographic & Johnsson M. (Eds.), Sedimentary Provenance: Critelli S. J., 420, 107-134. America Special Paper Apennines, fold (Central model for the Montagna dei Fiori fault-related in the construction of a forward stratigraphy Jurassic Geological Journal, DOI:10.1002/gj.1191. Studi Geologici Camerti, vol. spec. (1991/2), 143-149. Studi Geologici Camerti, vol. spec. 1991/2, 161-166. Studi Geologici Camerti, vol. centrale. alla scala 1:50.000. Studi 367 "Tagliacozzo" sedimentologia delle successioni carbonatiche di piattaforma comprese nel F. spec. (1991/2), 167-171. Geologici Camerti, vol. 115, 423-437. Boll. Soc. Geol. It., foredeep. Studi Geologici Camerti, vol. spec. 1991/2, 139-142. Studi Geologici Camerti, vol. 77, 185-195. Sedimentary Geology, Falcini F., Milli S., Moscatelli M., Stanzione O. & Salusti E., 2006 - A simple three layers model for the eulerian behaviour model for the eulerian behaviour 2006 - A simple three layers & Salusti E., Stanzione O. Moscatelli M., Milli S., F., Falcini Falcini F., Milli S., Moscatelli M. & Stanzione O., 2009 - On the possibility of inferring paleoflow conditions from turbidite Moscatelli M. & Stanzione O., Milli S., F., Falcini Doglioni C., 1991 - A proposal of kynematic modelling for west-dipping subductions - Possible application to the Tyrrhenian- subductions - Possible 1991 - A proposal of kynematic modelling for west-dipping Doglioni C., 1994 - On experimental reflected density currents and interpretation of certain turbidit Leeder M.R. & Best J.L., D.A., Edwards Critelli S., Le Pera E., Galluzzo F., Milli S., Moscatelli M., Perrotta S. & Santantonio M., 2007 - Interpreting siliciclastic- & Santantonio M., S. Perrotta Moscatelli M., Milli S., F., Galluzzo E., Le Pera Critelli S., 2010 - Contribution of different kinematic models and a complex J., & Poblet Bigi S. Santantonio M., S., Fabbi L., Di Francesco modelling of the Montagna dei Fiori fault-rel 2008 - Forward & Bigi S., J., Poblet, M., Santantonio, S., Fabbi L., Di Francesco Civitelli G., Corda L. & Mariotti. G., 1991 - Ulteriori dati sui minerali pesanti e sulle litofacies di alcuni depositi terrige 1991 - Ulteriori dati sui minerali Corda L. & Mariotti. G., Civitelli G., 1991 - Lito-biostratigr Pichezzi R.M. & Santantonio M., Molinari V., M. C., Giovagnoli F., Galluzzo D'andrea M., Compagnoni B., 35, 323-347. Sibillini Mountains. Mem. Soc. Geol. 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