Quaternary International 101–102 (2003) 93–101

Effects of uplift and tilting in the Central-Northern Apennines (Italy)

Ernesto Centamorea,*, Stefania Nisiob

aDipartimento di Scienze della Terra Universit "a ‘‘La Sapienza’’, P.le A. Moro, 5-00185 Roma, ItalybDipartimento dei Servizi tecnici Nazionali, Servizio Geologico Nazionale V. Curtatone, 3-00185 Roma, Italy

Abstract

The morphotectonics of the Central-Northern Apennines reflect the effects of Pliocene–Pleistocene regional uplift and tectonics.

High uplift rates and extensional tectonics prevailed in the axial sector, while lesser uplifting, eastward tilting, and gravity sliding

affected the Periadriatic belt. The axial sector has a chocolate-slab pattern of blocks with intermontane depressions, bounded by

normal faults and characterized by differential vertical movements. The Periadriatic belt is a NE dipping monocline, broken by

transverse faults into separate blocks with different evolutionary development. The evolution of the axial sector can be correlated

with that of the Periadriatic sector because the unconformities in the marine succession of the Periadriatic basin are linked to pulses

of uplift in the axial chain. The amounts of coarse-grained sediments in intermontane depressions and in the Periadriatic belt are

correlated with the erosion processes affecting the axial sector. This morphostructural pattern may be connected with the formation

of a long-wavelength bulge associated with mantle upwelling.

r 2002 Elsevier Science Ltd and INQUA. All rights reserved.

1. Introduction

By the end of the Lower Pliocene the formation of theApennine thrust belt was almost complete (Figs. 3b and5a). Then, during Middle Pliocene–Early Pleistocene,the inner axial part of the Apennine chain emerged as acontinental domain, while in the eastern sector, thePeriadriatic basin, the marine environment persisted(Fig. 5b).The morphostructural pattern of the Apennine

continental landscape is strongly controlled by: (a) theprogressive eastward shifting of extensional tectonics;(b) the regional uplift; (c) the behavior of the lithoidsubstratum; and (d) the climatic conditions.In contrast, in the Periadriatic basin the depositional

environments were tightly linked to: (i) the progressiveeastward tilting of this sector; (ii) the lithological supplyfrom the chain; and (iii) the latest phases of thecompressive tectonics which could be due to the effectsof gravity sliding along Messinian evaporites and LowerPliocene clay deposits.These processes operated with different mechanisms

in different sectors on a complex thrust belt, whose

evolution was controlled by the activity of the pre-thrusting structural elements. From the Middle Plioceneto Lower Pleistocene, the inner and the outer sectorswere subdivided into a set of blocks, bordered by faultsand affected by differential vertical movements (Bigiet al., 1997b; Nisio, 1997). The aim of the present paperis to propose some correlations between the evolution-ary trend of the inner Apennine chain sector and thePeriadriatic basin sector (see Fig. 1).

2. Apennine chain sector

After the Lower Pliocene the axial Apennine sectorslowly began to emerge under subarid climatic condi-tions, and was eroded to a low relief landscape, theremnants of which are recognizable today on the highestmountain tops (Summit surface, Demangeot, 1965;paleolandscape Auct. Figs. 3c and 5b). From the Middleto Late Pliocene in this sector, a relative tectonicquiescence between the compressive tectonics final phaseand the beginning of the extensional one can beobserved. Thus, in this interval, other low relief surfaceswere formed, enclosed in the Summit surface andarranged at different heights (relict surfaces, Centamoreand Nisio, 2002; Centamore et al., in press; ororographic terraces Ciccacci et al., 1989 and references

*Corresponding author.

E-mail addresses: ernesto.centamore@uniroma1.it (E. Centamore),

stefania.nisio@dstn.it (S. Nisio).

1040-6182/02/$ - see front matter r 2002 Elsevier Science Ltd and INQUA. All rights reserved.

PII: S 1 0 4 0 - 6 1 8 2 ( 0 2 ) 0 0 0 9 2 - 7

therein). Locally, these are covered by the firstcontinental deposits (Figs. 3c and 5c).In the Late Pliocene, a sharp and intense impulse of

regional uplift and the first notable development ofextensional tectonics can be observed. Extensional faultscut the substratum and the first continental depositswith offsets up to some hundreds of metres (Fig. 3d).Many of these faults have reactivated former structures,sometimes with tectonic inversion processes. The inter-montane depressions began to form in this tectonicstage, and to be filled by lacustrine and fluvial deposits.On the mountainsides, steep tectonic scarps formed

and, from these, large blocks or chaotic heaps slid intothe depressions. Large volumes of breccias formed,covering the paleosurfaces and landslides and filling theintramontane basins (Fig. 3d), sometimes with debrisflow processes, (Centamore and Nisio, 2002; Centamoreet al., in press). The gravitational movements and thedebris flow processes were triggered by an intenseseismic activity, linked to the increase in regional upliftand extensional tectonics (Centamore and Nisio, 2002;Centamore et al., in press).These features are clearly evident in many localities of

the Central-Northern Apennines, where the remains oflarge paleolandslides and of the Lower Villafranchianbreccias (Brecce di Poggio Poponesco; Brecce di Car-

amanico; Brecce di Poggio Macchione, etc.) crop out(Farabollini and Nisio, 1996; Nisio, 1997; Centamoreand Nisio, 2002; Centamore et al., in press, Fig. 3d).During the Lower Villafranchian, the regional uplifting,extensional tectonics, and seismic processes intensified,with the differences in height between the intermontanedepressions and the uplifting blocks growing to a totaloffset of 500–600m (Fig. 3d).

An example of these phenomena is found on thesouthwestern side of the Carcariola ridge (Fig. 2),located between the Salto and the Velino Valleys atthe northwestern edge of the Rieti Villafranchian basin.The Lower Villafranchian continental succession isfaulted and tilted, with an offset of 200–250m. Ananalogous situation is observed along the Fiamignano-Micciani fault where the paleolandslides, the Brecce di

Poggio Poponesco and the paleosurface are cut withoffsets of 250–300m (Centamore and Nisio, 2002;Centamore et al., in press, Fig. 3c).In the Upper Villafranchian, a relative tectonic

quiescence stage is observed. In the intramontanebasins, new continental deposits unconformably coveredthe faulted older continental deposits and the substra-tum (Barberi and Cavinato, 1993; Centamore and Nisio,2002, Fig. 3e).At the end of the Lower Pleistocene, the axial Apennine

chain was affected by a new, intense pulse of regionaluplift (up to 2000m, Dramis, 1993) and extensionalfaulting was accompanied by a climatic change towardscold conditions. These factors favored river erosion,forming very narrow and deep V-shaped valleys.In the Middle to Upper Pleistocene, several climatic

changes occurred, from cold-arid conditions to tempe-rate-wet ones. During the cold-arid stages a large outputof debris from the denuded slopes piled up in theintermountain basins forming large alluvial fans andcovered the alluvial plains. During the temperate-wetconditions the linear erosion processes started againwith the incision of former deposits and the deepeningof the valleys, indicated by the presence of severalalluvial terraces at different heights (Centamore andNisio, 2002; Centamore et al., in press).

Fig. 1. Location of the studied areas.

E. Centamore, S. Nisio / Quaternary International 101–102 (2003) 93–10194

Fig.2.(a)MorphologicalschemeoftheS.Vittorinoarea.a,Lithoidsubstratum;erosionalunits(relictsurfaces):b,CimatadelCastellouppersurface;c,Fontanellelowersurface;

Depositionalunits:d,S.Vittorinosyntheme(Olocene);e,Caporiosyntheme(UpperPleistocene);f,Canetra—Cittaducalesyntheme(MiddlePleistocene);g,Fontanellesyntheme

(UpperVillafranchian);h,Calcariolasyntheme(LowerVillafranchian);Continentaldeposits(Overprintonthesynthemecolour):i,recentalluvialdeposits;j,sandy-clayeylacustrine

deposits;k,conglomeraticalluvialdeposits;l,paleolandslides;m,alluvialfandeposits;n,breccias;o,alluvial–colluvialanddetritaldeposits;p,debrisslope;q,travertines;slope

landformsanddepositsduetogravity:r,landslidescarps;s,landslidedeposits;t,slopeinvolvedinslopedeepgravitationaldeformations(SDGD);u,trench;structuralelements:v,fault

withquaternaryactivity;w,buriedfaults;x,tectonicfacetslope.b,MorphotectonicschemeoftheS.Vittorinoarea.

E. Centamore, S. Nisio / Quaternary International 101–102 (2003) 93–101 95

At this time the regional uplift and extensionaltectonics activities continued, markedly contributing tothe arrangement of today’s morphostructural pattern. Avery important tectonic feature, with transtensive faults,

developed during the Middle Pliocene. At this tectonicstage the Fiamignano-Micciani fault and its associatedsystem of the Salto and Velino Valleys were reactivated(Faccenna et al., 1993; Bosi et al., 1994; Centamore and

Fig. 3. Sketch of the morphostructural evolution of an inner Apennine intermountain depression.

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Nisio, 2002; Centamore et al., 2002). The transtensiveactivity of these faults dislocated late Middle Pleistocenedeposits, and the S. Vittorino plain formed (Centamoreet al., in press; Fig. 2).

3. Periadriatic basin sector

From the Middle Pliocene to the Lower Pleistocene,the marine environment persisted only in the Periadria-tic basin, partly superimposed on the more easternsector of the Apennine thrust belt and partly on thechain foreland ramp (Fig. 5b). The physiography of thisbasin is therefore largely inherited from the complexLower Pliocene imbricate fan thrust system (Ori et al.,1991; Fig. 5a) and its evolution was controlled by theactivity of several structural elements of this system.These ones are represented by two buried ridges (theInner ridge and the Coastal ridge), trending approxi-mately N-S, located at the front of two main thrusts,and by transverse and oblique fault systems, oftensuperimposed on pre-existing structural elements (Bigiet al., 1997b, 1999b, and references therein, Fig. 4).The progressive growth of the two ridges controlled

the paleogeography evolution, the depositional systemgeometry and the detritus dispersal in the Periadriaticbasin (Ori et al., 1991; Bigi et al., 1997a, b, 1999b). TheInner and Coastal ridges represent two ramps-anticlinedetached at the Messinian evaporites level (Figs. 5cand d).The transverse and oblique faults split the Marchean-

Abruzzi sector of the Periadriatic basin into six sectors(Fig. 4), each having a different tectonic and sedimen-tary evolution (Bigi et al., 1996, 1997a, b). The Fermo

sector, filled by bathial deposits, and the Vasto sector, inwhich the Aventino-Sangro gravity flow slid, are thedeepest of these, while in the other sectors a shelfenvironment developed (Fig. 4). The marine successionof the Periadriatic basin presents numerous facies andthickness variations from one sector to another. Thesevariations are closely linked to the effects of synsedi-mentary tectonics, to the progressive eastward tilting,and to the interactions between these processes and theApennine chain uplift (Fig. 5).Several main depositional sequences have been

recognized inside the marine succession: P2, Qm, Qm1,Qc (Centamore and Micarelli, 1991) or MP1, MP2 UP, Q(Ori et al., 1991). Within these sequences, other lowerrank cycles have been distinguished (P2a,P2b, P2c, in theP2, and Qma, Qmb, Qm1 in the Qm sequences; Bigi et al.,1997a). Such sequences and minor cycles are boundedby angular unconformities in the innermost and margin-al sectors of the basin, while in the deeper partscomparable deposits attain maximum thickness anddepositional continuity, and correlative conformities areobserved. The bases of the main and minor rank cycles

are conglomerate and sandy deposits, related to themain erosional stages affecting the uplifting inner chain(Fig. 5). The unconformities are closely linked to theinteractions between the chain uplifting and theprogressive eastward tilting in the Periadriatic belt,while tectonic effects have been locally amplified orweakened by eustatic changes.The basal transgressive littoral deposits lie uncon-

formably on folded and eroded Messinian and Plioceneforedeep units (Fig. 5b). This shows a first tilting stageof the Periadriatic belt, then an erosional phase, andsoon afterwards marine sedimentation, linked to ahighstand event. The transgressive deposits are locatedbetween the inner uplifting chain and the easternpersistent marine domain. The age of the transgressiondiffers little between the Fermo sector and the southernones. In the former, the basal Periadriatic successionwas deposited in the early G. crassaformis zone, while inthe sectors to the south of the Tordino river thetransgression began in the upper part of the same zone.These differences are probably linked to different tiltingmagnitudes among these sectors.A remarkable Middle Pliocene tectonic stage can be

observed in the western marginal part of the Periadriaticbelt. The transgressive deposits are often dislocated byeastward-dipping normal faults. More recent depositsonlap these tectonic scarps, often with clay on claycontacts.In the Periadriatic belt other some important tilting

stages are indicated by unconformities within the marinesuccession:

(a) 2.1-Ma event is indicated by further growth of theInner and Coastal ridge (Bigi et al., 1996, 1997a, b).It is accompanied by intense rhyolitic explosivevolcanism (Bigazzi et al., 2000). During this stage(sequence P2c) the shoreline shifted to the E,accompanied by erosion (Fig. 5c). Near Bellante(Teramo sector) shoreface sediments were depos-ited, with 15–201 angular unconformity, on a tiltedopen marine succession at the top of the growinginner ridge.

(b) After the Emilian another important tilting stage,associated with a first uplift of the Periadriaticsector, with a marked regressive trend (sequenceQmb), is indicated by of Sicilian shoreface coarsedeposits resting on the tilted and eroded rocks ofthe former marine successions with a 20–251angular unconformity (Farabollini and Nisio,1996; Nisio, 1997; Bigi et al., 1997a, b andreferences therein). At the end of Sicilian the furthergrowth of the eastern Coastal ridge (Bigi et al.,1997a, b) and the gentle folds affecting the Siciliandeposits in the Montesilvano-Campomare ridge(Centamore et al., 1999) may result from the last,weak compressive episode probably due to gravity

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Fig.4.GeologicalschemeofthePeriadriaticbasin.

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tectonics along the Messinian evaporites and LowerPliocene deposits. Also the eastward monoclinepattern of the Periadriatic sector developed in thisstage (Fig. 5d).

(c) At the end of Lower Pleistocene, the last remark-able tilting movement and a general uplift in acontinental domain affected the Periadriatic sector(Sequence Qc). The ‘‘Crotonian’’ continental depos-its lie on the different tilted and eroded terms of themarine succession, with a 10–151 angular unconfor-mity (Fig. 5d). A very large amount of coarsesediment is arranged in a set of coalescent alluvialfans at the foot of the chain, an intermediate, wide

alluvial plain, while on the eastern side coastallagoons are present.

Within these two last stages the vertical movementsthat affected the Periadriatic basin varied from onesector to another, often with marked vertical movementinversion. The Middle-Upper Pliocene Mt. Ascensioneconglomerates were deposited in the Fermo sector at500–600m depth as the Middle Pliocene deposits of theVasto sector, and they are now at an altitude of 1100m.In contrast, the coeval sediments of the other sectors weredeposited in a shelf domain (200–250m) and today theyare located at an altitude of 250–450m. a.s.l. (Fig. 4).

Fig. 5. Scheme of the Plio-Pleistocene morphostructural evolution of the periadriatic sector.

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During the ‘‘Crotonian’’ stage, the Mt. Ascensionelandscape constituted an inselberg emerging from analluvial plain with some hundreds of metres (300–400)difference in height. In this interval the transverse andoblique faults assumed a very important role inseparating the different sectors and in controlling thetilt magnitude. In the more tilted and uplifted sectors theupper part of the Periadriatic succession is almostcompletely eroded and crops out only in a narrow beltnear the coast. In the less tilted sectors the entiresuccession is largely preserved from erosion, and theSicilian and Crotonian deposits crop out 40–50 km fromthe coast (Fig. 4). During the Middle to Late Pleisto-cene, the Periadriatic belt assumed its present daymorphostructural pattern (Fig. 5d). This is mainlycharacterized by parallel drainage perpendicular to theApennine trend (NNW-SSE) and superimposed on thetransverse structural elements (Bigi et al., 1996, 1997a, b,1999a; Nisio, 1997; Nisio et al., 1999; D’Agostino et al.,2001; Centamore et al., 2002) (Fig. 4). The drainagenetwork was tightly controlled by Pleistocene tectonics.Later drainage pattern modifications such as rivercaptures and divide migrations occurred partly duringa Middle Pleistocene stage, characterized by transtensivekinematics (Nisio, 1997; Bigi et al., 1997b, 1999b).

4. Discussion and conclusions

The Plio-Pleistocene evolutionary stages of theApennine axial chain can be correlated with those ofthe Periadriatic sector. In the Middle Pliocene thebeginning of the inner chain’s uplifting and emergenceis connected with the first tilting impulse, the onset oferosion and the transgressive phase affecting the westernborder of the Periadriatic basin (Fig. 5b).The sequences and the angular unconformities recog-

nized in the Periadriatic successions may be linked to thevarious Apennine chain uplift stages and to correlativetilting processes in the Periadriatic belt (Fig. 5b–d). Theformation and evolution of the Inner and the Coastal

ridge detached at the Messinian evaporites level, and theweak deformations of the Sicilian deposits, may beascribed to an eastward gravity sliding of the thin-skinned sedimentary cover, due to the tilting pulses(Fig. 5b–d). The large amount of coarse deposits at thebase of the Periadriatic basin sequences result from thestrong erosional processes affecting the inner chain, thatare very intense during the Villafranchian, as is indicatedby the remarkable thicknesses of the intermontanedepressions continental deposits and by those of thePeriadriatic successions. The development of the in-tramontane tectonic depressions in the axial part of thechain and the emplacement of widespread huge gravita-tional masses indicate that in the Lower Villafranchianthe first important and sharp stage of the extensional

tectonics, linked to an high rate uplift and accompaniedby the primer of intense seismic events, occurred(Figs. 3d and 5d).So, many different processes are observed in the same

interval in the Central-Northern Apennines:

(a) Extensional tectonics and an high uplift rateaffected the axial part of the Apennine chain, inwhich intramontane tectonic depressions formed.Active normal faulting and high seismologicalactivity are concentrated along the ridge crest; theyindicate an active crustal NE-SW extension.

(b) In the Periadriatic belt tilting processes, weakcompressive structures and a moderate late areobserved, accompanied by a moderate compres-sional seismicity activity, partly concentrated andmore intense along the two main buried ridges. Theearlier thrusts, the detachments and the east dippingnormal faults occurred in the Periadriatic sector arelinked to the gravity-sliding processes affecting theupper sedimentary cover.

The contemporaneous development of so differentprocesses along this Apenninic transept may be relatedto the effects of a long-wavelength doming, as Dramis(1993) postulated. Such a doming represents a lategeodynamic event, linked to the Tyrrhenian opening andfollowing, with the same eastward shifting, the Apenni-nic thrust-belt system. During the eastward buildingchain migration a progressive delamination and an E-directed gravity-sliding of blocks through E-dippinglow-angle normal faults are observed (Carmignani et al.,1994 and references therein; Keller et al., 1994; Finettiet al., 2001 and references therein). The high rate ofuplift and of extensional tectonics in the axial part of thechain, the tilting processes, with the joined gravitydetachments and thrusting, in the outer sector point outan higher swelling in the eastern limb of bulge, due arebounding effect for the block of the orogenic systemagainst the stable Adriatic foreland. According toseveral authors (Wezel, 1982; Locardi and Nicolich,1992; Luongo, 1992; D’Agostino et al., 2001), thebending of this long wavelength bulge may be due tomantle upwelling, and represents the most importantlate geodynamic event.

Acknowledgements

Work supported byMURST ex 40–60% (E. Centamore)financial grants. The authors gratefully acknowledgethe help of Prof. C. Ollier for the useful commentsand suggestions, and for the improvement of the Englishtext. Our heartfelt thanks to Dr. D. Rossi for his greatcare in work and picture editing.

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References

Barberi, R., Cavinato, G.P., 1993. Analisi sedimentologiche ed

evoluzione paleogeografica del settore meridionale del bacino di

Rieti. Studi Geologici Camerti, Special Volume 1993/1, 39–53.

Bigazzi, G., Bonadonna, F.P., Centamore, E., Leone, G., Mozzi, M.,

Nisio, S., Zanchetta, G., 2000. New radiometric dating of volcanic

ash layers in Periadriatic foredeep basin system. Paleogeography,

Paleoclimatology, Paleoecology 155, 327–340.

Bigi, S., Cantalamessa, G., Centamore, E., Didaskalou, P., Dramis, F.,

Farabollini, P., Invernizzi, C., Micarelli, A., Nisio, S., Pambianchi,

G., Potetti, M., 1996. La fascia periadriatica marchigiano-

abruzzese dal Pliocene medio ai tempi attuali: evoluzione tettonico

sedimentaria e geomorfologica. Studi Geologici Camerti. Geodi-

namica e tettonica attiva del sistema Tirreno-Adriatico (special

volume) 1995/1, 37–49.

Bigi, S., Cantalamessa, G., Centamore, E., Didaskalou, P., Micarelli,

A., Nisio, S., Pennesi, T., Potetti, M., 1997a. The periadriatic basin

(Marche-Abruzzi sector, central Italy) during the Plio-Pleistocene.

Giornale di Geologia, Ser., 31 59 (1–2), 245–259.

Bigi, S., Centamore, E., Nisio, S., 1997b. Elementi di tettonica

quaternaria nella fascia pedeappenninica marchigiano-abruzzese. Il

Quaternario 10 (2), 359–362.

Bigi, S., Centamore, E., Fumanti, F., Milli, S., Nisio, S., 1999a. Aspetti

geologico strutturali delle ‘‘aree di avanpaese’’ nell’Appennino

centro-orientale. Studi Geologici Camerti 14 (1996/97), 201–209.

Bigi, S., Centamore, E., Nisio, S., 1999b. Caratteri geologico-

strutturali dell’area pedeappenninica marchigiano-abruzzese dur-

ante il Pleistocene. Studi Geologici Camerti 14 (1996/97), 193–200.

Bosi, V., Funiciello, R., Montone, P., 1994. Fault inversion: an

example in central Apennines. Il Quaternario 7 (2), 577–588.

Carmignani, L., Decandia, F.A., Fantozzi, P.L., Lazzarotto, A.,

Liotta, D., Meccheri, D., 1994. Tertiary extensional tectonics in

Tuscany (Northern Apennines, Italy). Tectonophysics 238,

295–315.

Centamore, E., Micarelli, A., 1991. Stratigrafia. In: Regione Marche

(ed.): ‘‘L’ambiente fisico delle Marche’’. S.E.L.C.A., Firenze, 5–58.

Centamore, E., Nisio, S., 2002. Quaternary morfodinamics between

the Velino and Salto Valleys. International Workshop on Large-

scale Vertical Movements and Related Gravitational Processes.

Rome-Camerino, June 21–26, 1999, Studi Geologici Camerti

(special issue) 2002(1), 41–53.

Centamore, E., Fumanti, F., Nisio, S., 2002. The Central-Northern

Apennines geological evolution from Triassic to Neogene time.

Bollettino Societ"a Geologica Italiana (special volume) 1 (2001),

1–17.

Centamore, E., Nisio, S., Prestininzi, A., Scarascia Mugnozza, G.,

1999. Evoluzione morfodinamica e fenomeni franosi nel settore

periadriatico dell’Abruzzo settentrionale. Studi Geologici Camerti

14 (1996/97), 9–28.

Centamore, E., Nisio, S., Sabatinelli, A., in press. Nuovi dati

sull’assetto geologico-strutturale e morfotettonico della zona

d’incontro. Lazio Nord-Orientale (Ri). Bollettino Servizio Geolo-

gico d’Italia 68.

Ciccacci, S., D’Alessandro, L., Dramis, F., Fredi, P., Lupia Palmieri,

E., Pambianchi, G., 1989. Studio geomorfologico del comprensorio

di Valleremita (Appennino umbro-marchigiano settentrionale.

Studi Geologici Camerti 11, 49–65.

D’Agostino, N., Jackson, J.A., Dramis, F., Funiciello, R., 2001.

Interactions between mantle upwelling, drainage evolution and

active normal faulting: an example from the central Apennines

(Italy). Geophysical Journal International 147, 475–497.

Demangeot, J., 1965. G!eomorphologie des Abruzzes Adriatiques.

Centre Recherche et Documentation Cartographique. Memoires et

Documents, CNRS, Paris, 403pp.

Dramis, F., 1993. Il ruolo dei sollevamenti tettonici a largo raggio nella

genesi del rilievo appenninico. Studi Geologici Camerti (special

volume) (1992/1), 9–15.

Faccenna, C., Florindo, F., Funiciello, R., Lombardi, S., 1993.

Tectonic setting and sinkhole features: case histories from western

central Italy. Quaternary Proceedings 3, 47–56.

Farabollini, P., Nisio, S., 1996. Evoluzione geomorfologica quaternar-

ia del bacino del F. Vomano. Il Quaternario 10 (1), 101–104.

Finetti, I.R., Boccaletti, M., Bonini, M., Del Ben, A., Geletti, R.,

Pipan, M., Sani, F., 2001. Crustal section based on CROP seismic

data across the North Tyrrhenian–Northern Apennines-Adriatic

Sea. Tectonophysics 343, 135–163.

Keller, J.V.A., Minelli, G., Pialli, G., 1994. Anatomy of late orogenic

extension: the northern Apennines case. Tectonophysics 238,

275–294.

Locardi, E., Nicolich, R., 1992. Geodinamica del Tirreno e dell’Ap-

pennino centro-meridionale: La nuova carta della moho. Memorie

Societ"a Geologica Italiana 41, ;121–140.

Luongo, G., 1992. Tettonica Globale dell’Italia meridionale: Sub-

duzione o bending. Memorie Societ"a Geologica Italiana 41,

121–140.

Nisio, S., 1997. Evoluzione geologica e morfotettonica dell’area

compresa tra il Gran Sasso ed il Mare Adriatico. Geologica

Romana 33, 13–27.

Nisio, S., Prestininzi, A., Scarascia Mugnozza, G., 1999. I calanchi del

settore settentrionale della fascia periadriatica abruzzese: Quadro

morfotettonico e loro caratterizzazione. Studi Geologici Camerti

14 (1996/97), 29–46.

Ori, G.G., Serafini, G., Visentini, C., Ricci Lucchi, F., Casnedi, R.,

Colalongo, M.L., Mosna, S., 1991. The Plio-Pleistocene adriatic

foredeep (Marche and Abruzzo, Italy): an integrated approach to

surface and subsurface geology. Third E.A.P.G. Conference, Guide

Book, 83pp.

Wezel, F.C., 1982. The Tyrrhenian Sea: a rifted krikogenic-swell basin.

Memorie Societ"a Geologica Italiana 24, 531–568.

E. Centamore, S. Nisio / Quaternary International 101–102 (2003) 93–101 101