GeolCarp_Vol68_No1_68

GEOLOGICA CARPATHICA

, FEBRUARY 2017, 68, 1, 68 – 79

doi: 10.1515/geoca-2017-0006

www.geologicacarpathica.com

The Crati River Basin: geomorphological and

stratigraphical data for the Plio–Quaternary evolution of

northern Calabria, South Apennines, Italy

GAETANO ROBUSTELLI



and FRANCESCO MUTO

Department of Biology, Ecology and Earth Science, University of Calabria, Rende, Cosenza, Italy;



gaetano.robustelli@unical.it

(Manuscript received December 2, 2015; accepted in revised form November 30, 2016)

Abstract: In this paper, we present the results of an integrated geomorphological and stratigraphical study carried out in

the eastern side of the Crati River valley (northern Calabria, South Italy). This area is characterized by the occurrence of

three order palaeosurfaces that, along with low-sloping palaeovalleys and structural landforms, are striking features of the

landscape. The relationships between morpho-tectonic and sedimentary evolution of the Crati Basin has been assessed

through sandstone detrital modes, morphostratigraphy and geomorphological correlation with adjacent areas. The two

main unconformity surfaces that typify the Quaternary fill were correlated to different steps of landscape evolution.

The presence of both erosional and depositional palaeosurfaces has been a useful marker for reconstructing sedimentary

and morphogenetic events, and hence to detect drainage network evolution and changes in source sediment area.

In particular, we recognized that the study area experienced, during the late Pliocene–Early Pleistocene a period of sub-

aerial landscape modelling as suggested by low-sloping palaeovalleys and related fluvial deposits (1

Order Palaeo-

surface). At that time, the source of the detrital constituents of the PPS Unit sandstones was mainly from the Sila Massif.

The onset of Coastal Range identification and uplift (Early Pleistocene) marks a change in the geomorphic scenario with

tectonic driven stream incision and valley development along the eastern side of Coastal Range, along with the occur-

rence of depositional and erosional landsurfaces (2

Order Palaeosurface) at footslopes. During this period, the Coastal

Range and Sila Massif were the sources for the detrital constituents of the PlS Unit sandstones. The progressive uplift of

Coastal Range during late Early Pleistocene and the marked backstepping of the depositional systems along the Sila

footslope was accompanied by alternating phases of down-cutting and base-level stability resulting in the development

of a step-like distributed 3

Order Palaeosurface. The presence of dolostone in detrital modes is clear evidence of stream

piracy phenomena of ancient palaeovalleys by the Crati valley-facing drainage network.

Keywords: geomorphology, Plio–Quaternary, Calabria, southern Apennines, Italy.

Introduction

Calabria hosts a series of marine Plio–Quaternary basins,

which developed during the late stage of continental collision

(Patacca & Scandone 2001). Their evolution has been con-

trolled by a series of roughly NW- and WNW- trending strike-

slip fault zones formed during the Neogene. They controlled

the migration of the Calabrian Arc and experienced episodes

of extension (Van Dijk et al. 2000), responsible for the dis-

section of the Calabrian Arc (Lanzafame & Zuffa 1976;

Lanzafame & Tortorici 1981; Tortorici 1981; Knott & Turco

1988; Turco et al. 1990; Tortorici et al. 1995; Schiattarella

1998; Cifelli et al. 2006; Tansi et al. 2007). This resulted in an

alternation of morphostructural ridges and Plio–Quaternary

tectonic depressions bounded by high-angle fault scarps

(Fabbri et al. 1981; Barone et al. 1982; Argani & Trincardi

1993; De Rosa et al. 2002; Milia et al. 2008; Filocamo et al.

2009; Robustelli et al. 2005, 2009; Pepe et al. 2010; Spina et

al. 2011; Tripodi et al. 2013; Longhitano et al. 2014; Robustelli

et al. 2014; Zecchin et al. 2015). In particular, the Crati Basin

(Fig. 1) developed in the subsiding hangingwall of the Crati

fault system (sensu Spina et al. 2011), one of the active and

segmented normal fault systems of Calabria (Tortorici et al.

1995; Galli & Bosi 2003; Tansi et al. 2005; Spina et al. 2009).

The Crati Basin is bounded by N-trending fault systems, and

the relative tectonic landforms are morphologically well

apparent. Its boundary faults related to regional strike-slip

tectonics, but the structural evolution of the depression has

long been debated (Turco et al. 1990; Tortorici et al. 1995;

Tansi et al. 2007; Spina et al. 2011).

Anyway, the aforementioned studies focused their efforts on

clarifying the stratigraphical, structural and seismotectonic

framework of the Crati Basin, unfortunately their relationships

to geomorphological settings were not considered. We lack

studies of the geomorphological evolution of the Crati Basin

through the analysis of the landscape characterized by hanging

remnants of gentle erosional landsurfaces. Furthermore, very

little is known about correlations between the landscape and

marine morphostratigraphic records (Muto 2006), which could

be very helpful for the reconstruction and interpretation of

morphoevolutionary history.

These issues are addressed in our study of the left side of the

Crati River valley, where much evidence of ancient landscapes

can be found.

ROBUSTELLI and MUTO

GEOLOGICA CARPATHICA

, 2017, 68, 1, 68 – 79

starting in the Early Miocene, onto the carbonate

platform rocks of the Apulian continental margin

(Van Dijk et al. 2000; Bonardi et al. 2001; Butler et

al. 2004; Iannace et al. 2007).

Neogene thrusting and the progressive southeast-

ward migration of Calabrian Arc are closely related

to the opening of the Tyrrhenian back-arc Basin

(Kastens et al. 1988; Patacca & Scandone 1989),

and was associated with NW- and WNW trending

strike-slip fault zones. These controlled the migra-

tion of the Calabrian Arc along its borders, and were

responsible for extrusion of the deep-seated units of

the Calabrian Arc and of the underlying Mesozoic

carbonate units (Tansi et al. 2007).

Strike slip faults were also important features as

they were characterized by episodes of transtension

(Van Dijk et al. 2000), responsible for the Crati

Basin development (Knott & Turco 1988; Turco et

al. 1990; Tortorici et al. 1995; Tansi et al. 2007).

Since the Middle Pleistocene, the Calabrian Arc

has experienced a strong regional uplift, still active,

resulting from the detachment of the Ionian sub-

ducted slab (Westaway 1993; Wortel & Spackman

1993; Tortorici et al. 1995; Van Dijk et al. 2000).

This regional tectonic event led to the formation of

a series of grabens along the entire western sector of

the Calabrian Arc (the so-called Siculo-Calabrian

Rift Zone, sensu Monaco & Tortorici 2000)

The Crati Basin, forming part of this zone, is

bounded by the Coastal Range to the west, by the

Sila Massif to the east, by the Pollino Ridge to the

north and by a NW-trending ridge to the south

(Fig. 1). The basin is L-shaped and can be divided

into two sub-basins: the N–S oriented Crati and the

E–W oriented Sibari sub-basins (Colella et al. 1987).

The N–S elongated Crati sub-basin (hereinafter

called Crati Basin), which includes the study area

(Figs. 1, 2), is morphologically asymmetric with a

steeper and shorter fluvial drainage along its eastern

side. Its shape is strongly controlled by an array of

normal faults (“Crati Fault System” in Spina et al.

2009). The sedimentary infill derives from footwall

uplifted areas exposed to extensive erosion (Molin

et al. 2004; Olivetti et al. 2012), and overlies the

Palaeozoic crystalline-metamorphic bedrock of the

Calabrian Block and its Miocene sedimentary cover

(Fig. 2).

Stratigraphy of the Crati Basin

The Crati Basin is filled by Plio–Pleistocene deposits that

can be divided into two (Lanzafame & Tortorici 1981; Fabbri-

catore et al. 2014) or three main depositional sequences (Spina

et al. 2011; Zecchin et al. 2015) bounded by a regional angular

unconformity.

Regardless of the number of sequences, the key question

manly concerns the age of the base of the Crati Basin infilling

and, hence, the presence/absence of the “mid-Pliocene uncon-

formity” of Zecchin et al. (2015). In this regard, geological

data (Lanzafame & Tortorici 1981; Barone et al. 2008; Robus-

telli et al. 2009) and palaeontological analysis (Lanzafame &

Tortorici 1981; Corbi et al. 2009; Fabbricatore 2011; Spina et

Fig. 2. Lithological map of the left side of the Crati Basin: (1) Fluvial deposits

(Middle Pleistocene–Holocene); (2) Clay, sandstone and conglomerate (PlS Unit

in Fig. 3A) (Early–Middle? Pleistocene); (3) Complex clastic wedge (PPS Unit in

Fig. 3A) (Pliocene–Early Pleistocene). (4) Clay, sandstone and conglomerate

(Miocene); (5) Dolostone and limestone(Mesozoic); (6) Calabride Complex

(Paleozoic); (7) Liguride Complex (Mesozoic); (8) Sampled section for petro-

graphic analyses.

ROBUSTELLI and MUTO

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, 2017, 68, 1, 68 – 79

Pliocene–Early Pleistocene sedimentary unit (PPS)

This unit rests erosively and unconformably on Miocene

deposits as well as pre-Neogene crystalline and metamorphic

bedrock. Its thickness increases towards the Sibari Plain, as

shown also by deep wells for hydrocarbon exploration.

Based on lateral and vertical sedimentary wedge arrange-

ment, this unit forms a complex assemblage of clastic wedges

up to 250 m-thick in the North of the study area. Its basal part

consists of superimposed and juxtaposed deltaic depositional

systems grading laterally and vertically into marine sandstone

and silty clay. This portion of the succession pinches out to the

South, where this unit is only characterized by its uppermost

part consisting in clayey sediments passing upward to mixed

silici/bioarenites strata and, again, to clay (Fig. 3A). Based on

the occurrence of Hyalinea balthica, the uppermost part of the

succession is considered not older than Calabrian (older

Emilian).

Early–Middle? Pleistocene sedimentary unit (PlS)

The second unit rests erosively and/or unconformably on

the PPS unit, and locally directly onto the bedrock and the

Miocene sediments along the southern portion of the basin. It

consists of continental to marine stacking depositional sys-

tems deposited in response to tectonic-induced basin subsi-

dence; it started in the west and proceeded eastwards, causing

a diachronous transgression (Lanzafame & Zuffa 1976;

Lanzafame & Tortorici 1981; Tortorici 1981; Spina et al. 2009;

Fabbricatore et al. 2014). According to data provided by Lan-

zafame & Tortorici (1981) and by Young & Colella (1988),

this unit can be considered younger than 1.2 M.y. (late Early

Pleistocene).

In particular, moving to the East the related deposits consist

of massive to crudely stratified, locally amalgamated,

pebble-to-cobble alluvial-fan conglomerates grading basin-

ward into fine to coarse-grained deltaic and beach deposits.

The succession is more than 100 m thick and consists mainly

of shoreface and offshore sands and clays, and shoal-water

deltaic clinostratified gravels. To the South, they form alter-

nating clastic wedges, locally telescopically arranged. To the

North, the deltas are organized into vertically-stacked

sequences that display internal depositional architectures con-

sisting of alternating progradational and aggradational geome-

tries, developing a basinward offset delta sequences of

Gilbert-type deltas (Fig. 3B) very rich in dolomitic gravel.

This arrangement can be interpreted as a result of tectonic con-

trol of the basin margin (e.g. Longhitano 2008).

Morphotectonic data

The oldest geomorphological elements in the area are han-

ging relics of a low-relief landscape (hereinafter named the

Order Palaeosurface) occurring on the uplifted mountain

ridge (Figs. 4, 5A) ranging in elevation between 1000m and

1200 m a.s.l., and cutting crystalline and Miocene sedimentary

bedrock.

Its formation can be related to relief smoothing processes

— fluvio-denudational — acting during periods of relative

stability of erosional base-levels. In particular, this landscape

includes highly eroded fault scarps, with cross profiles locally

declined at 20°, and low-sloping palaeovalleys, hanging and

beheaded valleys, none of them linked to the present-day

drainage network. Scattered patches of fluvial conglomerates

characterize this gently rolling landscape, but no chrono-

logical constraint is available. Therefore, the development of

the 1

Order Palaeosurface can be ascribed to the Pliocene on

the basis of cross-cutting relationships with bedrock, and geo-

logical and geomorphological data provided (Tortorici et al.

1995; Robustelli et al. 2005; Milia et al. 2009, Olivetti et al.

2012)

Moving downslope towards the Crati Trough, the apparent

N-trending fault scarps correlated with a new generation of

low relief landscape (2

Order Palaeosurface). Remnants of

the 2

Order Palaeosurface, occurring between 400 and 600 m

a.s.l. (Fig. 4), are widespread throughout the study area; at the

footslope of Mt. Luta and Cozzo Sprovieri (Figs. 4, 5A), they

are locally associated with slope and alluvial sediments

(Fig. 5B). Elsewhere, they form gentle footslopes carved into

hard rock, showing similar degree of maturity and concave

slope breaks at comparable elevation. Because this landscape

seals PPS unit, its development occurred during the late Early

Pleistocene.

Downslope of the previous landscape (Figs. 4, 5C), it is

important to note much steeper elements of hanging relics of

the 2

Order Palaeosurface, outlining the latest phases of

basin infilling. These fault scarps are related to a block faul-

ting episode that caused the uplifting of the 2

Order Palaeo-

surface and the development of the recent Crati Basin; its

depositional top surface, representing the 3

Order Palaeosur-

face, occur as stepped sequences in which vertical spacing

varies from metres to tens of metres. The surfaces show an

uneven spatial and altimetric distribution across stepped,

inclined planes that are separated by scarps not related to tec-

tonic structures, as they largely match with top depositional

surfaces of basinward offset Gilbert-type deltas.

According to stratigraphic data, these step-like distributed

surfaces indicate that the final stages of basin infilling were

accompanied by progressive and continuous dissection of

ancient landscapes where alternating phases of down-cutting

and of base-level stability occurred fairly quickly.

Petrographic signature of Plio–Pleistocene deposits

Eighty arenite samples representing the Crati Basin infilling

were collected along the south-western part of the Crati

Trough between Rende and Lattarico. They were analysed

according to the Gazzi-Dickinson method (Gazzi 1966;

Dickinson 1970; Ingersoll et al. 1984; Zuffa 1985; Critelli &

Le Pera 1994).

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Petrographic analyses of the Plio–Pleistocene sandstones of

the Crati Basin determines petrofacies characterizing each

lithostratigraphic unit (Fig. 6A), hence petrofacies get the

same names as sedimentary units.

The PPS unit sandstones show different composition moving

upward in the succession, and to the South.

In the area of Montalto Uffugo, the lower porzion is quartzo-

feldspathic (NCE

– Qt

L + CE

) (Fig. 6). Low-

grade to medium-grade metamorphic lithic grains (Lm) are the

dominant lithic population and include phyllites and fine-

grained schist fragments (mean value of lithics Lm

Minor carbonate sedimentary lithic fragments consist of

micritic and sparitic limestones while siliciclastic sedimentary

lithic fragments do not occur.

The upper portion (NCE

– Qt

L + CE

) tends

toward a feldspatholithic composition (Fig. 6) rich in sedi-

mentary lithic grains (Lm

), mainly carbonate grains

(micritic and sparitic limestones). The intrabasinal carbonate

(CI) component, made up of bioclasts, increases upward.

To the south, in the area of Rende, the detrital-mode of the

PPS Unit sandstones shows a similar trend (from quartzofeld-

spathic — NCE

– Qt

L + CE

— to feldspatho-

lithic — NCE

– Qt

L + CE

— composition),

even though compositional data reveals a higher increase in

sedimentary detritus. Carbonate sedimentary lithic fragments

consist of micritic and sparitic limestones, whereas the intra-

basinal carbonate component increases upward, where bio-

clasts are very abundant.

The lower part of the PlS Unit sandstones (Fig. 6) are

quartzo feldspathic (NCE

– Qt

L + CE

), with

a composition comparable to the lower portion of the PPS

Unit, but richer in sedimentary lithic grains. The upper portion

of the PlS sandstones tends to have a more feldspatholithic

(NCE

– Qt

L + CE

) composition. These sedi-

ments contain carbonate sedimentary lithic grains (mean value

of lithics Lm

), but it is worth noting the progressive

increase, and then the decrease of dolostone moving to the

younger portion (uppermost in Fig. 6), also characterized by

a trend again toward a quartzofeldspathic composition.

The Early Pleistocene sandstones cropping out along the

right side of the Crati (Fig. 4) River valley are quartzo-

feldspathic (NCE

100

– Qt

L + CE

), with abundant

feldspar grains. Low-grade to medium-grade metamorphic

lithic grains (Lm) are the dominant lithic population and

include phyllites and fine-grained schist fragments (mean

value of lithics Lm

Quaternary basin evolution

The Crati Basin is one of the main basins in the Calabrian

Arc where landscapes and stratigraphic architecture are useful

tools for the reconstruction of the main stages of landscape,

tectonic and stratigraphic evolution during the Quaternary in

the northern Calabria.

The integrated analyses performed here highlight that tec-

tonics played a key role in the basin’s genesis and evolution

(Turco et al. 1991; Cifelli et al. 2007; Tansi et al. 2007).

The reconstructed geomorphological and sedimentary history

shows that the study area experienced a number of morpho-

genetic cycles since the Pliocene (Piacenzian?) and during the

Early–Middle? Pleistocene.

The main evolutionary steps of the Crati Basin are summa-

rized in the following morpho-evolutionary stages.

Fig. 4. Morphostructural sketch map of the left side of Crati Basin

showing the main recognized landforms and the distribution of

the three orders of Palaeosurfaces: (1) 1

Order Palaeosurface;

(2) 2

Order Palaeosurface (erosional); (3) 2

Order Palaeosurface

(depositional); (4) 3

Order Palaeosurface; (4) Eroded fault scarp;

(5) Fault scarp; (6) Direction of the main low-gradient paleovalleys;

(7) Direction of the secondary low-gradient paleovalleys; (9) Wind

gap; (10) River capture; (11) Main tops (thick cross) rising above the

Order Paleosurface, along with hypothesized ones (thin cross)

should form part of the ancient watershed of N- NE-directed

paleodrainage; (12) Homoclinal ridge.

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Stage 1 (Pliocene)

The oldest stages of landscape evolution are represented by

hanging remnants of the 1

Order Palaeosurface (Figs. 4, 5A),

carved into crystalline and sedimentary bedrock of the Coastal

Chain.

Although some surfaces presumably developed locally as

a border polje through karst processes at the contact between

limestones and crystalline rocks, this landscape is considered

to result from fluvio-denudational relief smoothing processes

acting during periods of relative stability of erosional base-

levels, as much geomorphological evidence strongly indicates

(e.g., concave-up, low gradient footslopes, low-sloping

palaeo valleys, alluvial conglomerate).

The absence of clear step-like distributed surfaces indicates

that the relief dismantling was quite continuous and characte-

rized by a long-term phase of base-level stability or slow base

level lowering. By considering geological and geomorpho-

logical data provided in northern Calabria (Robustelli et al.

2005; Barone et al. 2008; Robustelli et al. 2009; Spina et al.

2009; Pepe et al. 2010; Muto et al. 2015), the present upland

developed mainly during the Lower Pliocene and partly

correlates to the low-relief landscape characterizing the Sila

Massif (Olivetti et al. 2012).

Fig. 5. Overview of landscapes noticeable in the study area and morphostratigraphic section of the Crati Basin showing the distribution of the

three orders of Palaeosurfaces. A — View from the East of Cozzo Spriovieri-Mt. Luta ridge; white arrow indicates stream piracy evidence

responsible for feeding dolomitic clasts into delta wedges during the Early–Middle? Pleistocene; 1

Order Palaeosurface = solid line;

Order Palaeosurface = dashed line; 3

Order Palaeosurface = dotted line. B — View from the North of Castrolibero rigde accompanied by

a morphostratigraphic section; C — View from the South of Montalto Uffugo area characterized by a stepped sequence of 3

Order Palaeo-

surface related to stratigraphic architecture (see text for detail).

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In particular, these gently rolling landscape relics (1000 to

1200 m elevated and Late Miocene to Pliocene in age) do not

show clear evidence of being originally connected with the

Tyrrhenian coast (Fig. 7A). On the contrary, the occurrence of

some beheaded, low-sloping and dry river valleys that witness

a north-northeastward direction of palaeo-drainage, along

with the presence of fluvial conglomerates, made up of dolo-

mitic clast fed by the Triassic dolostone cropping out to the

South, strongly support the above hypothesis. Furthermore,

the size of the main palaeo-valleys and the degree of rounding

of fluvial gravel clasts strongly suggest that they were cut by

high-order streams with catchment areas that had to cover

much of the distance that nowadays separate them from the

south-southwestern source area (Tyrrhenian area; Fig. 7A).

Therefore, we might assume that the 1

Order Palaeosurface,

nowadays found near the Coastal Range summit line, formed

on the north-northeastern flank of the northern Calabrian

chain.

Stage 2 (late Pliocene – Early Pleistocene)

The upper Pliocene –lower Pleistocene marks the first split-

ting of the previous Palaeolandscape and its lowering west-

ward. This led to the development of a narrow trough bordered

Fig. 6. Ternary diagrams showing sandstone composition of PPS and PlS l Units. Mean (symbols at the centre of polygons) and standard

deviation (polygon); Qm (monocrystalline quartz), F (feldspars, K + P), and Lt (aphanitic lithic fragments and fine-grained polycrystalline

quartz + CE). NCE (extrabasinal noncarbonate grains), CE (extrabasinal carbonate grains), CI (intrabasinal carbonate grains).

ROBUSTELLI and MUTO

GEOLOGICA CARPATHICA

, 2017, 68, 1, 68 – 79

by N-trending faults, which records the onset of marine sedi-

mentation (PPS Unit), and represents the early structural

depression where the modern Crati Basin will develop later on

(Fig. 7B). This period clearly marks the initial stretching of

this portion of the southern Apennines,

Geological data suggests that tectonic subsidence provided

the accommodation space for the deposition of the PPS Unit,

for the progressive backstepping of the system, and for the

progressive drowning of bedrock moving to the south

Furthermore, comparison between the quartzolithic/feld-

spatholithic detrital modes of Coastal

Range littoral province (Le Pera &

Critelli 1999) and quartzofeldspathic

detrital modes of late Miocene wedge

top basins (Barone et al. 2008), indi-

cates a possible provenance of the

lower portion of the PPS Unit from

the Sila massif. Moreover, it is note-

worthy the similar detrital modes

between sandstones of the Rende

lower section and Pleistocenic sand-

stones cropping out along the eastern

side of the Crati Valley. Conversely,

feldspathic lithic arenite strata of the

upper part of the Late Pliocene–Early

Pleistocene sediments indicate de

creasing siliciclastic influx (NCE)

into the basin (favouring intrabasinal

carbonate productivity; e.g., Barone

et al. 2008) as well as a possible new

low-relief source area located to the

South as the northward decrease in

calcareous sedimentary detritus in

the PPS Unit suggests.

From the foregoing considera-

tions, we consider that the western

part of the 1

Order Palaeosurface

was poorly fragmented and lowered

next to base level. As result, the land-

scape underwent slow dissection,

which allowed reshaping of the

Order Palaeolandscape. Westward

of the study area, Milia et al. (2009)

also argued for the presence of

southern sediment source areas.

Stage 3 (late Early Pleistocene)

The early Pleistocene marks a sig-

nificant change in the geological and

Fig. 7. Simplified sketches of geological and geomorphological evolution of the Crati Basin

from upper Pliocene to Present (not in scale); faults shown in the following frames claim to

indicate the merely vertical component of tectonics: A — Development of the 1

Order

Palaeosurface characterized by NNE-trending palaeodrainage. B — During the late Plio-

cene–Early Pleistocene the study area experienced a first fragmentation of the previous land-

scape leading to a further reshaping of the 1

Order Palaeosurface. C — During the Early

Pleistocene the 1

Order Palaeosurface was uplifted and the Coastal Range started to be

identified; backstepping of the Sila fault system (black arrow); development of the 2

Order

Palaeosurface. D — Progressive uplift of the Coastal Range during the Early–Middle?

Pleistocene led to the development of the 3

Order Palaeosurface, and to stream piracy

phenomena. E — The drainage network facing the Tyrrhenian Sea was responsible for

disabling part of the sediment source toward the Crati valley.

GEOMORPHOLOGICAL EVOLUTION OF NORTHERN CALABRIA, SOUTH APENNINES, ITALY

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geomorphological scenario of the study area. A blockfaulting

episode caused the fragmentation of the 1

Order Palaeosurface,

the development of a depression bordered by high angle,

NNE-trending faults, and an eastward migration of the fault sys-

tem resulting in uplift and erosion of the Sila slope (Fig. 7C).

At the end of the Emilian the Coastal Range was likely

wider than today toward the West, but afterwards it has pro-

gressively assumed its modern shape.

As a consequence, a new base-level became established and

led to the development of the 2

Order Palaeosurface. Rem-

nants of this landscape occur at elevations between 400 and

600 m a.s.l. (Figs. 4, 5). They appear entrenched within rem-

nants of the 1

Order Palaeosurface to the South, and they are

very noticeable on the footslopes of the Coastal Range ridge

(Fig. 4). Here the 2

Order Palaeosurface relics are characte-

rized by depositional and erosional landforms (Figs. 4, 5), the

last ones carved into hard rocks and showing a similar degree

of maturity at comparable elevation. The drainage network

formed as a response to the uplift of the Coastal Range, pro-

ducing steep catchments from which alluvial deposition pro-

graded onto the piedmont zone (Fig. 5B).

A late Early Pleistocene age can be ascribed to the develop-

ment of the 2

Order Palaeosurface, as it rests erosively or

seals Hyalinea Balthica bearing deposits.

Over the same time-span, the coastal area experienced sub-

sidence, resulting in clastic sedimentary successions having

first a quartzofeldspathic composition. Although detrital modes

indicate a Sila Massif provenance, detrital components (richer

in carbonate sedimentary lithic grains) and palaeocurrents also

reflect provenance from the Coastal Range.

Stage 4 (late Early – Middle? Pleistocene)

After the development of the 2

Order Palaeosurface, tec-

tonics caused the formation of a depression bordered by high

angle, NNE-trending faults that draw progressively the recent

Crati valley profile (Fig. 7D, E).

Pulses of eastward migration of fault systems affected the

Sila Massif (Lanzafame & Tortorici 1981; Fabbricatore et al.

2014) and caused the drowning of coastal slices and uplift of

the Sila Massif. The presence of perched-fluvial terraces and

hanging stream-dissected fans found at different elevations

within the valleys of the Tyrrhenian slope of the Coastal Range

(Robustelli et al. 2005; Muto 2006) further support the uplift

affecting the ridge at issue. At the same time, the Crati Basin

experienced an almost continuous and fragmentary uplift

where gentle erosional landscapes did not form, but deposi-

tional landscapes still survive, though deeply dissected.

The tectonic control of the eastern basin margin from which

Gilbert-type deltas were sourced, forced an offset basinward

arrangement. Similarly, the influence of tectonics is also

strongly suggested by the marked backstepping of the deposi-

tional systems cropping out on the eastern side of the Crati

Trough (Fabbricatore et al. 2014).

In this framework, more than one depositional surface

developed. According to stratigraphical data and depositional

system arrangement, these step-like distributed surfaces

Order Palaeosurface) indicate that the final stages of

basin infilling were accompanied by progressive and

continuous dissection of ancient landscapes and characte-

rized by alternating phases of down-cutting and of base-

level stability that occurred fairly quickly through time

(Figs. 4, 5).

It is also worth noting the difference in sediment detrital

modes and partitioning in composition during this phase of

landscape evolution. Although detrital modes indicate variable

composition from quartzofeldspathic to feldspatholithic,

the increase and decrease of dolostone in fine-grained deltaic

sediments are clear evidence of stream capture phenomena

and recycling processes. In fact, as the rivers flowing toward

the Crati Basin had their longitudinal gradients increased due

to uplift, headward propagation of incision tended to capture

the NNE-directed palaeodrainage drainage (Fig. 7D) the

watershed of which still had to include Triassic dolostone

(M. Cocuzzo area; Figs. 2, 4).

Afterwards, river capture phenomena resulting from head-

ward retreat of river valleys flowing toward the Tyrrhenian

Sea were responsible for disabling the dolomitic sediment

source area toward the Crati valley (Fig. 7E), outlining the

current physiography of the study area.

Concluding remarks

The integrated geomorphological and stratigraphical

approach adopted for the study of the Crati Basin represents

another goal of improving our knowledge of the Plio–Quater-

nary landscape evolution of northern Calabria. The Crati Basin

development and evolution was reconstructed through a model

depicting the relationships between sedimentary units, boun-

ding surfaces and landsurfaces. In this regard, the timing of the

Crati landscape evolution was constrained between late

Pliocene and Middle Pleistocene

On the basis of sandstone detrital and geomorphological

evidences, we have better constrained the timing of landscape

evolution and its relationships with basin sedimentary

infilling.

The presence of Hyalinea balthica confirms the existing

inferred age for the lower boundary of the PlS Unit, and

reveals that the upper age limit of the 2

Order Palaeosurface

has to be younger than 1.2 M.y.

The depositional system arrangement of PlS Unit and the

related step-like distributed 3

Order Palaeosurface, result

from alternating phases of down-cutting and base-level stability,

and suggest the progressive and continuous dissection of

ancient landscapes.

The roles of tectonics and river piracy are emphasized as

control mechanisms for composition and provenance of the

sandstone strata. Tectonics caused a change in fluvial connec-

tivity and the re-arrangement of the formerly NNE-ward-

draining river network during the late Early Pleistocene and

then in more recent times.

ROBUSTELLI and MUTO

GEOLOGICA CARPATHICA

, 2017, 68, 1, 68 – 79

References

Amodio-Morelli L., Bonardi G., Colonna V., Dietrich D., Giunta G.,

Ippolito F., Liguori V., Lorenzoni S., Paglionico A., Perrone V.,

Piccarreta G., Russo M., Scandone P., Zanettin-Lorenzoni E. &

Zuppetta A. 1976: The Calabria-Peloritani arc within the

Apennine-Maghrebide chain. Mem. Soc. Geol. Ital. 17, 1–60.

Argnani A.

& Trincardi F. 1993: Growth of a slope ridge and its con-

trol on sedimentation: Paola slope basin (eastern Tyrrhenian

margin). International Association of Sedimentologists, Special

Publication 20, 467–480.

Barone A., Fabbri A., Rossi S. & Sartori R. 1982: Geological struc-

ture and evolution of the marine areas adjacent to the Calabrian

Arc. Earth Evolution Science 3, 207–221.

Barone M., Dominici R., Muto F. & Critelli S. 2008: Detrital modes

in a late Miocene wedge-top basin, northeastern Calabria, Italy:

compositional record of wedge-top partitioning. J. Sed. Res. 78,

693–711

Bonardi G., Cavazza W., Perrone V. & Rossi R. 2001: Calabria-Pelo-

ritani Terrane and Northern Ionian Sea. In: Vai G.B. & Martini

I.P. (Eds.): Anatomy of an Orogen: The Apennines and Adjacent

Mediterranean Basins. Kluwer Academic Publishers, Dordrecht/

Boston/London, 287–306.

Butler R.W.H., Mazzoli S., Corrado S., De Donatis M., Di Bucci D.,

Gambini R., Naso G., Nicolai C., Scrocca D., Shiner P. &

Zucconi V. 2004: Applying thick-skinned tectonic model to the

Apennine thrust belt of Italy: limitations and implications. In:

McClay K.R. (Ed.): Thrust tectonics and hydrocarbon system.

A.A.P.G. Memoir 82, 647–667.

Cifelli F., Rossetti F. & Mattei M. 2006: The architecture of brittle

postorogenic extension: Results from an integrated structural

and paleomagnetic study in north Calabria (southern Italy).

Geol. Soc. Am. Bull. 119, 1/2, 221–239.

Colella A., De Boer P.L. & Nio S.D. 1987: Sedimentology of a marine

intermontane Pleistocene Gilbert-type fan-delta complex in the

Crati Basin, Calabria, sothern Italy. Sedimentology 34,

721–736.

Corbi F., Fubelli G., Lucà F., Muto F. , Pelle T., Robustelli G., Scar-

ciglia F. & Dramis F. 2009: Vertical movements in the Ionian

margin of the Sila Massif (Calabria, Italy). Boll. Soc. Geol. Ital.

128, 731–738.

Critelli S. & Le Pera E. 1994: Detrital modes and provenance of Mio-

cene sandstones and modern sands of the Southern Apennines

thrust-top basins (Italy): J. Sed. Res. 64, 824–835.

De Rosa R., Dominici R.& Sonnino M. 2002: Evidences of sin-sedi-

mentary volcanism in the Plio-Pleistocene succession of the

Mesima trough (west-central Calabria). Il Quaternario, Ital. J.

Quat. Sci. 14, 25–36 (in Italian with English abstract).

Dickinson W.R. 1970: Interpreting detrital modes of greywacke and

arkose. J. Sed. Petrol. 40, 695–707.

Fabbricatore D, Robustelli G. & Muto F 2014: Facies analysis and

depositional architecture of shelf-type deltas in the Crati Basin

(Calabrian Arc, south Italy). Ital. J. Geosci. 133, 131–148.

Fabbri A., Gallignani P. & Zitellini N. 1981: Geologic evolution of

the peri-tyrrhenian sedimentary basins. In: Wezel F.C. (Ed.):

Sedimentary Basins in Mediterranean Margins. Tecnoprint,

Bologna, 101–126.

Fabbricatore D. 2011: Stratigraphy and facies analysis of Quaternary

deposits of the Crati river valley. Tesi di Dottorato di Ricerca

(PhD. Thesis), Unical, Rende, 1–206 (in Italian).

Filocamo F., Romano P., Di Donato V., Esposito P., Mattei M., Por-

reca M., Robustelli G.& Russo Ermolli E. 2009: Geomorphol-

ogy and tectonics of uplifted coasts: New chronostratigraphical

constraints for the Quaternary evolution of Tyrrhenian North

Calabria (southern Italy). Geomorphology 105, 334–354.

Galli P. & Bosi V. 2003. Catastrophic 1638 earthquakes in Calabria

(southern Italy): new insights from palaeoseismological investi-

gation. J. Geophys. Res. 108 (B1), doi:10.1029/2001jb001713

2004.

Gazzi P. 1966: Late Cretaceous sandstones of Modena Apennine:

relationships with the Monghidoro Flysch. Mineralogica et

Petrografica Acta 12, 69–97 (in Italian with English abstract).

Iannace A., Vitale S., D’Errico M., Mazzoli S., Di Staso A., Macaione

E., Messina A., Reddy S.M., Somma R., Zamparelli V., Zattin

M. & Bonardi G. 2007: The carbonate tectonic units of northern

Calabria (Italy): a record of Apulian paleomargin evolution and

Miocene convergence, continental crust subduction, and exuma-

tion of HP-LT rocks. J. Geol. Soc., London 64, 1165–1186.

Ingersoll R.V., Bullard T.F., Ford R.L., Grimm J.P., Pickle J.D. &

Sares S.W. 1984: The effect of grain size on detrital modes: a test

of the Gazzi–Dickinson point-counting method. J. Sed. Petrol.

54, 103–116.

Kastens K., Mascle J., Auroux C., Bonatti E., Broglia C., Channell J.,

Curzi P., Emeis K.C., Glacon G., Hasegawa S., Hieke W., Mas-

cle G., Mccoy F., Mckenzie J., Mendelson J., Muller C., Rehault

J.P., Robertson A., Sartori R., Sprovieri R. & Tori M. 1988: ODP

Leg 107 in the Tyrrhenian Sea: insights into passive margin and

back-arc basin evolution. Geol. Soc. Am. Bull. 100, 1140–1156.

Knott S.D. & Turco E. 1991: Late Cenozoic kinematics of the Cal-

abrian Arc, southern Italy. Tectonics 10, 1164–1172.

Le Pera E. & Critelli S. 1999: Sourceland controls on the composition

of beach and fluvial sand of the northern Tyrrhenian coast of

Calabria, Italy: implications for actualistic petrofacies. Sed.

Geol. 110, 81–97.

Longhitano S.G. 2008: Sedimentary facies and sequence stratigraphy

of coarse-grained Gilbert-type deltas within the Pliocene thrust-

top Potenza Basin (Southern Apennines, Italy). Sed. Geol. 210,

87–110.

Longhitano S.G., Chiarella D. & Muto F. 2014: Three-dimensional to

two dimensional cross-strata transition in the lower Pleistocene

Catanzaro tidal strait transgressive succession (southern Italy).

Sedimentology 61, 2136–2171.

Milia A., Turco E., Pierantoni P.P. & Schettino A. 2009: Four-dimen-

sional tectono-stratigraphic evolution of the Southeastern

peri-Tyrrhenian Basins (Margin of Calabria, Italy). Tectono-

physics 476, 41–56.

Molin P., Pazzaglia F.J. & Dramis F. 2004: Geomorphic expression of

active tectonics in a rapidly-deforming forearc, Sila Massif,

Calabria, southern Italy. Am. J. Sci. 304, 559–589.

Monaco C.& Tortorici L. 2000: Active faulting in the Calabrian Arc

and eastern Sicily. J. Geodyn. 29, 407–424.

Muto F. 2006: Neogene Quaternary geological evolution of

north-western Calabria. Tesi di Dottorato (PhD thesis), Univer-

sità della Calabria, 1–121 (in Italian).

Muto F., Critelli S., Robustelli G., Tripodi V., Zecchin M., Fabbrica-

tore D. & Perri F. 2015: A Neogene-Quaternary Geotraverse

within the northern Calabrian Arc from the foreland peri- Ionian

margin to the back-arc Tyrrhenian margin. Periodico semestrale

del Servizio Geologico d'Italia - ISPRA e della Società Geolo-

gica Italiana, Geological Field Trips, 7, n.2.2., 1–65.

Olivetti V., Cyr A.J., Molin P., Faccenna C. & Granger D. 2012: Uplift

history of the Sila Massif, southern Italy, deciphered from cos-

mogenic

Be erosion rates and river longitudinal profile analy-

sis. Tectonics 31, doi:10.1029/2011TC003037.

Patacca E. & Scandone P. 1989: Post-Tortonian mountain building in

the Apennines. The role of the passive sinking of a relic litho-

spheric slab. In: Boriani A, Bonafede M., Piccardo G.B., Vai G.B

(Eds.): The lithosphere in Italy. Advances in Earth Science

Research. t.Nat.Comm.Int.Lith.Progr., Mid-term Conf. (Rome,

5-6 May 1987), Atti Conv. Lincei 80, 157–176.

Patacca E. & Scandone P. 2001: Late thrust propagation and sedimen-

tary response in the thrust belt-foredeep system of the Southern

GEOMORPHOLOGICAL EVOLUTION OF NORTHERN CALABRIA, SOUTH APENNINES, ITALY

GEOLOGICA CARPATHICA

, 2017, 68, 1, 68 – 79

Apennines (Pliocene-Pleistocene). In: Vai G.B., Martini I.P.

(Eds): Anatomy of an Orogen: The Apennines and Adjacent

Mediterranean Basins, Kluwer Academic Publication, 401–440.

Pepe, F., Sulli, A., Bertotti, G. & Cella F., 2010. Architecture and

Neogene to Recent evolution of thewestern Calabrian continen-

talmargin: an upper plate perspective to the Ionian subduction

system, central Mediterranean. Tectonics 29, TC3007.

Robustelli G., Muto F., Scarciglia F., Spina V.& Critelli S. 2005:

Eustatic and tectonic control on Late Quaternary alluvial fans

along the Tyrrhenian Sea coast of Calabria (South Italy). Quat.

Sci. Rev. 24, 2101–2119.

Robustelli G., Lucà F., Corbi F., Pelle T., Dramis F., Fubelli G., Scar-

ciglia F., Muto F. & Cugliari G. 2009: Alluvial terraces on the

Ionian coast of northern Calabria, southern Italy: implications

for tectonic and sea level controls. Geomorphology 106,

165–179.

Robustelli G, Russo Ermolli E, Petrosino P, Jicha B, Sardella R. &

Donato P. 2014: Tectonic and climatic control on geomorpholog-

ical and sedimentary evolution of the Mercure basin, southern

Apennines, Italy. Geomorphology 214, 423–425

Schiattarella M. 1998: Quaternary tectonics of the Pollino Ridge, Cal-

abria-Lucania boundary, southern Italy. In: Holdsworth R.E.,

Strachan R:A. & Dewey J.F. (Eds): Continental Transpressional

and Transtensional Tectonics. Geol. Soc., London, Spec. Publ.

135, 341–354.

Spina V., Tondi E., Galli P. & Mazzoli S. 2009: Fault propagation in

a seismic gap area 18 (northern Calabria, Italy): Implication for

seismic hazard. Tectonophysics 476, 357–369.

Spina V., Tondi E. & Mazzoli S. 2011: Complex basin development in

a wrench-dominated back-arc area:Tectonic evolution of the

Crati Basin, Calabria, Italy. J. Geodyn. 51, 90–109.

Tansi C., Tallarico A., Iovine G., Folino Gallo M. & Falco

ne G. 2005:

Interpretation of radon anomalies in seismotectonic and tec-

tonic–gravitational settings: the southeastern Crati graben

(Northern Calabria, Italy). Tectonophysics 396, 3–4, 181–193.

Tansi C., Muto F., Critelli S. & Iovine G. 2007: Neogene–Quaternary

strike–slip tectonics in the central Calabrian Arc (southern Italy).

J. Geodyn. 43, 393–414.

Tortorici L. 1981: Analysis of brittle tectonics of post-orogenic sedi-

ments of northern Calabria. Boll. Soc. Geol. Ital. 100, 291-308

(in Italian with English abstract).

Tortorici L., Monaco C., Tansi C. & Cocina O. 1995: Recent and

active tectonics in the Calabrian Arc (southern Italy). Tectono-

physics 243, 37–55.

Tripodi V., Muto F. & Critelli S. 2013: Structural style and tecto-

no-stratigraphic evolution of the Neogene–Quaternary Siderno

Basin, southern Calabrian Arc, Italy. International Geology

Review, doi:10.1080/00206814.2012.723859.

Turco E., Maresca R. & Cappadona P. 1990: Plio–Pleistocene tecto-

nics of Calabria-Lucania boundary (cinematic model). Mem.

Soc. Geol. Ital. 45, 519-529 (in Italian with English abstract).

Van Dijk J.P., Bello M. & Brancaleoni G.P. 2000: A regional structural

model for the northern sector of the Calabrian Arc (southern

Italy). Tectonophysics 324, 267–320.

Westaway R. 1993: Quaternary uplift of southern Italy. J. Geophys.

Res. 98, 21741–21772.

Wortel M.J.R. & Spackman W. 1993: The dynamic evolution of the

Apenninic-Calabrian, Hellenic and Carpathian arcs: a unifying

approach. Terra Nova Abstract 5, 97.

Young J. & Colella A. 1988: Calcarenous nannofossils from the Crati

Basin. In: Colella A. (Ed.): Fan Deltas-Excursion Guidebook.

Università della Calabria, Cosenza, 79–96.

Zecchin M., Praeg D., Ceramicola S. & Muto F. 2015: Onshore to

offshore correlation of regional unconformities in the Plio–Pleis-

tocene sedimentary successions of the Calabrian Arc (central

Mediterranean). Earth-Sci. Rev. 142, 60–78.

Zuffa G.G. 1985: Optical analyses of arenites: influence of methodo-

logy on compositional results. In: Zuffa G.G. (Ed.): Provenance

of Arenites. Dordrecht, The Netherlands, Nato Advanced Study

Institute Series, Reidel 148, 165–189.