Late Quaternary geomorphological evolution and erosion rates in the clayeyperi-Adriatic belt (central Italy)

Marcello Buccolini a, Bernardino Gentili b, Marco Materazzi b,⁎, Tommaso Piacentini c

a Dipartimento di Geotecnologie per l'Ambiente ed il Territorio, Università “G. d'Annunzio” Chieti-Pescara, Via dei Vestini 30, 66013 Chieti Scalo (CH), Italyb Dipartimento di Scienze della Terra, Università di Camerino, Via Gentile II da Varano, 62032 Camerino (MC), Italyc Dipartimento di Scienze della Terra, Università “G. d'Annunzio” Chieti-Pescara, Via dei Vestini 30, 66013 Chieti Scalo (CH), Italy

a b s t r a c ta r t i c l e i n f o

Article history:

Received 14 February 2008

Received in revised form 16 October 2009

Accepted 21 October 2009

Available online 28 October 2009

Keywords:

Geomorphological evolution

Denudation rates

Small catchments

Central Italy

Last Glacial Maximum

This study analyses the geomorphological evolution during the last 20000 years in two areas representative

of the peri-Adriatic belt of central Italy: Mt. Ascensione in the high hilly sector (600–1100 m a.s.l.) and the

Atri district in the hilly-coastal sector (up to ca. 500 m a.s.l.). In both areas the lithostructural setting is

characterized by an east-verging monocline mainly composed of clayey formations. The two areas are

compared in relation to their morpho-chronological aspects and geomorphological dynamics. The results

suggest two fundamental evolutionary phases: 1) About 20000 yr BP sedimentation occurred along the main

valleys when the middle to upper portions of slopes were covered by colluvial deposits; and 2) At the

beginning of the Holocene, the climatic improvement triggered erosion along rivers, producing deep and

narrow valleys. Estimated denudation rates during the last 20000 yr are 7.8 mm yr−1 for the Mt. Ascensione

area and 2.4–3.0 mm yr−1 for the Atri district, reflecting frequent landslides and fluvial erosion. The rates are

consistent with the data available in literature. Denudation rates double if we assume most of the erosion

process took place after the beginning of the Holocenic warming phase.

© 2009 Elsevier B.V. All rights reserved.

1. Introduction

Small catchments may respond directly to environmental changes.

Their evolution is influenced by several factors: climate (Preece and

Bridgland, 1999; Starkel, 2003; Brocard et al., 2003), sea level

oscillations (Schumm, 1993; Mizutani, 1996; Holbrook et al., 2006),

tectonics (Merritts et al. 1994; Coltorti et al., 1996; Schumm et al.,

2000), lithostratigraphy and structural setting of bedrock, (Dunne,

1980; Currado and Fredi, 2000; Pellettier, 2003), and human activity

(Garcìa-Ruiz and Valero-Garcès, 1998; Buccolini et al., 2007).

Therefore, studies on small catchments may provide important

findings regarding relationships between geomorphic evolution and

environmental factors.

This paper discusses the origin and development of small

catchments in the peri-Adriatic belt of central Italy (Fig. 1) since the

Last Glacial Maximum, in relation to late Pleistocene–Holocene

environmental change. Our study is based on the analysis of two

sample areas (Mt. Ascensione and Atri), which are considered

representative of the clayey landscape of central Adriatic Italy

(Castiglioni, 1935; Demangeot, 1965; Parea and Valloni, 1983;

Centamore and Deiana, 1986; Moretti and Rodolfi, 2000). In these

areas certain chronological constraints based on the absolute dating of

slope deposits are available, despite the general difficulty in finding

datable materials in central Adriatic Italy (Gentili et al., 1998; Aringoli

et al., 2007). These deposits permitted the reconstruction of land-

forms at about 20000 yr BP and the estimation of the late Quaternary

erosion rates through a comparison with the current topography.

2. Geological and geomorphological settings

2.1. Regional settings

The two sample areas, Mt. Ascensione (Area 1) and Atri (Area 2),

are located in the peri-Adriatic belt (Fig. 1), which represents one of

the three fundamental physiographic units of central Adriatic Italy

together with the Apennine chain and the Pedemountain belt. In

particular the Mt. Ascensione area (between 400 and 1100 m a.s.l.,

about 35 km2) is located northward, along the western margin of the

peri-Adriatic belt; the Atri area, further to the south (between 0 and

450 m a.s.l., about 100 km2), is located on the eastern margin, along

the coastal belt. Both areas share analogous geological settings (Fig. 2)

and similar morphometric features as well as elevation.

The formation of the central Apennine originated from the

emersion of calcareous rocks in the westernmost areas (Late Trias–

Early Miocene). These rocks, folded and overthrust on the Laga

Formation turbidites (Messinian) due to the Late Miocene–middle

Pliocene compressive tectonics (Calamita and Deiana, 1988), formed

the Umbria–Marche Ridge (maximum elevation 2476 m a.s.l. at Mt.

Vettore) and the Gran Sasso d'Italia Massif (2912 m a.s.l.). Different

Geomorphology 116 (2010) 145–161

⁎ Corresponding author. Tel.: +39 737 402603; fax: +39 737 402644.

E-mail address: marco.materazzi@unicam.it (M. Materazzi).

0169-555X/$ – see front matter © 2009 Elsevier B.V. All rights reserved.

doi:10.1016/j.geomorph.2009.10.015

Contents lists available at ScienceDirect

Geomorphology

j ourna l homepage: www.e lsev ie r.com/ locate /geomorph

rocks occur eastward, along the peri-Adriatic belt, where the two

study areas are located. They belong to a Pliocene–Pleistocene

sedimentary succession (Fig. 1a), composed of clayey sediments

overlaid on the Messinian turbidites with frequent intercalation of

clastic deposits (sands and conglomerates with similar thickness or

lenticular geometry). The major sedimentary cycle along the Adriatic

coast ended with an extensive Sicilian–Crotonian deposition of sands,

conglomerates and gravels under the coastal or fluvial/deltaic

environment (Fig. 2a). The structural setting in the study areas,

characterized by an east-verging monocline, is very regular near the

surface but more complex in deep areas (Fig. 2b). It results, on the one

hand, from the extensive tectonic uplift since the Early Pleistocene

with decreasing intensity from west to east; on the other hand it is

influenced by the effects of the older compressive tectonics. The

estimated uplift rate, 0.8–1.0 mm yr−1, has been calculated along the

Mt. Ascensione–Ripatransone alignment from the Middle Pliocene

(for the former) and Sicilian–Crotonian (for the latter) up to the

present day. This value is the highest in the peri-Adriatic belt of

central Italy (Bigi et al., 1995; D'Agostino et al., 2001; Cantalamessa

and Di Celma, 2004; Crescenti et al., 2004).

The peri-Adriatic sedimentary succession has been incised, from

west to east (Fig. 1) following the regional topographic gradient, by

the main cataclinal rivers that have generated a cuesta morphology.

The resultant valleys contain fluvial deposits, mainly calcareous

gravels. Their deposition started in the Middle Pleistocene (deposits

at the first level, about 100–150 m above the present valley floor),

continued during the Middle to Late Pleistocene (second level, 40–

80 m above the floor) and ended in the Late Pleistocene (third level,

Fig. 1. Study area. (a) Geological map. (b) Shaded relief maps with hydrographic networks.

146 M. Buccolini et al. / Geomorphology 116 (2010) 145–161

15–30 m above the floor). Holocene deposits (fourth level, 4–10 m

above the floor) are also present, but they may reflect recent human

impact on hillslopes (Gentili and Pambianchi, 1987; Cilla et al., 1996;

Coltorti, 1997).

There are widespread stratified slope deposits connected with

periglacial conditions both on the Adriatic and Tyrrhenian versants

(Boenzi and Palmentola, 1975; Castiglioni et al., 1979). In particular,

along the peri-Adriatic belt of central Italy, these deposits can be

found at the foot of the slopes and at the lower altitudes of 200–300 m

(Demangeot, 1965; Coltorti and Dramis, 1987). Monoclinal valleys of

the high hilly sector are usually incised along the less resistant pelitic

layers and are characterized by a marked asymmetry, strictly

Fig. 2. Geological sections. (a) Representative stratigraphic columns. (b) Cross sections (Areas 1 and 2, see Fig. 1).

147M. Buccolini et al. / Geomorphology 116 (2010) 145–161

congruent with the structural setting of bedrock. The wide coastal

morphostructures (hilly coastal sector), on the other hand, are

dissected by almost symmetric secondary cataclinal valleys, directly

flowing towards the Adriatic Sea. Moreover, the coastal belt greatly

differs from the neighbouring inner landscape because of the presence

of more resistant sandy-conglomeratic rocks and the tectonic uplift

along the coastal belt (Fig. 2b).

2.2. Mt. Ascensione (Area 1)

Mt. Ascensione, the highest relief of the peri-Adriatic belt, is a thick

lithoid body (middle Pliocene) made up of five minor sedimentary

sequences. Each sequence is composed of sands and sandy clays

placed over a basal conglomeratic unit which alternates with closely-

stratified clays (Fig. 2a), dipping 15°–20° towards the ENE (Fig. 2b)

and widely outcropping along the southern and eastern portions of

the relief (Cantalamessa and Di Celma, 2004). Joint systems and low

displacement dip-slip faults oriented N–S, NNW–SSE, and WSW–ENE

(Gentili et al., 1995) affect the structure; the orientation of the main

hydrographic network and that of the main structural scarps are

connected to these elements (Fig. 3a).

There are two generations of stratified slope deposits, previously

considered as a single one (Centamore and Deiana, 1986). They are

respectively attributed to the Middle and Late Pleistocene (Gentili

et al., 1998). In particular, along the southern sectors, their distinction

is evident; they are separated by a wide erosive surface located at 420

to 800 m a.s.l.

Other major geomorphological features are the spectacular bad-

lands on slopes with strata dipping not parallel to the slope, whereas

mass movements are often present along versants with strata dipping

parallel to the slope (Fig. 3; also discussed by numerous researchers

such as Dramis et al., 1982 and Buccolini et al., 2007).

2.3. Atri (Area 2)

The second sample area, the Atri district, includes two small

catchments directly flowing towards the Adriatic Sea: the Calvano (ca.

34 km2) and Cerrano (ca. 15 km2) catchments (Fig. 1b). They can be

considered representative of conditions along the Adriatic coastal belt

of central Italy.

The bedrock, a marine succession of the Late Pliocene to Early

Pleistocene, is composed of finely-stratified marly–clayey lithotypes,

overlaid by sandy conglomeratic rocks (Fig. 2a). These represent the

closing deposits of the Plio-Pleistocene sedimentary cycle and the

consequent transition to a continental environment (Parea and

Valloni, 1983; Cantalamessa and Di Celma, 2004). They outcrop on

the highest portions of watersheds. Thin widespread surficial

deposits, such as detritic, eluvial and colluvial materials, cover the

bedrock. Limited outcrops of alluvial deposits are locally present. The

structural setting is almost homogeneous in both catchments and

shows a regular monoclinal trend (about 10°) towards the Adriatic

Sea (Fig. 2b). The area is characterized by a structural surface that

gently slopes towards the east. It is modelled on sandy-conglomeratic

deposits, with altitudes ranging from 250 to 450 m a.s.l. The valleys of

the Calvano and Cerrano streams are symmetric (Fig. 4). Near the sea,

ridges between the valleys stand about 250 m a.s.l.

3. Climate, vegetation and human impact

Sea-level variation during the Pleistocene influenced the Adriatic

area because of the shallow and regular bathymetry. About 125000 yr

BP, during the Last Interglacial, the sea level was comparable to the

current level. During the Last Glacial Maximum, about 20000 yr BP,

the sea level reached its lowest, 100–130 m below the present-day

level (Butzer, 1976; Pirazzoli, 1997; Lambeck et al., 2004) (Fig. 5).

Until 15000 yr BP, when the first deglaciation stage involved the

whole European continent, conditions were mainly glacial, although

there are also signs of cold phases until about 11500 yr BP (Orombelli

and Porter, 1982; Giraudi, 1998).

The successive and progressive warming activated a progressive

sea level rise (Orombelli and Ravazzi, 1996; Lambeck et al., 2004).

Despite this general warming, some cold-humid periods have been

recognized after 8500 yr BP (Grove, 1979; Giraudi, 2005). The most

recent one occurred between 1500 and 1850 AD. (The Little Ice Age),

when precipitation in hilly Mediterranean areas significantly in-

creased (Le Roy Ladurie, 1971; Lamb, 1982). Currently, rainfalls in the

study area range between 600 mm along the coast and 1000 mm in

the mountains (Fig. 6) (Fazzini and Giuffrida, 2005).

Cultural development in the Adriatic belt started around 4500 yr BP,

as in other areas of the Mediterranean basin (Vita-Finzi, 1969; Delano-

Smith, 1979; Panini, 1983). Before man's intervention, forests covered

thewhole peri-Adriatic territory of central Italy, from the coastal area to

the Apennine chain (1750–1800 m a.s.l. forest limit; Sereni, 1979;

Ballelli et al., 1981). In the study area, the first significant deforestation

took place during the Roman period but woods again took over the area

in the early Middle Ages. Deforestation becomes even more important

between the 16th and the mid-19th centuries, when extensive agro-

sylvan-pastoral activities occurred. Intense erosiveprocesses, connected

to the deforestation and the climatic deterioration of the Little Ice Age

were active under the lack of agricultural preservation works (Le Roy

Ladurie, 1971; Sereni, 1979; Lamb, 1982; Grove, 2001). Afterwards,

particularly in the 20th century, conservation workswere carried out to

reduce slope erosion and sediment transport to streams, which in turnFig. 3. Mt. Ascensione (Area 1). (a) Panoramic view of the southern slope. (b) Illustrative

sketch (G = remnant of slope deposit; L = landslide; B = badland).

148 M. Buccolini et al. / Geomorphology 116 (2010) 145–161

caused intense linear erosion. Then, in the early 1960s, significant land

transformation was carried out by means of powerful machinery to

increase agriculture (Desplanques, 1975; Gentili and Pambianchi, 2002;

Buccolini et al., 2007).

4. Methodology

We chose an integrated approach based on geomorphological

surveys at different scales, sampling and dating of Quaternary

deposits, and topographic and morphometric analyses in a GIS

environment. Geomorphological surveys were carried out at a

relatively rough scale for the whole study area, and at a finer scale

(1:10000) for the two sample areas. Landforms caused by mass

movements (landslide bodies, crowns and scarps) and by running

water (badlands and fluvial terraces) and Quaternary deposits were

also analysed with reference to their location, geometry and

morphology, relationship with bedrock, stratigraphic and granulo-

metric characteristics, presence of continental fossils, paleosols, and

datable material. The deposits were chronologically constrained

based on the AMS 14C dating of charcoal fragments and organic

levels, conducted at the Beta Analytic Radiocarbon Dating Laboratory,

Miami, USA. The calibrations were performed using the newest

(INTCAL 98) database (Talma and Vogel, 1993; Stuiver and van der

Plicht, 1998; Stuiver et al., 1998). For some dating results derived from

previous studies by the same authors, only non-calibrated conven-

tional 14C ages are presented.

In both study areas data acquired from the above mentioned

detailed geomorphological surveys allowed the correlation of the

remnants of erosion and depositional surfaces; in particular geometry,

Fig. 4. Cerrano stream. (a) Panoramic view. (b) Illustrative sketch (C = remnants of conglomerates; S = sand; Cl = clay; L = landslide; B = badland).

Fig. 5. Reconstructed shoreline at about 20000 yr BP (Last Glacial Maximum; modified

from Lambeck et al., 2004). The box indicates the location of the study area.

149M. Buccolini et al. / Geomorphology 116 (2010) 145–161

plano-altimetric location and absolute dating of deposits have been

used to reconstruct the paleo-topography at 20000 yr BP. This was

done using TINs (Triangular Irregular Networks) created from a set of

vertices (points) corresponding to surface remnants. The operation

was carried out with the 3D Analyst extension of ArcGIS 9.0 (ESRI) and by

processing vector topographic maps in 1:5000 and 1:10000 scales

provided by the Marche and Abruzzi regional administrations. The

volume between past and current topography made it possible to

calculate the denudation rate in the considered time span. Historical

information about geomorphic processes was acquired from public

and private archives, newspapers, and scientific publications with

local information.

5. Data

5.1. Mt. Ascensione (Area 1)

Of the two generations of stratified slope deposits mentioned in

Section 2.1, only the most recent one (Late Pleistocene) has been

analysed for this study (Figs. 7 and 8). The deposits are discontinuous

in distal limbs of dissected surfaces while they are more continuous in

the proximal areas; moreover they can be correlated along longitu-

dinal or transversal sections. The deposits are made up of alternating

sandy and gravelly layers. The paleoflows inferred from imbricated

gravels, prograding bars and pebbly clusters show a clear radial

pattern and channelized structures with granulometry. Subordinate

sedimentary structures associated with debris flows are also detect-

able (Gentili et al., 1998).

The type sequence is clearly represented by the stratigraphic

columns observed at Porchiano and Polesio (Fig. 8a). Clinostratifica-

tion is evident, with attitudes ranging from 12° and 15° (upper

portion) to sub-horizontal (distal portion); cementation is very weak.

The top layers of the deposits are mostly characterized by fine to very

fine yellowish sands. One or more brown paleosoils, which are 20–

50 cm thick and located at different heights with respect to the base of

the deposits, occur within the sequences. In general, the contact

between the base of deposits and the bedrock beneath (arenaceous-

conglomeratic in a part of the northern sector and pelitic in the other

places) is marked by an irregular pre-depositional surface. On the

contrary the top of the deposits shows an almost regular trend, totally

congruent with the clinostratification observed within the sequences

(Fig. 8b,c). The age of the deposits was obtained from four radiometric

datings of charcoal fragments. At the bottom of the deposit at

Porchiano, at about 30 cm from the bedrock, dating goes back to

N51000 yr BP (Beta-108533); the second sample found at about 1 m

above the bedrock, yielded 41640±1260 yr BP (Beta-108532); and

two further samples at Polesio, found 50 cm apart and located at

about 3 m from the top of the deposit respectively, provided dates of

23230±170 yr BP (Beta-108531) and 22680±170 yr BP (Beta-

108530) (Fig. 8a).

Other fundamental geomorphologic elements along the slopes are

small catchments, systematically asymmetric and deeply incised into

Fig. 6. Isohyetal map of annual precipitation (contours in mm) of the study area.

150 M. Buccolini et al. / Geomorphology 116 (2010) 145–161

Fig. 7. Geomorphological map of Mt. Ascensione (Area 1).

Fig. 8. Deposits and landforms in Mt. Ascensione (Area 1). (a) Stratigraphic columns with 14C dating results. (b) Regularized small valley (Rola). (c) Stratigraphy of slope deposits at

Polesio.

151M. Buccolini et al. / Geomorphology 116 (2010) 145–161

the pelitic bedrock. Numerous studies during the last thirty years have

indicated intense andwidespread erosion in the area, characterized by

badland formation and landslides. Inmany cases, the limbs of the slope

deposits are disjointed by fractures, trenches, benches, counterslopes,

scarps and steps. All these elements are typical of mass movements at

different evolutional stages, whose shear zones are located inside the

weathered levels of clayey bedrock. In some cases both newly formed

landslides (Rupe di Santa Polisia, Ripaberarda) and old ones

(Porchiano and Ripaberarda) were observed (Figs. 7 and 9). Very old

landslides left only crowns and/or scarps behind, and their toes have

already been removed by fluvial erosion. The morphodynamic setting

of the area is therefore characterised by long translational slideswhere

strata dip parallel to the slope and shear zones and spectacular

badlandswith local rotational slides, falls and toppleswhere strata dip

transversally to the slope (Figs. 7 and 9b,c).

Historical documents (Carlini De Carolis, 1792; Galiè and Vec-

chioni, 1999; Santoni et al., 2005) show that many landslides affected

villages since the 13th century (Table 1). In all cases, buildings

affected by the landslides were located near badlands or landslide

scarps, and mass movements were always preceded by an intense

deepening of the clayey bedrock by fluvial erosion. The most

significant example is represented by Castignano, a historical village

of the early Middle Ages, whose southern slope repeatedly experi-

enced large mass movements (Table 1) which forced the inhabitants

to move towards the northern sectors.

Historical studies and oral witnesses also evidenced the marked

increase in linear water erosion between 1850 and 1950 leading to

20–30 m of channel deepening; it was substantially reduced after

1950 due to the construction of small dams and groynes along the

river banks, mainly along the Bretta and Chifente streams (Fig. 7).

5.2. Atri (Area 2)

In the Atri district the main active morphogenetic processes are

also mass movements and fluvial erosion that form crowns, scarps,

rills, gullies and badlands (Moretti and Rodolfi, 2000; Buccolini et al.,

2007). A huge landslide occurred in 1627 at the hydrographic left

slope of the Cerrano stream that destroyed houses and killed

numerous animals (De Secinara, 1652); the disappearance of a port

between the mouths of the Calvano and Cerrano streams is also

Fig. 9. Landslide related features in Mt. Ascensione (Area 1). (a) and (b) Gravitational fissures and fractures within slope deposit and pelitic bedrock at Porchiano. (c) Tilted 15th

century tower bell at Ripaberarda.

Table 1

Chronology of major landslides in Mt. Ascensione (Area 1).

Chronology of major landslides

Castignano 1204, 1335, 1450, 1500, 1574, 1605,

1634, 1717, 1772, 1777 and 1927

Porchiano End of 16th century

Ripaberarda 16th century, 1999

Capradosso 16th century

Rotella 1755

Appignano 1548, 1561, 1573, 1650, 1703, 1725,

1757, 1765, 1803, 1819, 1847 and 1995

152 M. Buccolini et al. / Geomorphology 116 (2010) 145–161

ascribed to landslides at the beginning of the 16th century (Buccolini

and Crescenti, 1991).

For this study, essential geomorphological elements are the

discontinuous limbs of sub-horizontal erosion surfaces (Fig. 10); they

have no chronological correlationswith theMiddle and Late Pleistocene

fluvial terraces along the main valleys; they are hereafter called

“benches”. Many benches are located in both Calvano and Carrano

catchments at different altitudes, and some of them can be correlated.

Except for the highest one, which is located at the boundary of the

sandy-conglomeratic and pelitic units, the benches are rarely related to

bedrock structure (Fig. 11). They represent former wide valley bottoms

(Buccolini et al., 2007). In many cases, along the lower edge of the

benches, the accumulation of slope material is observed. Along the

Cerrano stream at an altitude of 125 m a.s.l., two levels of clayey silt

containing organic substances and intercalated with fluvial gravel were

found along the edge of a bench. The lower level yielded a 14C age of

19260±210 yr BP (23330 to 22 360 cal. yr BP) and the higher level

17650±100 BP (21550 to 20440 cal. yr BP) (Beta-192039, Beta-

192040; Fig. 12).

6. Data analysis and interpretation

6.1. Mount Ascensione district (Area 1)

We reconstructed the topography of Mt. Ascensione at about

20000 yr B.P using ArcGIS 9.0 (Fig. 13a). Geological and sedimento-

logical characteristics such as stratigraphic continuity confirmed by

the progressive decrease of granulometry and clinostratification

angle, as well as elevation of land surfaces allowed the reconstruction.

The chronological data of the deposits below the surfaces, between

40000 and 20000 yr BP, support the reconstruction. The recon-

structed surface is located about 220–240 m above the valley bottom

(Figs. 13b and 14).

Around 20000 yr BP, the fundamental features of Mt. Ascensione

were defined. A high border scarp on the northern sector was formed

on bedrock, whereas the middle to upper portions of the surrounding

slopes were covered with slope deposits. The slopes below fluvial

benches and scarps were partially affected by erosion along the small

tributaries of the Tronto River. Sediment supply from the tributaries

contributed to the formation of the Late Pleistocene alluvial fans and

terraces (Fig. 14).

The morphodynamic evolution of the last 20000 years can be

interpreted as a result of successive erosive phases. According to

Demangeot (1965), Castiglioni et al. (1979) and Coltorti and Dramis

(1987), the formation of the Mt. Ascensione slope deposits at ca.

20000 yr BP was associated with the periglacial conditions in the Last

GlacialMaximum. This situation lasted until the end of the Pleistocene,

when periglacial processes terminated and fluvial incision started

(Orombelli and Porter, 1982; Giraudi, 1998; Fig. 15a). Development of

vegetation cover under a warmer Holocene climate (Erhard, 1956;

Dramis et al., 1982) further limited debris production on slopes and

activated linear erosion that formed deep gullies (Fig. 15b).

Fig. 10. Geomorphological map of Atri (Area 2).

153M. Buccolini et al. / Geomorphology 116 (2010) 145–161

Fig.1

1.GeologicalandgeomorphologicalcrosssectionsandpanoramicviewsinAtri(Area2)indicatingthelocationofbenches(seeFig.10forthelocationofsections).(a)Profile1alongtheupperpartoftheCalvanocatchment.(b)Panoramicviewof

profile1.(c)Profile2alongthemiddlepartoftheCerranocatchmentclosetoMutignano.(d)Panoramicviewofprofile2.(e)Profile3alongthemiddlepartoftheCalvanocatchment.f)Panoramicviewofprofile3.

154 M. Buccolini et al. / Geomorphology 116 (2010) 145–161

Fig. 12. Geology of the southern slope of Cerrano Valley in Silvi Village. (a) Stratigraphic column of the sample site at the Silvi cemetery. (b) Geological and geomorphological profile

(profile 4). See Fig. 10 for the locations of the site and profile.

Fig. 13. Reconstruction of the topographic surface at 20000 yr BP in Mt. Ascensione (Area 1). (a) Topographic map showing the limit of the calculation area. (b) 3D view of the

reconstructed surface.

155M. Buccolini et al. / Geomorphology 116 (2010) 145–161

Historical data demonstrates thatmorphodynamics during the late

Middle Ages was analogous to that of the present, forming deep,

asymmetric valleys with landslides on one side and badlands on the

other (Fig. 15c). The activation of mass movements affected several

villages (Table 1), particularly between the 15th and 18th centuries. It

was certainly favoured by increased rainfall at that time as in some

other Mediterranean areas (Provansal, 1995; Dìez et al., 1996; Grove,

2001; Giraudi, 2005), and by intensified agriculture after the Middle

Ages (Calzecchi Onesti, 1957; Desplanques, 1975; Gentili and

Pambianchi, 1987, 2002; Ruiz-Flaño et al., 1992; Garcìa-Ruiz and

Valero-Garcès, 1998).

Consequently the small catchments of the tributaries of the Tronto

River mainly developed in the Holocene. Although available data are

limited, erosion seems to have intensified during the cold and humid

periods of the Holocene such as the Little Ice Age, as suggested by the

record of floods and landslides (Grove, 1979; Lamb, 1982; Pavese

et al., 1992; Camuffo and Enzi, 1992; Pfister, 1994; Provansal, 1995;

Dìez et al., 1996; Antonioli et al., 2000; Grove, 2001; Giraudi, 2005;

Aringoli et al., 2007).

6.2. Atri (Area 2)

The data acquired for the Atri district also enabled the reconstruc-

tion of the topographic surface at 20000 yr BP. We first correlated

surfaces with chronological references; then other surfaces on the

basis of their height and inclination with respect to the current valley

floor, as proposed by Selby (1985) and Starkel (2003) (Fig. 16).

The erosion process that formed the surface at 20000 yr BP seems to

have started during the Last Interglacial (Butzer, 1976), and it continued

slowly and progressively in response to the lowering of the sea level.

According to Erhard (1956) and Pellettier (2003), the erosion process

was enhanced under cold and arid conditions. These conditions, as well

as a low topographic gradient, prevented linear erosion. Therefore, we

assume a limited river incision at 20000 yr BP (Fig. 17).

As indicated by Mizutani (1996) and Trenhaile (2002), active marine

erosion after a marine transgression around 10000 yr BP created a

platform bounded by a cliff. This process and tectonic uplift along the

Fig. 14. Schematic block diagram showing the morphological setting of the southern slope of Mt. Ascensione (Area 1) at 20000 yr BP.

Fig. 15. Schematic cross sections showing geomorphological conditions in Mt. Ascensione

(Area 1) since 20000 yr BP. (a) 20000 yr BP. (b) Early Holocene. (c) Early Middle Ages to

the present.

156 M. Buccolini et al. / Geomorphology 116 (2010) 145–161

coast led to a relative loweringof the local base level of theCerranoRiver

in spite of the sea level rise, enhancing erosion along streams.

The presence of the benches at different levels may be related to

several phases of Holocene marine ingression (Mörner, 1982;

Pirazzoli, 1997). This may have also led to alternating phases of

rapid and slow stream incision, together with mass movements along

the valley sides. As indicated by Moretti and Rodolfi (2000), they may

also be responsible for the activation of badland development

(Fig. 18). Recent mass movements were enhanced by deforestation

for cultivation (Buccolini et al., 2007).

7. Estimation of late Quaternary erosion rates

The comparisonbetween thecurrent topographyand that at 20000 yr

BP allowed us to estimate the total volume of erosion since 20000 yr BP.

For Area 1 (9.7×106m2) a volume of 1.55×109m3 has been calculated,

Fig. 16. Reconstruction of the topographic surface at 20000 yr BP in Atri (Area 2). (a) Topographicmap showing the limit of the calculation area. (b) 3D viewof the reconstructed surface.

157M. Buccolini et al. / Geomorphology 116 (2010) 145–161

yielding a denudation rate of 7.8 mm yr−1. For Area 2 calculation was

made for an area along each of the Calvano and Cerrano streams. For the

Calvano (2.3×107m2), we obtained a volume of 1.1×109m3 and an

erosion rate of 2.4 mm yr−1; for the Cerrano (7.0×106m2), a volume of

4.3×108m3 and an erosion rate of 3.0 mm yr−1. These values can be

considered as being the highest erosion values which refer to the time

span considered. When referring the volume of eroded soil to the entire

surface of each hydrographic basin, the following values resulted:

1.6 mm yr−1 for the Calvano stream 1.4 mm yr−1 for the Cerrano. They

canbeequatedwith theminimumerosionvalues regarding the time span

considered. Erosion rates double if we assume most erosion took place

after the onset of the Holocenic warm climate.

The difference in the erosion rates of the two study areas (2.4 or

3.0 mm yr−1 versus 7.8 mm yr−1) can be partly associated with

different morphostructural settings (monoclinal valleys with intense

landslide activity versus symmetric valleys) and different climatic

conditions (more frequent rainfalls in Area 1). The main factor,

however, seems to be the initial difference in relief, which is about

twice in Area 1. In Japan, Oguchi (1996) also suggested that the

magnitude of hillslope incision since the Pleistocene–Holocene

climatic change correlates positively with topographic relief.

Erosion rates in Europe reported in literature (Table 2) show that

the estimated erosion rates for our study area are lower than or

similar to those determined through in-situ measurements, in

particular small areas affected by active erosion processes such as

badlands and landslides. In contrast, lower erosion rates have been

reported for wider areas composed of less erodible bedrock than the

clayey rocks in our study area.

8. Conclusion

This study has discussed the geomorphological evolution of two

areas in the peri-Adriatic belt of Central Italy, and has estimated

erosion rates since the Last Glacial Maximum. It is possible to

distinguish the following evolutionary stages of landforms. Towards

the end of the late Pleistocene, sedimentation processes led to

deposition along the main valleys. At the same time the deposition of

slope deposits associated with periglacial conditions occurred, and

small tributaries located higher than the main valley, experienced

lateral erosion and/or sedimentation. The warmer climate since the

early Holocene activated linear erosion and resultant channel

deepening. Such processes resulted in high erosion rates since the

Last Glacial Maximum: 2.4–7.8 mm yr−1.

Acknowledgements

This study was supported by the following research projects:

1) MIUR-PRIN 2002, “Soil erosion in the Mediterranean environment:

direct and indirect evaluation in sample areas and hydrographic

basins” (Coordinator: G. Rodolfi), including a sub-project “Fast erosion

processes in sample hydrographic basins of the Marche-Abruzzi

Adriatic sector” (Local Coordinator: B. Gentili); and 2) MIUR-PRIN

2004, “The influence of climatic variations and/or of land use changes

on erosion processes in the Mediterranean environment” (Coordina-

tor: G. Rodolfi), with a sub-project “Impact of rural landscape

transformations on slope degradation processes during the Holocene

and its consequences on the fluvial–coastal system (Adriatic sector of

central Italy), (Local Coordinator: B. Gentili). The authorswish to thank

Prof. Francesco Dramis, University of Roma Tre and Prof. Giuliano

Rodolfi, University of Florence for their comments and suggestions for

an early draft, and Prof. Takashi Oguchi, University of Tokyo and

anonymous reviewers for their critical review.

Fig. 17. Block diagram of the Cerrano catchment in Atri (Area 2) at 20000 yr BP.

Fig. 18. Schematic cross sections showing geomorphological conditions in the Cerrano

catchment, Atri (Area 2) since 20000 yrBP. (a) 20000 yrBP. (b) EarlyHolocene. c) Present.

C = conglomerate; S = sand; Cl = clay.

158 M. Buccolini et al. / Geomorphology 116 (2010) 145–161

Table

2

KnownerosionratesintheMediterraneanareaandsurroundings.

IDLocality

Environment

Lithology

Method

Erosionrate

Period

Author

1SouthernApennineChain

Mountainbelt

Limestonesandmarly

limestones

GISanalysisonsummitalpaleosurfaces

0.22–0.30mm/yr

MiddlePleistocene–

Present

Amatoetal.

(2003)

2Alps

Mountainchain

Various

Sedimentvolumetrappedinvalleysandlakebasin

1.77mm/yr

LateGlacial

Hinderer(2001)

3Alps

Mountainchain

Various

Sedimentvolumetrappedinvalleysandlakebasin

0.6mm/yr

Last17000yr

Hinderer(2001)

4CentralSpain

Mountainchain

Granitesandgneisses

Dendrogeomorphologicalmethods

1.7–2.6mm/yr

Last101years

Bodoqueetal.

(2005)

1.1–1.8mm/yr

Last42years

5Blackseasourcearea

Mountainchains,hills

andplains

Various

SedimentsvolumetrappedinBlackSea

0.063mm/yr

Holocene

Degensetal.

(1976)

6AdriaticCentralItaly

Mainfluvialbasin

Alluvialdeposits

Thermochronometry

0.7–1.5mm/yr

Last20000yr

Coltortietal.

(1991)

7LacChambon(Massifcentral,

France)

Mountainbasin

Lacustrinedeposits

Qualitativeestimation

0.12mm/yr

Lastdeglaciation

Gayetal.(1998)

8LacChambon(Massifcentral,

France)

Mountainbasin

Lacustrinedeposits

Qualitativeestimation

0.05–0.1mm/yr

Holocene

Gayetal.(1998)

9EbroBasin(NE-Spain)

Badlandsonhillyarea

Clayeybedrock

Directmeasuresonerosionplotsinbadlandareas

5.6–11.2mm/yr

Present(1991–1993)Sirventetal.

(1997)

10SouthernTuscany

Hillyarea

Clayeybedrock

Directmeasures

15–30mm/yr(badlands)

Present

Ciccaccietal.

(2006)

60–90mm/yr(landslides)

11CentralItaly

Hillyareas

Clayeybedrock

Directmeasurescomparedwithindirectestimation

fromquantitativegeomorphologyondrainagenetwork

10–25mm/yr(badlands)

Present

DellaSetaetal.

(2007)

30–40mm/yr(landslides)

12Europe

Various

Soil

Various

10–20tha−

1yr−

1(overall)

Present

Verheijenetal.

(2009)

455tha−1yr−

1(gullyerosion-

maximumvalue)

13Mt.Ascensione(Area1)

Highhills

Slopedepositsandclayey

bedrock

RadiometricdatingsandGISanalysis

7.8mm/yr(156tha−1yr−

1)

Last20000yr

Thispaper

15.6mm/yr(312tha−

1yr−

1)

Holocene

14Atri(Area2)

Coastalhills

Colluvialdepositsandclayey

bedrock

RadiometricdatingsandGISanalysis

2.4–3mm/yr(48–60tha−

1yr−

1)

Last20000yr

Thispaper

4.8–6mm/yr(96–120tha−1yr−

1)

Holocene

159M. Buccolini et al. / Geomorphology 116 (2010) 145–161

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