Journal of Maps, 2009, 94-102
Geomorphological Map of the Ionian Area between the Tri-
onto and Colognati River Catchments (Calabria, Italy)
`
GAETANO ROBUSTELLI1 , FEDERICA LUCA1 , FABIO CORBI2 , GIANDOMENICO
2 1
FUBELLI , FABIO SCARCIGLIA and FRANCESCO DRAMIS2
1 Department of Earth Sciences, University of Calabria, via P. Bucci, 87036 Arcavacata di Rende, Cosenza, Italy; robustelli@unical.it
2 Department of Geological Sciences, Roma Tre University, Largo S. Leonardo Murialdo 1, 00146 Rome, Italy.
(Received 16th September 2008; Revised 18th December 2008; Accepted 23rd December 2008)
Abstract
This paper describes a geomorphological map representing a sector of the Ionian coastal belt, located
in north-eastern Calabria, between the catchments of the Trionto and Colognati Rivers. The landforms
have been distinguished according to their origin into: a) structural and tectonic-controlled landforms;
b) gravity-induced landforms; c) landforms formed by running water; d) coastal and transitional land-
forms; e) anthropic landforms, using as support a simplified topographic map on scale 1:20,000. The
geomorphological map provides information about the long-term evolution of the landscape and iden-
tifies the geomorphic processes presently active. Therefore, the map could be used in developing land
management and planning guidelines.
(Received 16th September 2008; Revised 18th December 2008; Accepted 23rd December 2008)
94
ISSN 1744-5647
Journal of Maps, 2009, 94-102 a
Robustelli, G., Luc´ , F. et al.
1. Introduction
This geomorphological map was produced as part of a joint research program under-
taken by the Departments of Earth Sciences (University of Calabria) and Geological
Sciences (Roma Tre University) to better understand the Quaternary evolution of north-
eastern Calabria. Along the Ionian coast, primarily through the analysis of marine ter-
race staircases, connections between climate, sea level changes and uplift rates have
been identified (Cosentino et al., 1989; Cucci and Cinti, 1998; Carobene, 2003; Cucci,
2004; Zecchin et al., 2004). Less developed are studies regarding the geomorphological
evolution of the landscape through the analysis of alluvial deposits and terraces (e.g.
Robustelli et al., 2005; Pagliarulo, 2006), these can be helpful in the reconstruction and
interpretation of the morphoevolution of the landscape.
The study area, located on the eastern flank of the Sila Massif, the northernmost portion
of the Calabrian-Peloritan Arc (Critelli, 1999), has been also chosen because it expe-
rienced uplift during the Pleistocene and shows evidence for coseismic fault growth
(Galli et al., 2006). Furthermore fault systems, coupled with lithology, exert a strong
control on landform distribution and the drainage network.
2. Methodology
The work was achieved through geological and geomorphological analysis carried out
by means of large-scale field survey and mapping supported by air photo interpretation.
The 1:10,000 and 1:5,000 sheets of the Carta Tecnica Regionale (edited by the Cassa del
Mezzogiorno and by Calabria Region, respectively), were used as the field base maps.
The geomorphological map, and its legend, were designed to emphasise both the long-
term landscape features and active and/or recent landforms, whose activity status has
been detected directly through repeated field observations and by comparing air photos
and maps.
The legend uses coloured symbols to represent morphogenesis, colour gradations for
activity status, plain solid filled polygons for bedrock geology unit and terrace orders,
following in part the schema of Panizza (1972), Brancaccio et al. (1994) and Castiglioni
et al. (1999).
The landforms, first surveyed at detailed scale (1:5,000 and 1:10,000), have been tran-
scribed onto a smaller scale, 1:20,000 topographic base with a 50 m contour interval and
depicting spot elevations at the main summits.
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Robustelli, G., Luc´ , F. et al.
3. Geological and geomorphological setting
The bedrock of the study area consists of a Hercynian crystalline basement (Sila Unit)
overlain by a Mesozoic and Cenozoic sedimentary succession (Critelli, 1999). Sedi-
mentation occurred from late Serravallian to middle Pleistocene, and was controlled
by strike-slip and extensional tectonics (Van Dijk et al., 2000).
The base of the stratigraphic succession (Roda, 1967) consists of the continental Con-
glomerati Rossi Irregolari Formation, overlain by the deltaic/shallow marine Arenaceo-
Conglomeratica Formation, which passes upward to the clayey offshore Argilloso-Marnosa
Formation. The Calcare di Base Formation and the overlaying Argille Marnose Salifere For-
mation, both heteropic with the Molassa di Castiglione Formation, were deposited during
the Messinian salinity crisis. The Gessi Formation and the Argille Scagliose Formation cap
the Miocene succession, onto which upper Pliocene and Pleistocene deltaic and marine
deposits lie unconformably. These deposits are truncated by a fluvial erosion surface.
Since the middle Pleistocene, the study area has been affected by rapid uplift, as testified
by the alluvial terrace staircase, occurring in the eastern sector of the study area (Molin
et al., 2004; Robustelli et al., 2009).
Morphologically, the study area, including the lower catchments of the Trionto, Coserie
and Colognati Rivers, can be divided into three different sectors:
1. Southern Sector: dominated by a mountainous landscape with deep, V-shaped
river valleys and summit remnants of an ancient flat or gently undulated land-
scape, that gently slopes to the north;
2. Intermediate Sector: characterized by more erodible lithologies, low-angle slopes,
and slightly incised valleys with wide braided rivers;
3. Northern Sector: characterized by five orders of alluvial terraces due to a combi-
nation of large-scale uplift and eustatic sea level changes (Robustelli et al., 2009).
Both lithology and structure are important in the formation of the drainage network.
A dendritic pattern with high drainage density is present east of Coserie River where
the lithologies are less permeable and more erodible. To the west of Coserie River, struc-
turally controlled geomorphic features, including small-scale chevron-shaped landforms
and a well developed trellis drainage pattern are present.
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Journal of Maps, 2009, 94-102 a
Robustelli, G., Luc´ , F. et al.
4. Structurally-controlled and tectonic landforms
Landform development related to the passive control exerted by alternating weak and
resistant lithologies are commonly observed in hilly topography along strongly to gen-
tly NE-dipping homoclinal ridges (hogback, cuesta). The upper surfaces of these land-
forms are undulating and sinuous due to changes in dip angle of layer, as well as the
presence of landslides in the underlying erodible lithologies that border valley sides
and progressively migrate upslope (Figure 1).
Figure 1. Undulating cuestas between the limestone rocks of the Calcare di Base Formation and the underlying and
overlying clayey/marly-clayey deposits of the Argille Marnose Salifere Formation and Argilloso-Marnosa Formation.
A) talus slope at the base of limestone (Calcare di Base Formation) cliff; B) translational landslide in the Argilloso-
Marnosa Formation
Notwithstanding recent tectonic activity in the study area (Robustelli et al., 2009), tec-
tonic landforms are not easy to distinguish from structurally-controlled features: low
scarps aligned along faults could be generated either by recent surface faulting (fault
scarps) or by selective erosion along ancient fault planes (fault-line scarps). The relation-
ships are observed along streams parallel to fault planes (subsequent streams).
5. Landforms formed by slope processes
The study area is widely affected by landslides of several different types (Cruden and
Varnes, 1996), and their size and evolution depend upon the litho-structural setting
and slope angle. Debris flows commonly develop where thick weathering mantles de-
velop on the Paleozoic and Eocene bedrock; rock falls are scattered on the Calcare di
Base Formation (limestone) and Molassa di Castiglione Formation (sandstone) cliffs. Rota-
tional/translational slides, usually evolving to mudflows, are the main slope processes
affecting the clayey/marly-clayey outcrops. Rotational slides occur where the thickness
of deposits is high; where these deposits are thinner, typically less than 20 m (e.g. in ho-
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Journal of Maps, 2009, 94-102 a
Robustelli, G., Luc´ , F. et al.
moclinal structures), translational slides move downslope over the underlying resistant
rock.
The term landslide catchments has been introduced to represent the main source areas
of deposits composing landslides, but not to distinguish between individual landslide
types. These source areas are located predominantly on both sides of the Coserie River
valley, where marls and clay of the Argilloso-Marnosa Formation and Argille Marnose Salif-
ere Formation crop out. The retrogression upslope of landslide scars on these valley side
slopes has developed a narrow, undulating watershed, mapped as landslide degradation
crests.
6. Landforms formed by running water
Sectors strongly affected by rills and persistent gullies (slope/wash processes in the map)
are frequently found on cultivated slopes underlain by clayey/marly-clayey deposits.
V-shaped, small valleys are developed in both weak and resistant terrains.
The modern river system in the study area is characterized by a strongly contrasted
seasonal regime with absence of water during most of the year and winter flooding. In
the western part of the northern sector of the study area, the riverbeds are wide and
braided, made of large blocks and boulders, transported downstream from the moun-
tain valleys by large winter floods. Artificial levees (embankments in the map) separate
the rivers from the adjacent alluvial/coastal plain.
The study area is characterized by the presence of five alluvial terraces, whose depo-
sitional body is composed of sub-rounded gravels and sands. The 1st order terrace
(Figure 2) ranges between 218 and 154 m a.s.l. The 2nd order terrace lies between 137
and 90 m a.s.l. and is separated from the upper terrace by a well-preserved fault scarp,
reaching about 40 m in height. Sometimes the surfaces appear to be incised because of
channel-head retreat and retrogression of the back slopes. The lowest terraces, located
at 87-70, 70-46 and 50-30 m a.s.l., respectively, are telescopically inset within each other.
From geological-geomorphological considerations, the terrace staircase is middle to late
Pleistocene in age (OIS 11 to OIS 5; Robustelli et al., 2009).
Above the quoted terraces (up to 471 m a.s.l.), between the Trionto and Coserie Rivers,
flat to gently rolling surfaces, overlain by relic limbs of alluvial deposits, are present.
These features likely represent an ancient foot-slope of the Sila Massif, remnants of a
strongly uplifted paleo-landscape.
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Robustelli, G., Luc´ , F. et al.
Figure 2. Overview of the first order alluvial terrace on the right side of the Coserie River valley
7. Marine and transitional landforms
The coastal plain in the study area is formed of the present beach, which is developed
subparallel to the coastline and reaches no more than 30-50 m in width, coupled with
various transitional landforms. The latter consist of fluvial deltas, filled swamp basins
and dunes that are almost entirely altered, destroyed or buried by human activities dur-
ing the last century, or outcrop in extremely small areas and therefore are not mappable
at the 1:20,000 scale. Dunes have been identified from pedological data reported by Di-
mase and Iovino (1996) or were inferred from bore holes and through communication
with local residents.
The coastline is affected by a general retreating trend, mainly caused by reduced debris
supply by the rivers to the sea, a result of agricultural practices upstream. However
the role of Pleistocene and Holocene sea level rise and increase wave activity cannot be
excluded.
The coastline retreat has been very rapid on the eastern side of the Trionto River delta,
while to the west some evidence for limited local advance has been observed.
8. Conclusion
Field surveys and air photo interpretations allowed the characterization of the main
morphological landforms present between the Trionto and Colognati Rivers (north Cal-
abria, Italy). This study demonstrates the linkage between lithology and structure con-
trol both landform distribution and the drainage network.
Where lithologies with different degrees of erodibility crop out, homoclinal ridges and
chevron landforms pattern are developed; in contrast, low permeability and highly
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Robustelli, G., Luc´ , F. et al.
erodible lithologies are characterized by a dendritic pattern. Also the type of landslides,
that widely affect the study area, is strongly influenced by the nature of the bedrock.
Widely distributed remnants of alluvial terraces are the most important landforms present
in the northern part of the study area. The overall distribution and character of these
landforms have been useful in developing a long-term model of landscape evolution.
Moreover, the data concerning landslides, slope erosion by running water and coastline
advance/retreat may represent a useful tool for evaluating the susceptibility of the area
to these processes and proposing suitable practises for land management and planning.
Software
All cartographic design was carried out using the ESRI ArcView 3.2. Data collected
by means of field survey and air photo interpretation have been geo-referenced and
digitized in order to carry out a spatial analysis of landform distributions. For each
mapped landform, a database containing attributes of the main features observed has
been developed.
Acknowledgements
We are grateful to R.C. Orndorff, G. Mastronuzzi, A.J. Stumpf and B. Rogers who helped
improve the manuscript and map.
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