Quaternary International 101–102 (2003) 125–135

Early uplift history of the Abruzzi Apennines (central Italy): availablegeomorphological constraints

Fabrizio Galadini*, Paolo Messina, Biagio Giaccio, Andrea Sposato

CNR-Instituto di Ricerca sulla Tettonica Recente, Via del Fosso del Cavaliere 00133 Roma, Italy

Abstract

Remants of a flat paleolandscape of erosional origin (top paleolandscape, TPL) have been detected in the Abruzzi Apennines

(central Italy) at high elevations (1350–1500m a.s.l.). According to current views, the TPL formation occurred at an elevation close

to sea level, and probably marks the first significant geomorphic event in the investigated sector. Since this erosional paleolandscape

affects an already deformed pre-Pliocene marine substratum and different structural units, its formation occurred after the thrust-

faulting phase, which affected the investigated area. The present elevation of the TPL remnants indicates a significant uplift

following the formation of this geomorphic feature. This uplift began during the Pliocene (age of the first post-thrusting continental

deposits, subsequent or sub-contemporaneous to the TPL and related to the formation of intermontane basins). Pliocene deposits

have been found in the Turano, Salto, and Fucino basins. The origin of these basins was conditioned by the activity of normal faults,

which affected and displaced the TPL during the Pliocene. Considering (1) that the TPL experienced uplift since the Pliocene and

(2) that after the beginning of the uplift phase it was displaced during the Pliocene by the faults responsible for the evolution of the

mentioned basins, uplift of the Apennine chain and normal faulting are closely related. The analysis of the mentioned basins

permitted to hypothesise a succession of Pliocene–early Pleistocene geomorphic and tectonic events: (1) Pliocene formation of the

TPL at low elevation a.s.l.; (2) beginning of the uplift and displacement of the TPL due to the activity of normal faults; (3) formation

of the Turano, Salto, and Fucino Pliocene basins; (4) fault activity responsible for the displacement of the Pliocene deposits;

(5) erosional phase affecting all the investigated basins; (6) deposition of the Early Pleistocene units.

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1. Introduction

The definition of the complex geodynamic processeswhich have been responsible for the formation of theItalian peninsula has benefited from data and hypoth-eses from different earth science branches, e.g. geo-kinematics, petrography, marine geology, geophysics,geodesy, seismology (e.g. Boccaletti et al., 1982; Pataccaet al., 1990; Doglioni, 1991; Serri et al., 1993; Amatoet al., 1993; Bartole, 1995; Bernabini et al., 1996;Faccenna et al., 1996; Mantovani et al., 1996) and fromnumerical modelling (e.g. Carminati et al., 1999).During the 1980s, geomorphologists and quaternaristsprovided a large amount of regional data (constraininggeodynamic models) which were summarised in theNeotectonic Map of Italy (CNR-PFG, 1987) and in anumber of papers focusing on regional uplift and Plio-Quaternary faulting (e.g. Aprile et al., 1979; Centamore

et al., 1980; Ambrosetti et al., 1982; Bartolini et al.,1982). After this period and for almost a decade, thecontributions of the geomorphology to define regionalconstraints for the geodynamic history were definitelyless numerous.

More recently, the geomorphological perspective hasgained new ground and traditional or quantitativegeomorphological approaches have been used mainlyin works focusing on the tectonic processes which havebeen responsible for the formation of mountain chains(Argnani et al., 1997; Calamita et al., 1999; Bartolini,1999; Coltorti and Pieruccini, 2000; D’Agostino et al.,2001). Following this new approach, the present paperreports and discusses the geomorphological data whichcan constrain the Pliocene–Early Quaternary tectonicevolution (uplift and faulting) of the Abruzzi Apennines(central Italy), through the analysis of three intermon-tane basins (Turano and Salto valleys, Fucino plain).The geological evolution of the basins will be proposedin specific sections followed by the description of theavailable continental stratigraphic framework. The

*Corresponding author.

E-mail address: galad@irtr.rm.cnr.it (F. Galadini).

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PII: S 1 0 4 0 - 6 1 8 2 ( 0 2 ) 0 0 0 9 5 - 2

regional tectonic implications which may be derivedfrom the basin tectonic histories will be summarised.Moreover, the characteristics of the top paleolandscape(TPL) (an uplifted old landscape which originated byareal erosion involving large portions of the AbruzziApennines) and the tectonic constraints which can bederived from this geomorphic feature will be discussed.Finally, a succession of geomorphic, depositional, andtectonic events will be proposed, together with somegeodynamic implications.

2. Geological framework

The structure of the central Apennines results from thesuperimposition of the extensional tectonics to thecompressive one since the Late Cenozoic. The latter isdue to the progressive NE migration of the Apennine arcrelated to the flexural retreat of the lithosphere platelocated in the Adriatic Sea (e.g. Malinverno and Ryan,1986; Royden et al., 1987; Patacca et al., 1990; Doglioni,1991). The contemporaneous opening of the Tyrrhenianbasin is due to rifting processes west of the presentApennine chain (e.g. Faccenna et al., 1996). Whilecompressive structures affected the progressively migrating

Apennine front and rifting occurred in the Tyrrhenianarea, extensional tectonics affected the Apennine chain(e.g. Meletti et al., 1995; Doglioni, 1995). Normal faulting(Fig. 1) is evident in the displacement of the Pliocene-Quaternary continental sediments (e.g. CNR-PFG, 1987).Pliocene deposits testify to the emersion of the investigatedApennine sector from the sea.

The present landscape of the Abruzzi Apenninesconsists of alternating NW–SE ridges (with peaks atmore than 2000m a.s.l.) and valleys (Fig. 1A). Theformer are generally carved into the Meso-Cenozoiccarbonate substratum, while the latter generally affectthe Miocene flysch. Plio-Quaternary continental deposi-tion occurred in the numerous normal-fault-boundedintermontane basins. In the following sections, adescription of some basins of the central-westernAbruzzi Apennines will be presented.

3. Turano valley

The middle Turano valley was a lacustrine basinduring the Pliocene (Bosi, 1989). Its evolution wasconditioned by the activity of the normal fault locatedalong the NE flank of the valley (Melchiorri, 1987). The

Fig. 1. (A) Main Quaternary faults of the Abruzzi Apennines; the remnants of the TPL mentioned in the text are encircled by white lines; (B) main

Quaternary normal faults and Plio-Quaternary basins of the investigated area; the limit of the Fucino Plain follows the border of the Holocene lake;

Legends: SVF—Salto valley fault; TVF—Turano valley fault; DMF—Duchessa Mts. fault; MVF—Mt. Velino fault; TMF—Tre Monti fault;

SVF—San Vittorino fault; MHF—Marsicana highway fault; SBGF—San Benedetto dei Marsi-Gioia dei Marsi fault; TF—Trasacco fault;

LVF—Liri valley fault; VLF—Vallelonga fault.

F. Galadini et al. / Quaternary International 101–102 (2003) 125–135126

oldest deposition in the Turano valley (first unit, ‘‘SantaCroce’’) consists of sandy-silty deposits with sparsearenaceous and carbonate pebbles, which turn toconglomerates (with arenaceous pebbles more abundantthan the carbonate ones) alternating with sands and silts(Fig. 2A). The presence of blocks (larger than 1m3)(both calcareous and arenaceous) along the NE flank ofthe Turano valley indicates that this slope was affected

by instability during the deposition of the Santa Croceunit. The beginning of the deposition more clearlyconditioned by the presence of carbonate slopes(therefore marking the formation of a more indentedlandscape) is indicated by slope-derived breccias con-formably covering the mainly silico-clastic deposits. Thedescribed succession (more than 200m thick) is entirelytilted towards N or NE (Fig. 2A) as the result of the

Fig. 2. Pliocene-Early Pleistocene deposits in the investigated area: (A) Tilted Pliocene sands and silts in the Turano valley (the road is horizontal);

(B) slope-derived breccias of the second unit (Early Pleistocene) in the Turano valley; (C) detail of the sedimentologic characteristics of the breccias

showed in B; (D) Pliocene lacustrine succession in the Salto valley; note the Salto valley fault (see also Fig. 1B) in the background (indicated by the

arrows) and the NE high-dipping attitude of the lacustrine deposits (inset); (E) arenaceous blocks within the middle portion of the Pliocene

succession in the Salto valley; (F) view of huge carbonate blocks within the Pliocene deposits of the Fucino basin; the entire village of Aielli was built

over one of these blocks.

F. Galadini et al. / Quaternary International 101–102 (2003) 125–135 127

activity of the fault bordering the Turano valley to theNE (Fig. 1).

A clear unconformity separates the first unit from thesecond one (‘‘Le Grotte’’), i.e. from layered slope-derivedbreccias (Fig. 2B), made of angular-to-sub-roundedcarbonate pebbles usually in pink-orange matrix(Fig. 2C), sometimes characterised by an open-worktexture. These deposits are dipping towards SW andseveral tens of metres thick.

4. Salto valley

During the Pliocene and the Quaternary, a basinaffected by continental deposition developed in the SaltoValley (Bosi et al., 1989). The evolution of the basin wasconditioned by a fault (with mainly normal movements)located along the NE flank of the valley (Figs. 1 and 2D;Bosi, 1975; Mariotti and Capotorti, 1988; Morewoodand Roberts, 2000; Galadini and Messina, 2001).

The beginning of the continental deposition (first unit,‘‘Piagge’’) is indicated by a succession of fine sands withalternating levels of gravels (Bertini and Bosi, 1976;Bertini et al., 1986; Bosi et al., 1989). Similar to thesuccession described for the Turano valley, the presenceof carbonate pebbles within the coarse beds increasesupward. Arenaceous blocks in sandy matrix have beenfound in the middle part of the succession (Fig. 2E),while carbonate blocks of several cubic metres have beenobserved in the upper part. Also in this case the presenceof the blocks indicates a deposition close to unstableslopes feeding landslides. The first unit is outcroppingfor at least 300m and is generally dipping towards NEdue to the activity of the fault bordering the depressionto the NE (Fig. 2D).

The second unit (‘‘Canalicchio’’) mainly consists ofcarbonate gravels; some horizons consist of arenaceousboulders and carbonate pebbles in a sandy matrix (Bosiet al., 1989). Similarly to the first unit, also theCanalicchio unit displays some horizons (‘‘Strati diConcerviano’’ and ‘‘Strati di Rocca Ranieri’’ in Bosiet al., 1989) consisting of huge (mainly carbonate, butalso arenaceous) blocks indicating instability of theslopes adjacent to the depositional area. Slope-derivedcarbonate breccias are also part of this unit. Thesedeposits have the classical facies already described forthe Turano valley. The Canalicchio unit is outcroppingfor about 150m.

5. Fucino basin

The Fucino basin is the largest intermontane basin ofthe Apennines, bounded to the east and north by anormal fault system (Fig. 1) which was responsible forthe formation of a half-graben since the Pliocene

(Galadini and Messina, 1994). The beginning of thecontinental deposition (first unit, ‘‘Aielli’’) is indicatedby lacustrine sands and clays which originated from theMiocene flysch (Bosi et al., 1995; Cavinato et al., 2002).The middle–upper part of the succession is characterisedby the increasing presence of carbonate clasts. As in thepreviously described basins, horizons with carbonateblocks have been identified. In particular, along thenorthern border of the basin, huge carbonate blocks(hundreds of m3) within a clayey-sandy matrix havebeen found (Fig. 2F; Bosi et al., 1995). The upper part ofthe Aielli unit consists of carbonate gravels in sandymatrix. The thickness of the outcropping deposits,which may be related to the Aielli unit is about 400m.

A subsequent erosional phase is indicated by a flaterosional surface carved into the Aielli unit (Bosi et al.,1995). The second unit (‘‘Cupoli’’) deposited at lowerelevations, after the formation of the erosional surface.It is mainly made of carbonate gravels, alternating withsilty-sandy horizons, related to fluvial and lacustrineenvironments (Bosi et al., 1995). The basin borders havebeen affected by the deposition of the slope-derivedbreccias already described for the Turano and Saltobasins. The thickness of the outcropping deposits, whichmay be related to the Cupoli unit is about 120m in theNE sector of the basin.

Both units are evidently affected by the activity of thefaults bordering the basin (Galadini and Messina, 1994).Data reported in the mentioned work indicate that faultactivity has been persistent since the deposition of thefirst unit. An evident unconformity marks, indeed, thelimit between the deposits of the Aielli and theCupoli units along the N and NE basin border andwhile the former unit is tilted northward, the lattermaintain a subhorizontal attitude (Galadini andMessina, 1994).

6. Correlation of the Pliocene–Early Pleistocene

continental successions

Data on the Plio-Quaternary continental stratigraphyof the Abruzzi Apennines can be derived from thenumerous works dedicated to the neotectonics or to thegeological evolution of intermontane basins (Deman-geot, 1965; Bosi and Bertini, 1970; Raffy, 1970, 1982;Bertini and Bosi, 1976, 1993; Bertini et al., 1986;Zarlenga, 1987; Bagnaia et al., 1989; Bosi and Messina,1990; Galadini and Messina, 1993; Bosi et al., 1995;Cavinato and Miccadei, 1995; Giuliani and Sposato,1995; Miccadei et al., 1997, 1998; Ciccacci et al., 1999).Few works summarised, however, the available data atthe regional scale through the correlation of thestratigraphic successions of different intermontanebasins (Bosi, 1989; Bosi and Messina, 1991). We followthe correlations proposed by Bosi and Messina (1991),

F. Galadini et al. / Quaternary International 101–102 (2003) 125–135128

enriched by new data on the stratigraphy of the Turanovalley (see Section 3) and on the paleomagneticallyinferred age for the slope-derived breccias of theyoungest unit (D’Agostino et al., 1997; Messina et al.,2001) (Fig. 3).

Due to the lack or scarcity of direct chronologicalconstraints (see the discussion in Bosi, 1989; Bosi andMessina, 1991; Galadini, 1999), the chronology of thetwo units reported in Fig. 2 was derived on the basis ofindirect evidence. As for the youngest (second) unit, theEarly Pleistocene age has been defined by consideringthat (1) slope-derived breccias, for which paleomagneticdata indicate an age older than the Bruhnes–Matuyamalimit (D’Agostino et al., 1997; Messina et al., 2001), arepresent in each of the investigated successions; (2) thedeposition clearly preceded the younger units charac-terised by a high content of volcanic minerals (related tothe Middle Pleistocene volcanic activity in central Italy;Fornaseri (1985) and Barbieri et al. (in press)); (3) thedeposition occurred a very long time after that of theoldest unit (see points 4 and 5 below).

The definition of the chronology of the oldest (first)unit is even more difficult. The lack of direct chron-ological constraints only permit this unit to be assignedto a generic Pliocene, without further specification. Thequalitative bases for the chronological attribution are:(1) this unit is clearly younger than the Messiniancontinental deposits involved in the compressionalApennine deformations (Bosi and Messina, 1990;Cipollari et al., 1999); (2) a clear unconformity separatesthe first unit from the underlying marine Miocenesubstratum (e.g. Bertini and Bosi, 1976); (3) clasts withinthis unit sometimes originated from areas not related tothe present physiography, while the abundance (in thelower part of the first unit) of clayey-sandy depositsindicates that the deposition was fed from areas entirelymade of Miocene flysch (the Quaternary deposition is,instead, entirely conditioned by the presence of thecarbonate bedrock suggesting a physiography similar tothe present one); (4) an extended erosional surface iscarved into these deposits and formed before the deposi-tion of the second unit deposits; (5) an unconformity

Fig. 3. Stratigraphic units in the investigated area.

F. Galadini et al. / Quaternary International 101–102 (2003) 125–135 129

separates the first unit (strongly deformed and displacedalong normal faults) from the second unit; and (6) thelacustrine deposits related to the first unit are char-acterised by a huge thickness (more than 300m ofoutcropping deposits in the Salto valley and the Fucinobasin). Point 3 indicates a physiography of thepaleobasins significantly different from that of thesecond unit and therefore suggests that a long timespan has passed between the deposition of the first andthe second units. A similar conclusion may be drawn onthe basis of points 4 and 5. Point 6 indicates that thedeposition of the first unit may have lasted for a longtime. Moreover, the geological evolution of the last1Ma in the investigated area, as derived from works atthe scale of the single basin (e.g. Bosi et al., 1989, 1995),indicates that physiographic changes in the investigatedarea are definitely less evident than those related to theperiod during which the first and second units deposited.Assuming that the rates of landscape modification arenot significantly changed during the entire continentalhistory of the investigated sector, this indicates that thetime span of the geological history defined by the firstand second units is longer than that related to thegeological evolution of the investigated area in theperiod following the deposition of the second unit.

All the reported points qualitatively support, in ouropinion, a Pliocene age for the first unit. On the basis ofpoint 6 it is not possible to exclude, however, that partof the deposition occurred during the Early Pleistocene.

7. Some constraints for the tectonic activity and the

geological evolution

The implications of the distribution, sedimentologiccharacteristics and deformation of the oldest depositsdetected in the Turano, Salto, and Fucino basins arereported below:

(1) The huge thickness of the Pliocene successions(sandy-clayey portions, i.e. persisting lacustrinefacies without evidence of a shallowing upwardenvironment; e.g. Einsele, 2000) indicates thatdeposition occurred in subsiding basins.

(2) The presence of landslide deposits within thePliocene succession suggests that the depositionwas conditioned by an increasing amplitude of reliefalong the basin borders; this conclusion is sup-ported by the increase of carbonate clasts, indicat-ing the formation of a more dissected landscape inthe basin areas (also carved into the carbonatesubstratum and not only into the Miocene flysch).

(3) The presence of landslide deposits within thePliocene succession, close to the slopes presentlybordering the basins, indicates a coincidencebetween some Pliocene and Quaternary slopes, i.e.

the coincidence of the Pliocene and the Quaternarybasinal areas.

(4) The presence of the landslide deposits along theslopes, which are affected by the faults borderingthe basins (N and NE basin flanks) indicates thatthe available relief has a probable tectonic compo-nent.

(5) The unconformities between the deposits of the firstand second units indicate that the faults borderingthe basins were active also during the Pliocene; thePliocene deposits are, indeed, significantly tilted (upto 501) towards N and NE, while the EarlyPleistocene deposits are generally slightly tilted orapparently untilted.

8. The top paleolandscape

Although investigations and discussions on thepresence of some old, uplifted erosional landscapes inthe Apennines started many decades ago (Sawicki, 1909;Castiglioni, 1934; Demangeot, 1965), the more recentliterature indicates that the interest in these geomorphicfeatures has not declined, particularly in studiesdedicated to neotectonics (Bosi, 1978; Boenzi, 1979;Marchetti et al., 1979; Bartolini, 1980, 1999; Sestini,1981; Nesci et al., 1982; Calamita et al., 1982, 1999;Ciccacci et al., 1985; Cinque, 1992; Dramis, 1992; Bosiet al., 1996; Coltorti and Pieruccini, 1997, 2000; Amatoand Cinque, 1999; Basili et al., 1999).

We have recently made investigations on the Aqui-lente, Anzano and Mt. Marine top paleolandscape (TPLin the next; Figs. 1 and 4) remnants. These featuresdisplay geomorphic characteristics already described inother parts of the world and typical of complexerosional landscapes (P!ecsi, 1970; Ollier, 1993; Fother-gill and Ma, 1999; Coltorti and Ollier, 1999). Since thepresence of extended TPL remnants with the samegeomorphic characteristics and located at the sameelevation in a relatively small area cannot be accidental,we believe that the formation of the Aquilente, Anzanoand Mt. Marine TPLs is the probable result of asynchronous erosional process acting in the investigatedApennine sector.

In the three above-mentioned areas, the TPL displaysthe following characteristics: (1) it is entirely carved intothe deformed marine substratum; (2) it is flat andsubhorizontal over large areas (hundreds of km2); (3) itis located at elevations ranging from 1350 to 1500ma.s.l.; (4) it is clearly suspended over the present valleybottoms (sometimes located more than 1000m belowthe TPL). Each of the reported points has an importantimplication: (1) the TPL formed after the thrust phase inthe investigated sector (see also Calamita et al., 1999;Coltorti and Pieruccini, 1997, 2000); (2) the TPL formed

F. Galadini et al. / Quaternary International 101–102 (2003) 125–135130

during a period of stable regional base level, i.e. theformation occurred close to the sea level (see alsoSestini, 1981and Bartolini, 1999); (3), (4) the TPLexperienced a significant uplift (e.g. Sestini, 1981;Dramis, 1992; Bartolini, 1999) and it did not form inrecent times (see below).

The formation of the TPL in the Abruzzi Apennineshas been related to the Pliocene (Bosi, 1989; Bosi andMessina, 1991). According to these authors, the TPLformed after the deposition of the first unit in thedifferent basins. However, recent investigations per-mitted us to hypothesise that the TPL may have formedbefore or contemporaneously to the earliest depositionof the first unit. As reported in the previous section, thepresence of landslide deposits within the Pliocene unitsindicates significant available relief at the basin borders,while the huge thickness of the lacustrine depositsindicates subsidence over a long time span. All thesefactors suggest that, at the end of the first unitdeposition, the physiography was already dissectedand sectors of the Abruzzi Apennines have alreadyexperienced significant vertical movements. The forma-tion of an extended and flat erosional landscape in suchconditions seems improbable.

Moreover, the Aquilente TPL and the Salto basin areseparated by the slope affected by the NW–SE faultwhich was active during the Pliocene (see previoussection) and has been responsible for the basin evolution(Fig. 1). The characteristics of the Pliocene deposits

(indicating the growing of the NE Salto basin slope), theevidence of Pliocene activity along the fault borderingthe basin and the position of the Aquilente TPL in thefootwall of the fault suggest that the Pliocene basinformed as the result of the displacement of the AquilenteTPL.

The hypothesis of the TPL formation after the firstunit deposits implies the planation of a dissectedPliocene landscape (with mountain slopes feeding land-slide deposits and deep Pliocene continental basins) overa very long time span. During this time interval, thepreviously active fault bordering the Pliocene Saltobasin was affected by minor activity or was quiescent.The same fault previously dormant should havebeen responsible, during the Quaternary, for thedisplacement of the Aquilente TPL and for theformation of a new basin in the same area of thePliocene basin. This complex succession of eventsseems less reliable, since significant phases of tectonicstability consistent with this geological evolutionare not documented from the kinematic studies onthe Pliocene building of the Apennine chain (e.g.,Patacca et al., 1990).

These considerations indicate that the TPL probablyformed during the Pliocene and imply that it is theoldest geomorphic feature of the investigated area. Thelatter conclusion was already drawn for the Umbria–Marche sector of the central Apennines by Dramis(1992).

Fig. 4. Panoramic views of remnants of the TPL in the Abruzzi Apennines (see Fig. 1A for location): (A) Aquilente TPL; the arrows indicate the area

where the erosional landscape affects tilted carbonate layers; (B) Mt. Marine TPL (black arrows); the white arrows indicate the base of the fault scarp

bordering the upper Aterno valley; (C) Anzano TPL; note the suspended position of the landscape over the more recent valleys (background);

(D) Anzano TPL; some incisions (headward truncated) affect a gentle slope.

F. Galadini et al. / Quaternary International 101–102 (2003) 125–135 131

9. Uplift and tectonic activity: a possible succession of

events

As reported in the section dedicated to the TPL, thepresence of remnants of this geomorphic feature at highelevations (1350–1500m) indicates that a significantuplift (about 1000m) affected the central Apenninessince the Pliocene (age of the post-thrusting continentaldeposition and of the emersion from the sea water of theinvestigated area), assuming that the TPL formationoccurred at few hundred metres a.s.l. Considering thatthe Pliocene basin formation is the effect of thedisplacement of the uplifting TPL, uplift and faultingseems to be closely related.

On the basis of the available data, Pliocene–EarlyPleistocene geomorphic, depositional and tectonic eventscan be summarised as follows (Fig. 5): (1) formation

(during the Pliocene) of the TPL at low elevation a.s.l.,as a result of erosional phenomena acting over largeareas; (2) displacement of the TPL (contemporaneous toits uplift) due to the activity of normal faults and indi-cated by the nucleation of the Pliocene basins and by thedeposition of the first unit lacustrine sediments; (3)deposition of the entire first unit in the Turano, Saltoand Fucino basins; (4) fault activity responsible for thedisplacement of the first unit deposits; (5) erosionalphase affecting all the investigated basins; (6) depositionof the second unit. Uplift is continuing through theevents 3–6.

Based on point 2, the uplift seems to be the maincause of the normal faulting in the Apennines. Therelationship between uplift and normal faulting, alreadypointed out in other works (e.g. Doglioni, 1995;D’Agostino et al. 2001), is therefore also indicated bythe available data on the Pliocene-Early Pleistocenecontinental evolution of the Abruzzi Apennines.

10. Conclusions

Available stratigraphic and geomorphologic datahave permitted to make new hypotheses on thePliocene-Early Pleistocene history of the uplift andnormal faulting in the Abruzzi Apennines (central Italy)and on the relationship between the two phenomena.Stratigraphic data indicate that the intermontanebasins have formed since the Pliocene. The basinevolution has been conditioned by the activity of faultswhich were responsible for the formation of a dissectedlandscape affected by deep basins and mountain slopeswhich fed landslide deposits. This Plio-Quaternarylandscape resulted from the displacement of an olderpaleolandscape (TPL), whose origin may be relatedto erosional processes occurred at an elevation close tothe sea level, subsequent to the thrust phase in theinvestigated area. The presence of remnants ofthe TPL at high elevation (1350–1500m a.s.l.) indicatesa significant uplift (about 1000m) since the Pliocene (ageof the first post-thrusting continental deposition). ThePliocene basin formation as a result of the TPLdisplacement and its synchroneity with the AbruzziApennine uplift (after the TPL formation) suggest adirect relationship between the two phenomena. Inparticular, uplift is the probable main cause of normalfaulting.

Acknowledgements

We are grateful to F. Dramis (University of RomaTre) and A. Pizzi (University of Chieti) for productivediscussions on the top paleolandscape and on thePlio-Quaternary tectonic history of the Apennines. We

Fig. 5. Schematic (not to scale) Pliocene–Early Pleistocene tectonic

history of the western Abruzzi Apennines: (A) Formation of the TPL

over the deformed marine substratum; (B) beginning of an intense

uplift phase; displacement of the TPL by normal faults and nucleation

of Pliocene continental basins; (C) evolution of a Pliocene continental

basin and deposition of the presently tilted lacustrine sediments; (D)

displacement of the Pliocene deposits; (E) erosional phase affecting the

deposits; (F) deposition of the Early Pleistocene sediments.

F. Galadini et al. / Quaternary International 101–102 (2003) 125–135132

are also grateful to E. Gallo (CNR, Area di Ricerca diRoma-Tor Vergata, Roma) for her help with biblio-graphic research.

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