Late Quaternary environmental evolution of the intermontane basin, southern

Micla Pennetta, Filippo Russo & Carlo Donadio

Rendiconti Lincei SCIENZE FISICHE E NATURALI

ISSN 2037-4631 Volume 25 Supplement 2

Rend. Fis. Acc. Lincei (2014) 25:231-240 DOI 10.1007/s12210-014-0334-9

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Rend. Fis. Acc. Lincei (2014) 25 (Suppl 2):S231–S240 DOI 10.1007/s12210-014-0334-9

INTERMONTANE BASINS IN CENTRAL-SOUTHERN ITALY

Late Quaternary environmental evolution of the intermontane Valle Caudina basin, southern Italy

Micla Pennetta • Filippo Russo • Carlo Donadio

Received: 20 December 2013 / Accepted: 5 September 2014 / Published online: 25 September 2014 Ó Accademia Nazionale dei Lincei 2014

Abstract The Valle Caudina intermontane basin in the suffered a substantial downsizing or has disappeared southern Apennines (Italy) lies between the Mt. Taburno on between 5 kyr BP and the Roman Age. A clayey deposit the North and the Avella–Partenio mountains on the South. testifies a first lacustrine phase, which has affected the whole An analysis of its present-day landscape, and of its strati- plain. Above this unit, heterogeneous deposits indicate the graphic and geoarcheological features, has been carried out end of the lacustrine phase and the beginning of a clear fluvial to reconstruct the Late Quaternary evolution of the basin, sedimentation. Volcaniclastic deposits from the erosion of filled by alluvial, colluvial and volcaniclastic deposits. The the Campanian Ignimbrite follow. They are overlapped by a depositional pattern and geomorphological context allow to widespread second lacustrine unit. Finally, a reworked and recognize lacustrine and fluvial–lacustrine sediments, int- altered volcaniclastic level closes the stratigraphic sequence, erbedded with ignimbritic layers originating from the while particularly fertile topsoil covered all the plain. Phlegrean Fields and with a Vesuvius pumice level, that represent significant chronological markers. The two lacus- Keywords Geomorphology Á Intermontane basins Á trine episodes are connected with volcanic events radio- Quaternary Á Southern Apennines Á Italy metrically dated (De Vivo et al. in Mt. Somma Vesuvius and Volcanism of the Plain. Spec Issue, Mineral Pet- rol. Springer, Berlin, vol 73, pp 47–65, 2001). The older 1 Introduction predates the Campanian Ignimbrite deposit (*39 kyr BP), while the younger deposited before 5 kyr BP, as indicated by The intermontane basins are significative elements to the recovery of Neolithic artifacts. The presence of Roman understand the late geological and morphological phases of ruins in the center of the valley suggests that the lake has mountain chains evolution (Pizzi et al. 2002; Rodrı´guez- Ferna´ndez and Sanz de Galdeano 2006; Pedrera et al. 2010). In the Apennines, these structures are expression of inherited This peer-reviewed article is part of a coordinated collection of scientific researches on the comparative evolution of intermontane landscapes mainly modeled under the Quaternary tectonic– basins of the central-southern Apennines. climatic conditions (Porreca and Mattei 2010; Zembo et al. 2012). The Valle Caudina basin discussed in the present M. Pennetta Á C. Donadio (&) paper (Fig. 1a) is located in a sector of the southern Apen- Department of Earth Sciences, Environment and Resources, nines where the deformation is strictly linked to the forma- University of Naples Federico II, Largo San Marcellino 10, 80123 Naples, Italy tion of the main thrust system referred to the Miocene e-mail: [email protected] compressional tectonic events (Burdigalian–Messinian). M. Pennetta Since the Late Pliocene, different extensional tectonic pha- e-mail: [email protected] ses have led to the partial collapse of the chain with formation of structurally depressed areas bounded by normal fault F. Russo systems. Early Pleistocene block-faulting evidences are well Department of Science and Technology, University of Sannio, 59/A Via dei Mulini, 82100 , Italy documented along the marginal slopes of these depressions. e-mail: fi[email protected] Generally, the subsequent erosion phases related to the uplift 123 Author's personal copy

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Fig. 1 Geological sketch of the Valle Caudina intermontane basin sandstone, silty sandstone and marl (Miocene); 11 polygenic breccias (after Abate et al. 1998): 1 fluvial–lacustrine sediments (Holocene); 2 (intercalated between Miocene and Cretaceous); 12 whitish dolomitic landslide deposits (Holocene); 3 clays and sandy clays (Pliocene); 4 limestone and well-cemented clastic limestones (Cenomanian–Ap- ignimbritic deposits (Late Pleistocene); 5 Phlegrean cinerites (Late tian); 13 clastic limestones (Neocomian–Lias); 14 well-cemented Pleistocene–Early Holocene); 6 incoherent debris deposits with clastic limestones (Lias); 15 fault: a exposed, b buried or presumed; (a) rare olistoliths (Pleistocene); 7 alluvial sediments and alluvial 16 limit of geological units; 17 altitudine (m a.s.l.), 18 drilling; 19 fans (Pleistocene); 8 slope breccia (Pliocene); 9 sands and yellowish trace of geological section sandstones (Pliocene); 10 terrigenous deposits in flysch facies: of the Apennine chain have produced the dismantling of the (Fig. 1b), bounded by NW–SE normal faults, developed region with accumulation of thick alluvial fan deposits. This during the Apennine extensional tectonic phases (D’Ar- extensional tectonics during the Middle Pleistocene led to genio 1967; Vezzani et al. 2010). This intermontane basin the formation of large half-grabens (Brancaccio and Cinque (Fig. 1) lies between the Mesozoic carbonate massifs of 1988), in which fluvial and lacustrine basins formed. Among Taburno to the North (Fig. 2) and Avella–Partenio to the these, there are the Caudina valley here discussed and the South. The carbonate relief of Mt. Taburno (D’Argenio adjacent Calore of Volturno River and Telese valleys, far 1967; Vallario 1973; Comentale 2010) consists of marine tens of kilometers to the Northwest of the studied area Triassic dolomite, Jurassic dolomitic limestone and Late (Magliulo 2005; Magliulo and Russo 2005; Magliulo et al. Cretaceous limestone. The sequence continues with trans- 2007). Other authors have attributed the origin of the above gressive Paleocene–Eocene limestones and marls, and intermontane basins to dextral transcurrent movements Early Miocene calcarenite beds. Also the carbonate reliefs along the NE–SW lineament of Valle Caudina–Benevento– of Mts. Avella–Partenio consist of Jurassic and Cretaceous Buonalbergo, and along the E–W faults of Faicchio–Cerreto limestone (D’Argenio et al. 1973; Bravi et al. 2006), par- Sannita–Pontelandolfo–Montefalcone and –Paup- tially covered by Tertiary terrigenous units. On both the isi (Ortolani et al. 1992). The Quaternary periglacial events massifs, Quaternary pyroclastic deposits locally outcrop in the southern Apennines have controlled the modeling of covering the bedrock units. The Avella–Partenio mountain the hillslopes, producing large volumes of debris which ridge, 20 km long and N120° striking, is bordered by a accumulated at the foothills of the mountains and in the thrust to the North and largely affected by high-angle tectonic depressions (Brancaccio et al. 1979). faults. In the eastern sector, a siliciclastic flysch outcrops, including large olistoliths emplaced during the Early Miocene orogenic phases. The continental basin fill con- 2 Geological outline sists of epiclastic Quaternary deposits, slope debris, allu- vial, lake and fluvial–lacustrine deposits. The Valle Caudina is a subtrapezoidal tectonic plain of The analysis of the subsurface stratigraphy from bore- about 40 km2 at an average elevation of 260 m a.s.l. holes and the detailed field surveys have allowed to

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Fig. 2 Main aspects of the discussed area in a NW–SE view (from the top of Mt. Taburno relief; 3 along-the-slope dissected rectilinear castle): 1 Valle Caudina depression: moderately and subparallel channels; 4 alluvial fans and ancient breccias, anthropized, it extends between the northern foot of Mts. Avella– cemented, fractured and karstified; 5 concave profile of the lower Partenio and the southern foot of Mt. Taburno, both Mesozoic slope probably representing the ancient base level of the depression, carbonate massifs; 2 a relic strip of leveled paleosurface preserved on dislocated during the Early-Middle Pleistocene

Fig. 3 Late Pleistocene breccias (B), with reverse grading of the debris flow–talus scree (in the box: grain-size coarsening upwards), mixed with pyroclastics and pyroclastic colluvium. This unit forms the basal detrital cover of the most recent fault scarps. In the higher part, a bench of yellowish pyroclastics (P), partially covered, outcrops. N–S view recognize, in addition to fluvial–lacustrine deposits, poorly remains of prehistoric pottery have been observed, both cemented slope breccias mixed with pyroclastics (Fig. 3), useful for a chronostratigraphic dating of the last lacustrine alluvial fan sediments mixed with slope-waste deposits, phases. In particular, this sequence starts with a well- ancient red breccias, yellow lithoid tuffs and argillified humified paleosol overlayed by levels of pumice, sand and volcaniclastics. Suspended on the Taburno and Avella– thinly laminated ash. On these levels, separated by an Partenio slopes, facing to the Valle Caudina depression, erosional unconformity, volcanic products related to the deformed coarse-grained breccia beds (Ancient Breccia Phlegrean ignimbrite are recognizable. At the top, small unit) outcrop. Their clasts, well cemented, originated by outcrops of volcaniclastics, formed by thin and highly the erosion and retreat of the carbonate slopes during the altered layers of pumice and lapilli, are present (Di Gi- Early Pleistocene. The silty–clayey deposits in fluvial– rolamo et al. 1984). These deposits cover yellow tuffs and lacustrine facies cover most of the studied area, from poorly lithified pyroclastics, both to the right and the left of , and Cervinara up to Montesarchio the Isclero River. (Fig. 1). These sediments are due to reworking and rede- position of pyroclastic deposits outcropping in the sur- rounding zones, originating from the Phlegrean Fields 3 Geomorphological features volcanic complex, about 45 km far from the studied area. Interbedded with these deposits, a Vesuvius pumice level The intermontane basin of Valle Caudina is a Pleistocene occurs (Avellino Pumices, *3.8 kyr BP; Lirer et al. 1973; tectonic depression showing a subtrapezoidal shape, with a Scandone et al. 1991; Mastrolorenzo et al. 2006) and maximum extension of about 8 km along the NW–SE axis 123 Author's personal copy

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Fig. 4 Geomorphological map of Valle Caudina: 1 contour line (m alluvial fan; 8 hanging valley; 9 polje; 10 fault scarp: (a) retreating, a.s.l.); 2 altitude (m a.s.l.); 3 watershed; 4 subsequent drainage; 5 limit (b) rejuvenated; 11 paleosurface: a summital, b downlifted; 2 of fluvial terrace; 6 fluvial terrace: (a) first and (b) second order; 7 landslide pile; 13 basin depocenter; 14 paleothreshold and 4 km along the NE–SW direction. The extension of the to hanging valleys, whose genesis is linked to tectonic area is *40 km2 with an average gradient of 0.35 % displacements that have truncated the pre-existing mor- (*0.2°) in the SE–NW direction, while it is subhorizontal phology. Remnants of ancient erosional land surfaces are along the SW–NE axis. The perimetral slopes show a present at the top of the main carbonate mountain ridges of gradient ranging from *18 % (10°) up to over 70 % the study area, with different elevations. Such landforms, ([35°) (Ceccarelli et al. 1999). shaped by denudational processes, are represented by strips The analysis of aerial photographs allowed the assem- of paleosurfaces at the top of the carbonate reliefs (*800/ blage of a geomorphological map (Fig. 4), which shows 1400 m a.s.l.) or lowered slopes (*500 m a.s.l.) and two contrasting morphologies: that of the steep Taburno delimited upwards by steep structural slopes (Cinque and Avella carbonate massifs that rise from the flat plain of 1992). Karst morphologies, both epigean (karstic fields, the Valle Caudina, and the rounded morphologies at the small polje) and rare underground (caves), characterize the Tertiary mostly terrigenous rocks that confine the valley to Mt. Taburno and Mts. Avella–Partenio landscapes and their the East. (D’Argenio 1967). The carbonate massifs are Quaternary breccias. Among the denudational forms of the characterized by structural landforms modified by sub- slopes there are occasional small rocky landslides (Vallario sequent drainage, mostly superimposed on faultlines, and 1973). 123 Author's personal copy

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Fig. 5 Fluvial terraces of first (1) and second (2) order modeled along a sinuous segment of the Isclero River, in the Northwest of the valley (Moiano), at the foot of Mt. Taburno. Strong changes of the river landscape occurred between b 1998 (Abate et al. 1998) and a 2013 (this article). NW–SE view

Fig. 6 Geological sections along the Valle Caudina basin. RP reworked and altered pyroclastics, AF alluvial fan deposit with rare The depositional and erosive forms are represented by travertine lenses, FD fluvial coarse debris, LII lacustrine II unit, GT alluvial fans and fluvial terraces, respectively (Figs. 4, 5). gray tuff, CI Campanian Ignimbrite, FL fluvial–lacustrine unit, LI The alluvial fans are exclusively at the base of the car- lacustrine I unit, AT Ancient Tuff, FS fluvial sands, BC Basal Clay, bonate slopes and consist mainly of volcaniclastics with MC Miocene–Pliocene clay, DL dolomitic limestone, open circle drilling number, solid circle intersection of geological cross-section characters of secondary deposition, due to the reworking of the cineritic cover (Di Girolamo 1968) on the down- lifted paleosurfaces of Mt. Partenio. Moreover, the allu- 4 Methodology vial fans of Mt. Taburno and Mt. Avella show the volcaniclastic component significantly subordinated to the The reconstruction of geomorphological evolution of Valle limestone–clastic one. The fluvial terraces are mainly Caudina intermontane basin has been carried out through the located along the northwestern foothills of the valley analysis of surface and subsurface geological data, as well as (Fig. 4). Among these, the second-order terrace is carved the study of aerial photographs. Topographic maps at in the ignimbritic deposit over 230 m height a.s.l., while 1:25,000 scale have been used for updating the previous the first-order ones are modeled in the alluvial sediments geomorphological map of Abate et al. (1998), while maps at of the Isclero River (Fig. 5). It is worth noting that in 1:10,000 scale were used for the interpretation of the flat both, the alluvial and ignimbritic deposits, thin inter- zones of the valley, in both cases with a GIS application bedded paleosols and lacustrine sediments are recogniz- (Ceccarelli et al. 1999). In particular, geomorphological able, reflecting oscillations in the morphoevolutionary surveys, sediment sampling and stratigraphic data interpre- processes. tation of 70 continuous core drillings for water researches

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Table 1 Dynamics of the Valle Caudina intermontane basin during paleoenvironments of the basin. Different lithofacies, the Late Quaternary linked to different geological, morphotectonic and climatic conditions, have been identified, and the distribution of the drillings in the basin has permitted to trace three NE–SW and NW–SE geological sections (Figs. 1, 6). The stratigraphic log in the borecores begins with the Basal Clay unit (BC, Table 1), consisting essentially of clay deposits interbedded with thin layers of sand, passing upward to a thick layer of fluvial sands (FL) with uncertain lateral continuity. Volcaniclastic layers consist of grayish cineritic deposits alternating with coarse-grained levels (Ancient Tuff; AT, Table 1). The sequence continues with clayey lacustrine sediments system (lacustrine I unit, LI), in which peat lenses are present. Upwards, a coarse-grained unit suggests the transition to a fluvial–lacustrine unit (FL). The stratigraphic succession continues with gray tuffaceous deposits that gradually fade upwards to yellowish ones, with a variable degree of cementation; they represent the distal facies (Di Girolamo et al. 1984) of the Campanian Ignimbrite (CI;*39 kyr BP; De Vivo et al. 2001). Finally, heterogeneous deposits (gravels, medium to fine sands and clays) form the next lacustrine II unit (LII). Locally, in The three main phases of morphoevolution and sedimentary cycles some boreholes of the southeastern sector of the valley, at occurred (the volcanological markers of continental paleoenvironments 265/260 m a.s.l., inside these units, a post-Campanian are highlighted in gray,thesolid star indicates archeological remains) Ignimbrite, gray pyroclastic materials have been found at C continental, T transition paleoenvironments: subscript L lacustrine, Lanzilli (GT; section a–b in Fig. 6a). F fluvial, FL fluvial–lacustrine, V volcaniclastic, climate: R–W Riss– Wu¨rm interglacial, W Wu¨rm glacial (from I to IV) and relative The areal distribution of the various lithofacies suggests interstadial phases, HCO Holocene climate optimum, CWP cool wet a complex continental environmental evolution. In partic- period, RWP Roman warm period, units: BC Basal Clay, AT Ancient ular, the extension of the Basal Clay and the Ancient Tuff Tuff, LI lacustrine I, AF alluvial fan, FL fluvial–lacustrine, CI (BC and AT; section a–b in Fig. 6a) seems limited to the Campanian Ignimbrite, LII lacustrine II, AP Avellino Pumices, RP reworked pyroclastics stratigraphy, c clay, s sand, g gravel, cycles: southern sector of the valley; on the contrary, there is a A pre-ancient Tuff, B post-ancient Tuff—pre-Campanian Ignimbrite, wide distribution of the lacustrine I unit (LI; section c–d in C post-Campanian Ignimbrite Fig. 6c) that evidences a quite large lacustrine paleobasin. The fluvial–lacustrine unit (FL; section e–f in Fig. 6b), (Abruzzese 1979) have allowed to delineate the Late Qua- in the geological cross-section, appears quite large: it ternary geological and morphological evolution of this basin stretches with some areal continuity from Paolisi up to the (Figs. 1, 4). The boreholes drilled between 262 and 400 m mouth of the valley, to the West and to its center, reaching a.s.l. reach a maximum depth of 80 m, with an average depth Cervinara to the South (Fig. 1). The erosive activity along of 35 m. A significant support for the reconstruction of the the slopes of the Avella–Partenio massif could have been main geological and morphological phases of the analyzed increased significantly during the last post-glacial times, area is the already mentioned occurrence of three pyroclastic which determined a coarsening upward sequence with the layers, as well as of archeological and prehistoric remains, deposition of alluvial fan prograding towards the lake that especially frequent in the Caudina valley (Abate et al. 1998). extended in the valley depocenter. Finally, to better understand the recent morphodynamics of The Campanian Ignimbrite (CI; section e–f in Fig. 6b) is the valley, three geological cross-sections, based on the present in the valley like a deposition lobe which develops stratigraphic correlation from boreholes, outcrops and geo- from Cervinara up to Montesarchio, from South to North. morphological survey, were drawn (Fig. 6). In the northwestern area (Moiano), this unit has been modeled to form a fluvial terrace of second order. Two pyroclastic layers separated by paleosols with a 3-m-thick 5 Analysis of stratigraphic data grayish ignimbritic bedrock at the base, outcrop 700 m far to the Northeast of Moiano, along a 12-m-high steep cliff, The analysis of numerous well stratigraphies has allowed at 245 m a.s.l. (Fig. 1). This volcanic deposit is texturally to reconstruct the sedimentary processes and the related and altimetrically well correlatable with the Ancient Tuff 123 Author's personal copy

Rend. Fis. Acc. Lincei (2014) 25 (Suppl 2):S231–S240 S237 found in some drillings at 230/235 m a.s.l., 4 km apart the central sector of the valley. The outcrop of Pliocene (AT; section a–b in Fig. 6a), with a radiometric age dated clays (Pescatore 1964) in the eastern part of the section c– at *100 kyr BP (De Vivo et al. 2001). Finally, the d, suggests a large mudflow expanded down to the valley deposits of the lacustrine II unit extend almost in the entire center. plain (LII; Fig. 6), with the exception of two small zones The analysis of the geological data (field survey, dril- (Cervinara and Paolisi), where two large alluvial fans from lings and cross-sections), suggests that the basin fill besides the northern Mt. Avella extend towards the center of the the role of the Ancient Tuff and the Campanian Ignimbrite valley. is attributable to a distinctly lacustrine and fluvio-lacustrine deposits, in which the distribution of facies was strongly controlled by the pre-existing morphology of the basin and 6 Discussion by climatic events and related runoff. The latter was characterized by different rates: at times, of markedly The Quaternary successions of the Valle Caudina inter- riverine type, with deposition of alluvial sediments and montane basin may be divided into four main facies types: dissection of the various units (De Pippo et al. 2006, 2008); 1. lacustrine sensu stricto 2. fluvial–lacustrine, 3. alluvial at other times, of a lacustrine type, with decantation of fine fan, and 4. pyroclastic deposits, of which the uppermost is sediments and formation of peats (De Pippo et al. 2001, represented by the Campanian Ignimbrite and the deeper 2004). Starting from the Basal Clay (BC), which corre- one by an older ignimbritic episode. The textural and sponds to an environment of calm waters’ deposition, the stratigraphic features of these deposits suggest the persis- oldest tuffs (AT) deposited, testifying that an intense tence in the basin of different paleoenvironments, ranging pyroclastic event occurred. This level marks a first barrage from marsh to continental. The geological cross-sections of the Isclero paleoriver with the consequent flooding of (Fig. 6) cover almost the entire plain, except for the sector the upstream plain. Lenses of peat in the clays overlying of Moiano to the Northwest. Their analysis has allowed to the oldest pyroclastic unit suggest small marshes at the reconstruct the relationships between the various units here lower lake levels. Subsequently, during the Pleistocene, an recognized and the Mt. Partenio and Mt. Taburno carbon- increase in slope erosion has allowed the sedimentation of ate massifs. coarse-grained deposits (FL; fluvial–lacustrine unit) with Section a–b extends in the Apennine direction (NW–SE) discrete sediment transport from the perimetral channels to and crosses longitudinally the valley. Below the reworked the plain. Given the shallow depth of the lake, it can be pyroclastic unit (RP; Fig. 6a), the lacustrine II unit (LII) is assumed that the fluvial processes were still active, thus characterized by alternations of clay, sand and gravels, enabling the deposition of sediments with heterogeneous which completely overlie the buried Campanian Ignimbrite. grain size in the central area of the valley. At about 39 kyr In the southeastern area along the entire valley lacustrine BP, the Campanian Ignimbrite completely covered the deposits attributable to the first paleoenvironment (lacus- fluvio-lacustrine and lacustrine deposits. The ignimbritic trine I unit, LI) are present. In the middle of this section, lobe, widely outcropping in the central part of the valley, both pyroclastics (AT, Ancient Tuff) and a thick sandy layer has probably barred the discharge of the Isclero paleoriver lie above the clayey unit (BC, Basal Clay), which represents and of its tributaries, creating the conditions for an over- the local substrate. In the geological sections c–d and e–f flow of the watercourses. The waters gradually have floo- (Figs. 6b, c) on the base of drilling data, a buried alluvial ded the entire plain, creating a wide shallow lake, which fan has been identified at Cervinara, interbedded into the was affected by the climatic oscillations of the time as lacustrine I unit (LI). In particular, the cross-section c–d evidenced by peat levels or by desiccation cracks. During shows that the alluvial fan partially lies on a carbonate the Holocene, at the gorge of Mt. Porrito (near Moiano), in bedrock, while some travertine lenses spread at the foot of the northwestern sector of the basin the combined action of the Avella massif. Moreover, a deeper alluvial fan is int- the lake overflow and of the regressive erosion in the erstratified with the deposits of the lacustrine I unit (LI), at downstream section of the Isclero paleoriver very likely the bottom of the section e–f (Fig. 6c). activated the erosion of pyroclastic deposits which barred The alluvial deposits of Valle Caudina, as well as of the threshold, favoring the outflow of the lacustrine basin. other basins of the southern Apennines (e.g., Campania The erosion of this threshold has continued over time, Plain), are strictly interlinked with volcaniclastic products. modeling also the present-day morphology characterized At the base of the reworked and superficial volcaniclastic by two orders of fluvial terraces and by topographically deposits, the lacustrine II unit (LII) lies in stratigraphic depressed zones, where the Isclero, Varco and Tesa Rivers contact with the underlying younger ignimbritic bank (CI). currently flow (Fig. 4). Below this volcanic formation, the fluvial–lacustrine unit Finally, the Holocene debris and alluvial fan deposits (FL) rests above the lacustrine I unit (LI), present only in represent ancient colluvial products placed along the foot 123 Author's personal copy

S238 Rend. Fis. Acc. Lincei (2014) 25 (Suppl 2):S231–S240 of the carbonate slopes which delimit the basin. We 7.1 First morphosedimentary phase (*100/40 kyr BP) highlight that the current coalescing alluvial fans at the base of the Taburno massif are migrating upstream with During this phase, a series of pyroclastics dated respect to the buried ones, thus reflecting the process of a *100 kyr BP (De Vivo et al. 2001) formed. These ancient parallel slope retreat. The interposition of fluvio-lacustrine ignimbritic products currently outcrop to the Northwest and lacustrine sediments (at the base of the Campanian and have been found in some drillings to the South of the Ignimbrite), both in the deeper and higher alluvial fans, is valley, in a zone which then was probably its depocenter, likely attributable to a massive rejuvenation of the Mt. with correlatable thickness. The ignimbritic deposit (AT, Partenio and/or to a drier climate (Wu¨rm I, Wu¨rm II Ancient Tuff) has very likely determined the damming of interstadial: 55–45 kyr BP; Bergomi et al. 1975). The the Isclero paleoriver as well as of its tributaries. To this presence of pyroclastics (AT) dated *100 kyr BP (De the flooding of the valley followed, with the development Vivo et al. 2001) at the base of the oldest lacustrine sedi- of a large, shallow lacustrine basin upstream the threshold ments (LI; lacustrine I unit) represents the end of the that was characterized by clayey sedimentation (LI, ancient continental phase and the beginning of the transi- lacustrine I unit). The subsequent fluvial–lacustrine stage tion paleoenvironment. (FL, fluvial–lacustrine unit) has been attributed to a general To determine the chronology of the most recent lacus- erosion of the pyroclastic layers which barred the valley, or trine event (LII; lacustrine II unit), the finding of some to neotectonic deformation which unlocked the mainstem stone tools and artifacts has been very helpful; they are outflow and activated the regressive erosion of the paleo- dated to prehistoric, protohistoric or to historical periods river. Interstratified with the lacustrine and fluvial–lacus- (Berglund 2003). Pottery with sharp edges and red bands’ trine successions, slope debris and alluvial fans (AF; as decoration, still well preserved, in primary position have colluvial deposits) are present, gradually shifted upstream been attributed to the Serra d’Alto style (3500–3000 BC), from a parallel slope retreat. Finally, the Campanian falling in the Middle Neolithic. At the top, there is a thin Ignimbrite (CI), *39 kyr BP (De Vivo et al. 2001), closed layer of pumices of the eruption of Mt. Somma-Vesuvius, this phase of transition entirely covering the fluvial– dated 3.78 kyr BP, known as Avellino Pumices (Albore lacustrine sequence. Livadie et al. 1998). Therefore, the last lacustrine deposits fall within the Neolithic (5500–2600 BC). Towards the 7.2 Second morphosedimentary phase (*40/5 kyr BP) center of the valley the ruins of the Roman town have moreover been found, from which the name of the The emplacement of the Campanian Ignimbrite (CI) orig- valley. In its necropolis, some proto-Corinthian pots, dated inated a new succession similar to the previous one. A new to 710 BC, have been also found (Albore Livadie and barrage developed forming a second lake basin and the Gangemi 1985; Albore Livadie 1986). This confirms the consequent deposition of lacustrine sediments (LII, lacus- wide extension of the lacustrine environments in the Cau- trine II unit). Also in this case, slope debris and alluvial dina valley, showing they continuously characterized fans (AF) are interstratified with the lacustrine deposits; almost the entire valley between *39 and *3.8 kyr BP. these progressively moved upstream due to the constant parallel slope retreat. The culmination of the most recent lacustrine episode can be reconstructed thanks to the dis- 7 Conclusions covery of prehistoric and protohistoric artifacts, such as remains of Neolithic ceramics dated back to 5.5–5 kyr BP The analysis of the geomorphological characteristics of (solid star). The latter have been found in primary position Valle Caudina as well as of the depositional pattern of this in the clay of the most recent lacustrine sequence (LII, intermontane basin allowed to obtain general information lacustrine II unit). Thus, the sedimentation of the deposits about the paleoenvironments and related sedimentary pro- of this phase is attributable to an interval between*39 cesses during the Late Quaternary, after the tectonic kyr BP (age of Campanian Ignimbrite) and *5 kyr BP structuration of this depression. Starting from a lacustrine (Middle Neolithic). clay substrate, two significant ignimbritic episodes follow. Subsequently a fluvio-lacustrine and two lacustrine events 7.3 Third morphosedimentary phase (*5 kyr BP/ have occurred alternating during the Late Pleistocene– present-day) Holocene. Therefore, the morphological evolution of the basin during the last 100 kyr can be subdivided into three The presence of a Roman settlement in the center of the main phases (Table 1), with development of different pa- valley (ancient Caudium) suggests that the lacustrine basin leoenvironments along a segment of the present-day Isclero has undergone a substantial downsizing or even that it was River valley, as follows. completely dried up between *5 kyr BP and the Roman 123 Author's personal copy

Rend. Fis. Acc. Lincei (2014) 25 (Suppl 2):S231–S240 S239 period (*2.5 kyr BP; solid star). At present, in the Valle impact of the « Avellino Pumices » eruption of Somma-Vesu- Caudina basin, the Isclero river flows, running from the vius on old bronze age sites in the Campania Region (Southern Italy). Quaternaire 9(1):37–43 Southeast to the Northwest. Berglund BE (2003) Human impact and climate changes—synchro- In the first phase, the fluvial–lacustrine unit (FL), fol- nous events and a causal link? Quatern Int 105:7–12 lowing the lacustrine I unit (LI), could have been activated Bergomi C, Manfredini M, Martelli G (1975) Note illustrative della by erosion of the pyroclastic threshold, by neotectonic carta geologica d’Italia. Foglio 173, Benevento Bordoni P, Valensise G (1998) Deformation of the 125 ka marine displacement (Cinque 1992) and/or subsidence. Consider- terrace in Italy: tectonic implications. In: Coastal Tectonics. ing the age of the underlying Ancient Tuff (AT) formation Geol Soc London, Spec Publ 146:71–110 and its altitude, as well as the thickness of the overlying Brancaccio L, Cinque A (1988) L’evoluzione geomorfologica sequences, the vertical lowering rate of soil results dell’Appennino campano-lucano. Mem Soc Geol It 41:83–86 Brancaccio L, Cinque A, Sgrosso I (1979) Forma e genesi di alcuni *0.2 mm/y in the last 100 kyr. This value is quite low, so versanti di faglia in rocce carbonatiche: il riscontro naturale di un most likely it is due to subsidence, in accordance with the modello teorico. Rend Accad Sci Fis e Mat Napoli, ser values calculated by Bordoni and Valensise (1998) for 4(46):7–22 some plains of central-southern Italy from the Tyrrhenian Bravi S, Civile D, Martino C, Putignano ML (2006) La struttura da interferenza nei carbonati mesozoici della dorsale di Monte (125 kyr BP) to the present. Moreover, it has not been Fellino (Appennino Campano). Boll Soc Geol Italiana, Ital J possible to precisely determine the timing of the fluvial– Geosci 125:105–116 lacustrine phase (FL, fluvial–lacustrine unit), subsequent to Ceccarelli M, Pignone N, Russo F (1999) Geomorfologia, G.I.S. e the first lacustrine stage (LI, lacustrine I unit), which could rischi naturali in Valle Caudina. Proc. Conf. ‘‘Le Pianure. Conoscenza e salvaguardia. Il contributo delle Scienze della also represent a separate episode. It occurred during the last Terra’’, 8–11 Nov, Ferrara (Italy) 278–281 glaciation, probably between about 60 and 40 kyr BP Cinque A (1992) Distribuzione spazio-temporale dei movimenti (Wu¨rm II), when the erosional processes were intense with tettonici verticali nell’Appennino campano-lucano: alcune rif- production of large detrital-alluvial deposits and large lessioni. St Geol Camerti, vol spec 1992(1):33–38 Comentale B (2010) Le massif du Taburno-Camposauro, une amount of coarse-grained sediments, as found in the montagne calcaire en position de charnie`re a` l’e´chelle de boreholes of the central and southern zones of the valley. l’Apennin me´ridional (Italie du Sud). Physio-Ge´o 4:27–42 The intercalation of fluvial–lacustrine deposits in the older D’Argenio B (1967) Geologia del gruppo Taburno-Camposauro and younger alluvial fans may be due to a rejuvenation of (Appennino campano). Atti Acc Sc Fis Mat, ser 3a 6(2):35–218 D’Argenio B, Pescatore T, Scandone P (1973) Schema geologico the slopes or to the low degradation characterized by a dry dell’Appennino Meridionale (Campania, Lucania). Atti Conv climatic period (Wu¨rm I, Wu¨rm II interstadial). Finally, the ‘‘Moderne vedute sulla geologia dell’Appennino’’. 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