GeolCarp_Vol62_No1_65

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA

, FEBRUARY 2011, 62, 1, 65—76 doi: 10.2478/v10096-011-0006-y

Quaternary alluvial fan systems of the Agri intermontane

basin (southern Italy): tectonic and climatic controls

SALVATORE IVO GIANO

Dipartimento di Scienze Geologiche, Basilicata University, Campus Macchia Romana, 85100 Potenza, Italy; ivo.giano@unibas.it

(Manuscript received June 8, 2010; accepted in revised form December 6, 2010)

Abstract: The Agri River high valley is a Quaternary intermontane basin located in southern Italy. The tectonic evolution
of this basin was controlled by Lower Pleistocene strike-slip master faults, subsequently reactivated as normal faults until
the Middle Pleistocene. The Quaternary sediments of the basin infill are mainly constituted of continental clastics, repre-
sented by coarse-grained alluvial deposits divided by unconformities. The arrangement of clastic deposits suggests that the
Pleistocene to Holocene alluvial fan system developed along the eastern margin of the valley. Five generations of slope and
alluvial fan systems have been recognized in the Agri basin. The oldest fans have formed on both slope and alluvial
deposits. The younger alluvial fans are located along the entire valley floor and arose upon the earlier fan apexes originat-
ing in these valleys. The youngest fans are arranged in two different generations and show proximal facies distributed
along the foot slopes. Plan view morphology, fan slope profiles, and sedimentary features of the fan system have been used
here to determine the magnitude of the tectonic deformation episode affecting the faulted mountainous front of the Agri
basin eastern margin. Both fast and slow tectonic episodes occurred during the different regional Quaternary tectonic
stages that affected the southern Apennine chain. These tectonic episodes have therefore been analysed in relation to
climatic conditions in order to determine their contributions to the evolution of the Pleistocene to Holocene fan systems.

Key words: Quaternary, Italy, southern Apennines, tectonics and climate, geomorphology, alluvial fans.

Introduction

There  are  many  studies  regarding  the  role  of  tectonics  and
climate  control  on  both  the  origins  and  the  development  of
Quaternary alluvial fans in the literature (Bull 1967; Silva et
al. 1992; Ritter et al. 1995; Frostick & Reid 1999; Viseras et
al. 2003; Harvey 2004; Harvey et al. 2005; Robustelli et al.
2009). These elements are commonly considered to be very
important  in  understanding  the  recent  evolution  of  young
orogens.

It has long been realized that the controlling factors of

drainage  basin  properties  influence  the  supply  of  water  and
sediment to the fan, and therefore the sedimentary processes
and the resulting fan morphology. However, tectonic control
may  influence  sediment  production  in  the  source  area,  and,
together  with  gross  topography,  appears  to  primarily  influ-
ence fan location, fan setting and gross fan geometry (Harvey
et al. 2005). Furthermore, it has been demonstrated that fan
morphology  and  fan  sediment  sequences  are  dependent  on
tectonics and the amount of accommodation space (Silva et
al.  1992;  Viseras  et  al.  2003).  Recently,  Robustelli  et  al.
(2009)  observed  that  tectonic  and  sea-level  changes  rather
than climate conditions were the main factors in controlling
the sediment/discharge ratio of alluvial fans.

After the Early Pleistocene, the axial zone of the southern

Apennine chain was affected by strike-slip faulting, followed
in Early—Middle Pleistocene by normal faulting. Large inter-
montane basins, including the Agri, Diano, Pergola-Melandro,
Mercure, Sanza, and Noce basins (Schiattarella et al. 2003),
were  produced  by  active  extensional  tectonics  of  the  axial
zone  of  the  southern  Apennine  chain.  These  basins  were
filled  by  coarse  to  fine  continental  deposits  represented  by

different generations of Quaternary alluvial deposits and fan-
related landforms. Differences in basin shape and size were
strongly controlled by the activity of the faulted mountain
front and the transverse drainage.

In order to understand the roles played by short-term tec-

tonic episodes, punctuating longer term tectonic events, and
climatic  stages  on  Quaternary  fan  system  evolution,  strati-
graphic  and  morphological  analyses  have  been  carried  out,
focusing on the eastern side of the Agri intermontane basin.
In this area several generations of slope and alluvial fan sys-
tems, Early—Middle to Late Pleistocene in age, are located at
the  foot  of  a  tectonically  active  mountain  front  (Di  Niro  &
Giano 1995; Giano et al. 2000).

Geological and geomorphological setting

Regional framework

The southern Apennines (Fig. 1a) are a NE-verging oro-

genic  wedge  accreted  from  Late  Oligocene—Early  Miocene
to Pleistocene. The chain is composed of Mesozoic-Cenozo-
ic sedimentary cover arising from the deformation of several
paleogeographic domains (i.e. the Ligurian oceanic crust and
the western passive margin of the Adriatic plate) and of the
Neogene-Pleistocene piggy-back basin, and foredeep depos-
its  of  the  active  margin.  Recent  shortening  has  occurred  on
the belt front deforming Pleistocene sediments and volcanics
(Pieri  et  al.  1997;  Beneduce  &  Schiattarella  1997)  whereas
widely documented extension is still active along the Apen-
nines  axis  (Ortolani  et  al.  1992;  Amato  &  Montone  1997).
The average direction of the chain axis is about N150°, cor-

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responding to the strike of the main thrusts and coaxial nor-
mal  faults.  The  axial  zone  of  the  belt  was  also  affected  by
strike-slip faults trending, mainly N120° ± 10° and N 50°—60°
and by low-angle normal faults (Schiattarella 1998; Schiatta-
rella  et  al.  2003,  and  references  therein)  during  Pliocene—
Pleistocene  times,  extensional  tectonics  characterized  the
Middle  Pleistocene  to  Present  time  interval  (Schiattarella
1998; Giano et al. 2000).

In the area from the Tyrrhenian Sea to the Adriatic

(Apulian) foreland (i.e. from the top to the bottom of the tec-
tonic  stack)  the  following  main  tectonic  units  can  be  seen
(Pescatore  et  al.  1999):  (1)  Jurassic  to  Oligocene  polyde-
formed  ophiolitic  units,  unconformably  covered  by  syntec-

tonic  deposits,  Early  Miocene  in  age  (Liguride
units);  (2)  a  carbonate  platform  unit  (Campania-
Lucania  platform),  whose  age  ranges  from  Late
Triassic to Early Miocene; (3) several units main-
ly composed of deep-sea sediments, ranging from
Lower Triassic to Lower—Middle Miocene (Lago-
negro units); (4) a frontal imbricate fan made up
of Cretaceous to Lower Miocene deep-sea marls,
shales and sandstones covered by Middle to Up-
per  Miocene  flysch  deposits; (5)  Pliocene  to
Pleistocene  foredeep  clastic  deposits; (6)  the
Apulian carbonate platform, which has been part-
ly  incorporated  at  the  base  of  the  accretionary
wedge,  forming  in  an  easterly  direction  the  least
deformed foreland area.

Geological and geomorphological background
of the Agri basin

The upper valley of the Agri River is a NW-SE

oriented intermontane basin located in the Luca-
nian Apennine (Fig. 1a,b). This fault-bounded
basin is about 30 km long and 12 km wide and it
developed during Quaternary times in the axial
zone of the fold-and-thrust belt.

The pre-Quaternary bedrock of the Agri basin

(Fig. 1b) is constituted of Mesozoic to Cenozoic
shallow-water and slope carbonates of the Cam-
pania-Lucania  platform  that  thrusted  on  coeval
pelagic  successions  (Lagonegro  units)  cropping
out along the western and the eastern sides of the
valley, respectively. Toward the East and South-
East the bedrock is composed of Tertiary silici-
clastic  sediments  (Albidona  and  Gorgoglione
Formations),  which  occupy  the  southern  part  of
the  basin.  During  the  Quaternary,  the  Neogene
compressive  structures  were  truncated  by  high-
angle  faults  with  different  kinematics,  which
caused the development of the Agri valley, con-
trolling  depositional  architecture  and  landscape
evolution (Boenzi et al. 2004).

The Pleistocene Agri basin succession crops

out in the southern sector of the basin, and it is
overlain by Holocene deposits in the northern sec-
tor. The outcropping succession consists of conti-
nental clastic sediments, represented by Lower to

Fig. 1. a – Geological sketch map of the southern Apennines (the study area is re-
ported in the frame). Legend: 1 – Plio-Quaternary clastics and volcanics deposits;
2 – Miocene syntectonic deposits; 3 – Cretaceous to Oligocene ophiolite-bearing
internal units; 4 – Meso-Cenozoic shallow-water carbonates of the Apennine plat-
form; 5 – Lower—Middle Triassic to Miocene shallow-water and deep-sea succes-
sions of the Lagonegro units; 6 – Meso-Cenozoic shallow-water carbonates of the
Apulian platform; 7 – thrust front of the chain; 8 – volcanoes. b – Geological
sketch map of the Agri basin.

Upper Pleistocene, coarse-grained talus, and by Middle Pleis-
tocene alluvial deposits (“Complesso Val d’Agri”, Di Niro et
al. 1992). During the Early Pleistocene, the Agri basin devel-
oped in response to left-lateral strike-slip N120° trending mas-
ter  faults,  reactivated  as  normal  faults  after  the  Middle
Pleistocene (Giano et al. 1997; Schiattarella et al. 1998). This
tectonic  regime  is  also  responsible  for  the  development  of
many  Quaternary  intermontane  basins  of  the  southern  Apen-
nines, even though a more complex structural setting has been
suggested  for  the  Agri  valley’s  evolution  (Di  Niro  &  Giano
1995; Giano et al. 1997; Schiattarella et al. 1998; Giano et al.
2000;  Cello  et  al.  2000).  Meso-structural  analysis  performed
on fault planes indicates a recent regime with a NE-SW tensile

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GEOLOGICA CARPATHICA, 2011, 62, 1, 65—76

axis. That such a tectonic regime is still active has been in-
ferred from the regional seismicity and in situ stress measure-
ments (Amato & Selvaggi 1993; Amato & Montone 1997)
and proven by the occurrence of Upper Pleistocene paleosols
involved in faulting (Giano et al. 2000).

Local uplift rates have been computed through the eleva-

tion  of  hanging  relics  of  ancient  landscape  (Paleosurface
Auctt.),  whose  age  is  considered  to  span  from  1.8  to
0.125 Ma.  (Brancaccio  et  al.  1991;  Amato  &  Cinque  1999;
Amato  2000;  Schiattarella  et  al.  2003;  Boenzi  et  al.  2004).
The  values  of  the  Quaternary  local  uplift  rates  range  from
0.4 mm/yr to about 0.7 mm/yr, compared to the regional uplift
rate, equal or higher than 1 mm/yr in the last 1.2 Myr (Schiatta-
rella et al. 2003, and references therein). Due to high slip rates
on  fault  planes  (0.5  to  0.8 mm/yr  in  the  1.2—0.73 Myr  time

span) the major portion of the amplitude of relief can be as-
cribed to the activity of basin-border faults. However, the lo-
cal  morphostructural  offsets  have  to  be  coupled  with
regional  uplift  of  the  orogen  to  obtain  the  total  amount  of
Quaternary uplift. It should be noted that during Late Pleis-
tocene to Holocene times the same fault system was charac-
terized  by  strongly  decreased  slip  rates  of  up  to  0.1 mm/yr
(Schiattarella et al. 2003; Boenzi et al. 2004).

Stratigraphic setting of the Quaternary continental basin-fill

The Agri intermontane basin (De Lorenzo 1898; Di Niro et

al. 1992) is filled by Lower Pleistocene to Holocene continen-
tal clastic deposits (Fig. 2). During the Pleistocene, the deposi-
tional systems changed in time and space from fluvial

Fig. 2. Geological map of the Quaternary deposits crop out in the Agri intermontane basin. The Grumento Synthem is characterized by allu-
vial fan and coeval fluvial plain and lacustrine deposits; the Sarconi and the Villa d’Agri Subsynthems are constituted by coeval alluvial fan
and fluvial plain deposits and by coeval alluvial fan and lacustrine deposits, respectively; the Bosco San Lorenzo Synthem is formed by co-
eval alluvial fan and fluvial deposits. The alluvial fan deposits of each synthem represent the fan systems discussed later in the text.

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(alluvial  fans  and  plain)  to  lacustrine  (Di  Niro  et  al.  1992;
Zembo  2010).  The  stratigraphy  of  the  southern  sector  of  the
Agri basin was first described by De Lorenzo (1898). Di Niro
et  al.  (1992)  informally  called  this  Middle  to  Upper  Pleis-
tocene  interval  the  “Complesso  Val  d’Agri”  and  divided  it
into three sedimentary units (lower, middle, and upper units),
characterized  by  an  overall  coarsening-upward  trend.  More-
over, Di Niro & Giano (1995) improved the Agri basin strati-
graphic  resolution  through  the  recognition  of  coarse-grained
slope deposits, of Early to Late Pleistocene age, cropping out
in the north-eastern and south-western basin margins (“Brecce
di Galaino e Marsicovetere”, Di Niro & Giano 1995; Giano et
al. 1997; “Brecce di Serra Mare” Boenzi et al. 2004).

Recently, Zembo (2010) proposed an allostratigraphic

model for the Agri basin infill introducing the “Agri Valley
Allogroup”. This allogroup cropping out in the southern sec-
tor of the basin, is constituted of four unconformity-bounded
alloformations,  and  overlies  the  Lower  Pleistocene  deposits
of  the  Spinoso  Conglomerate  Alloformation.  Accordingly,
the Agri Valley Allogroup is subdivided, from bottom to top,
into  the  Pietra  del  Pertusillo,  Valle  del  Nasillo,  Vallone
dell’Aspro and Torrente Casale Alloformations.

Carbone et al. (2010) recognized a number of sedimentary

units in the basin infill, by means of the lithostratigraphy and
unconformity  bounded  stratigraphic  unit  approach  (sensu
Salvador  1987),  including  the  Brecce  di  Galaino  and  the
Conglomerati  di  La  Serra  lithostratigraphic  units,  and  the
Pietra del Pertusillo Supersynthem. This latter was itself di-
vided,  from  bottom  to  top,  into  the  Grumento,  the  Bosco
dell’Aspro, and the Bosco San Lorenzo Synthems (Fig. 2). A

correlation between the sedimentary units recognized by
these different authors and the present is reported in Table1.

The Agri basin alluvial fan systems

Depositional setting

The Agri intermontane basin is characterized by Pleisto-

cene to Holocene slope and alluvial fan deposits, all included
in the Pietra del Pertusillo Supersynthem and in the Con-
glomerati di La Serra and Brecce di Galaino Units (Di Niro
et al. 1992; Di Niro & Giano 1995; Giano et al. 2000; Zembo
2010; Carbone et al. 2010). These fan systems crop out
mainly along the eastern basin margin, even though smaller
fan bodies occur in the southern margin (Fig. 2).

The basin-wide unconformities recognized in the Quater-

nary clastic succession of the basin (Di Niro et al. 1992;
Zembo 2010; Carbone et al. 2010) have been partially used
to define alluvial fan sedimentary sequences from coeval flu-
vial and lacustrine deposits. Five Pleistocene to Holocene
fan systems have been recognized within the sedimentary in-
filling of the Agri basin (Figs. 2 and 3).

The Lower to Middle Pleistocene fan sequence (fan

system I) consists of about 20—30 m thick (Fig. 4), coarse-
grained breccias and conglomerates pertaining to the Con-
glomerati di La Serra and Brecce di Galaino Units (Carbone
et al. 2010; Fig. 2 and Table 1). The deposits of fan system I
are mainly composed of two lithofacies. The first one consists
of clast- to matrix-supported, coarse-grained breccias with in-

Fig. 3. Details of the fan deposits crop out in the faulted mountain front of the Agri eastern basin. Fan systems II and III deposits are divided by
an unconformity that crops out between the Casale and Rifreddo Stream mouths (a); faulted coarse-grained deposits of the fan systems I
coming from the Galaino village, note the syntectonic architecture of the breccia deposits and the erosion top surface (b); fan systems III
and IV deposits are divided by a P3 paleosol in the Alli Stream (c); fan systems I and IV deposits are separated by a paleosol of uncertain
attribution near Marsicovetere town (d).

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terbedded  reddish  paleosols;  this  lithofacies  merges  laterally
into roughly stratified fine-grained breccias containing a red-
dish sand or clay matrix. Coarse-grained breccias have sharp
and slightly irregular contacts. Clast shape ranges from angu-
lar to sub-angular, whilst matrix is a mixture of fine to coarse
sands,  containing  terra  rossa-type,  reddish-brown  mud  and
scattered  pebbles.  Breccias  are  stratified  and  locally  massive
(Fig. 3b,d). The second lithofacies consists of polymictic, gen-
erally  massive  conglomerates  containing  a  reddish-brown
clayey matrix. Clast shape ranges from rounded to sub-round-
ed, and the matrix is composed of fine-grained sand, silt and
terra  rossa-type  reddish-brown  clay.  Fine-grained  lenses,  in-
terbedded with conglomerates, randomly occur.

As a whole, the deposits of fan system I form coarse-

grained slope to alluvial depositional systems (Di Niro et al.
1992). Fans were most likely delivered from bedload-domi-
nated, braided channels (Zembo 2010), whereas slope depos-
its resulted from: (i) sediment-gravity flows produced both

by  bedrock  cliff  and  colluvial  slope  failures,  or  (ii)  fluid-
gravity  flows  due  to  colluvial  slope  failures  (Blair  &
McPherson  1994).  These  deposits  can  be  interpreted  as  de-
bris  flows,  and  colluvial  slides  (Type I  fan,  sensu  Blair  &
McPherson 1994). A reddish paleosol (P1, Fig. 4) developed
on the top of fan system I indicates biostasy conditions and a
locally non-depositional statement in the fan.

Middle Pleistocene alluvial fan deposits (fan systems II),

corresponding to the coarse-grained deposits of the Grumen-
to Synthem of Carbone et al. (2010) crop out extensively in
the Agri valley axis (Fig. 2, Table 1). Fan system II deposits,
about  30 m  thick  (Fig. 4),  consist  of  well  to  poorly  sorted
conglomerates with pebble- to boulder-sized clasts in the fan
apex.  In  this  area,  sediments  are  polymictic,  texturally  im-
mature and form normal to inverse grading beds that are lo-
cally massive. Reddish to brown sandy-clayey matrix is also
present.  Fan  toe  deposits  are  formed  by  gravels  alternating
with sandy, trough cross-laminated beds. Silty to sandy lens-
es  also  occur,  locally  showing  soft-sediment  deformation
structures and plant fragments. These deposits are interpret-
ed  as  the  result  of  colluvial  slope  failure  processes.  Sedi-
ment-gravity  flows,  such  as  debris  flows  dominate  the
deposits of the fan apex (proximal fan), whereas fluid-gravi-
ty flows, such as sheetfloods, characterize the fan toe (distal
fan) (Type II fan, sensu Blair & McPherson 1994). Prograda-
tion of fan system II toward coeval lacustrine successions of
the  Agri  basin    occurred  during  the  Middle  Pleistocene
(Di Niro et al. 1992). During the Quaternary, recurrent sub-
aerial exposures affected the top of fan system II, causing the
development  of  paleosols  and/or  erosion  surfaces  (P2,
Fig. 4).  In  particular,  Zembo  (2010)  indicates  a  well-devel-
oped  pedogenic  calcrete  horizon  at  the  top  of  these  fans
which indicates a lack of sediment input for a prolonged pe-
riod and semi-arid to arid climatic conditions.

After the late Middle to Late Pleistocene a new fan growth

episode occurred, producing the alluvial fan sequences of fan
system III. This system consists of coarse-grained deposits of
the  Sarconi  Subsynthem  (Bosco  dell’Aspro  Synthem  of
Carbone et al. 2010; Fig. 2, Table 1). Alluvial fans are located
at  the  eastern  and  southern  basin  margins.  Fan  deposits  are
about 5—10 m thick (Fig. 4) and consist of monomictic, mas-
sive  or  crudely  stratified  conglomerates  in  the  fan  head.  The
clasts  are  of  cobble  to  boulder  size,  and  are  sub-angular  to
rounded with low sphericity in shape. In the fan toe, massive
or normally-graded silty to sandy lenses are interbedded with
gravels,  beds  are  plain  parallel  and  imbricated  clasts  are
present. Normal graded layers of massive silty sands alternat-
ing with sandy silts also occur (Fig. 3a,d), showing local low-
to  high-angle  cross-stratification.  The  fan  head  succession
suggests the occurrence of sediment gravity flows, such as de-
bris  flows,  whereas  the  coeval  fan  toe  deposits  represent  the
results of fluid-gravity flows, such as sheetfloods and incised
channels.  They  are  diagnostic  of  sheetflood-dominated  fans
(Type II fan, sensu Blair & McPherson 1994). A paleosol sev-
eral  meters  thick  (P3,  Fig. 4)  developed  at  the  top  of  fan
system III, suggesting biostasy conditions and low sedimenta-
tion rates over a long time span. Paleosol P3 corresponds to a
mature fersiallitic weathering profile bright brown to reddish-
brown in colour. Pedological features have suggested to Zembo

Fig. 4. Stratigraphic log of Agri basin fan systems and relationships
among the fan deposits.

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(2010) a high degree of pedogenetic evolution in a warm-hu-
mid “Mediterranean-like” climate corresponding to a Late
Pleistocene interglacial phase (Tyrrhenian, MIS 5; Martinson
et al. 1987; Shackleton et al. 2003).

An erosion surface affected the paleosol P3 and was over-

lain  by  a  new  alluvial  fan  sequence  that  produced  the  Upper
Pleistocene fan system IV (Fig. 3c). This alluvial fan system is
closely  adjacent  to  the  north-eastern  Agri  basin  margin
(Fig. 2).  Deposits  consist  of  coarse-grained  conglomerates
corresponding to the Upper Pleistocene Villa d’Agri Subsyn-
them  (Bosco  dell’Aspro  Synthem  of  Carbone  et  al.  2010;
Fig. 2, Table 1). The succession, about 20 m thick (Fig. 4), is
composed of coarse-grained, massive conglomerates, that are
polymictic,  poorly  sorted  and  clast-supported  with  reddish-
brown  clayey  sand  matrix.  Interbedded,  massive  gravelly  to
fine-grained sand lenses rarely occur. Depositional features in-
dicate  sediment-gravity  flows  produced  by  colluvial  slope
failure processes, feeding debris-flow-dominated fans (Type I
fan, sensu Blair & McPherson 1994). A deep weathered pro-
file,  developed  at  the  top  of  fan  system IV  (P4,  Fig. 4),  con-
sists  of  a  thick  reddish-brown  pedological  complex.  These
paleosols,  classified  as  two  transitional  brunified-fersiallitic
paleosols  by  Zembo  (2010),  may  suggest  a  transition  from
dry-cold to humid-warm climate during the MIS3 interglacial.

The most recent fan growth, Holocene in age, led to fan

system V. Fan deposits, about 10 m thick (Fig. 4), consist of
matrix- to clast-supported cobble to boulder sized conglom-
erates. Clast shape ranges from angular to sub-rounded. Sand
lenses  and  organic-rich  horizons  are  also  interbedded
(Fig. 3d).  Fan  system  V  is  the  uppermost  interval  of  the
Bosco  San  Lorenzo  Synthem  of  the  Carbone  et  al.  (2010)
(Fig. 2, Table 1). It crops out close to the faulted basin mar-

gin and at the base of the oldest incised fan system, forming
coalescent  fans  (Fig. 5).  Coarse-grained  deposits  indicate
sediment-gravity  flows  produced  by  bedrock  cliff  failures
and  are  diagnostic  of  debris-flow-dominated  fans  (Type I
fan, sensu Blair & McPherson 1994). Fan sedimentation oc-
curred  in  the  deepened  valleys  incised  by  fluvial  network
during  the  Late  Pleistocene  tectonic  stage.  Both  OSL  and
AMS

C dating on fan deposits fix the absolute age between

5.2 ± 0.5 ka and 3.3 ± 0.45 ka BP (data from Zembo 2010).

Geomorphological features

The eastern Agri basin is characterized by a faulted moun-

tain front that has controlled the shape, morphology and sed-
imentary  evolution  of  the  basin  from  Early—Middle
Pleistocene up to the present (Di Niro & Giano 1995; Giano
et  al.  2000).  Moreover,  historical  seismicity  shows  that  the
study  area  has  been  affected  by  recurrent  and  large  earth-
quakes  such  as  the  1857  Basilicata  Earthquake.  Several  su-
perimposed  alluvial  fans  (sensu  Blissenbach  1954)  with
different  morphological  features  and  ages  (Fig. 5a,b)  were
produced during the Quaternary evolution of the Agri basin.
All  the  fans  have  been  dissected,  partially  dissected  or  not
incised  by  fluvial  networks  at  the  Present-day  (Fig. 6),  and
the  amount  of  fluvial  deepening  varies  from  about  43 m  in
the Rifreddo Stream Valley to a few meters in the Molinara
Stream Valley (Fig. 7). A comparison of both slope and in-
cised channel fan profiles of the Casale, Rifreddo, Alli, and
Molinara Streams (Fig. 7) reveals that fluvial deepening has
only occurred in the Rifreddo and Casale Streams and not in
the  Alli  and  Molinara  Streams.  With  regard  to  fan  toe,  the
amount  of  dissection  of  the  Rifreddo  and  Casale  Streams

Table 1: Comparison among this and previous studies on the valley fill deposits of the Agri basin.

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ranges from about 43 to 50 m and from about 30 to 45 m, re-
spectively. The shifting of the vertical deepening in these
streams was produced by an incomplete backwearing of the
stream channel network of the Agri basin.

In order to differentiate between the various generations of

the fan systems of the Agri basin, plan view topographic
contour and radial slope profile analyses have been carried
out. Plan view extension of the eastern basin margin shows
an irregular distribution of fan systems, coalescing to form a
narrow bajadas (Fig. 5a,b).

As suggested by Keller & Pinter (1996), alluvial fans are

conical in shape under geometrically-simple and tectonical-
ly-stable  conditions.  Topographic  contours  across  a  cone-
shaped  fan  are  similar  to  segments  of  evenly  spaced
concentric circles. It has also been recognized that if a coni-
cal fan is tilted, contour lines across the fans form segments
of ellipses and not of circles. Plan view extension of the Agri
basin  fan  systems  shows  that  the  topographic  contour-lines
across fan systems III, IV, and V do not correspond to seg-
ments of concentric and evenly spaced circles, but rather to
ellipses (Fig. 5b). Therefore, it is possible to surmise that the
evolution of these fan systems was controlled by the tectonic
activity  of  the  mountain  front  during  the  late  Middle  Pleis-
tocene to Holocene time span. Moreover, the development of
fan system I was also controlled by the Early Pleistocene tec-
tonic  activity  (Figs. 3b,  5a)  and  its  first  plan  view  contour-
line  has  not  been  preserved  in  the  present-day  landscape.
Unfortunately, no data on tectonic rates (fast or slow tectonic
episodes) can be provided from topographic contour-lines of
the fan systems I, III, IV, and V. On the other hand, no mor-
phological  features  have  been  obtained  from  fan  system II
plan view analysis, because it has been almost entirely bur-
ied by the younger fan system III deposits (Fig. 5a,b).

Topographical surveys indicate that the fan system areas

are  clearly  superimposed  and  show  a  decrease  in  area  from
fan system II to fan system V. On the other hand, an increase
of plan view area can be seen moving from fan system I to
fan system II (Fig. 5a,b). Furthermore, fan systems II and III
have large  plan view areas and show a low fan slope gradi-
ent  (Fig. 8).  On  the  contrary  fan  systems I,  IV,  and  V  have
small plan view areas and exhibit an high fan slope gradient
(Figs. 5a,b,c,d  and  8).  In  a  faulted  mountain  front,  rapid
hanging  wall  subsidence  and  footwall  uplift  produce  small
piedmont  fans  and  proximal  axial  rivers,  whereas  a  slower
deformation leads to large, low-gradient fans and distal axial
rivers  (Burbank  &  Anderson  2001).  Accordingly,  during
each  of  the  several  Quaternary  long-term  tectonic  stages  of
the southern Apennines which have affected the Agri basin,
a short-term fast tectonic episode of the mountain front could
have  controlled  the  development  of  the  smaller  fan
systems I, IV, and V. On the contrary, a short-term slow tec-
tonic episode of the mountain front could have occurred dur-
ing  the  evolution  of  the  larger  fan  systems II  and  III
(Fig. 5a,b).

Alluvial fans of the Agri basin are characterized by a

slightly concave-upward slope profile divided by several
clear break-in-slopes that permit the detection of different ra-
dial segments (Fig. 8). Concave-upward slope profiles of the
Galaino, Molinara, Alli, Casale, and Rifreddo fans (Fig. 8)

Fig. 7. Longitudinal fan slope profiles and incised channels of the
Molinara, Alli, Casale, and Rifreddo Streams.

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GEOLOGICA CARPATHICA, 2011, 62, 1, 65—76

have  been  divided  into  several  straight-line  segments  (Bull
1977).  Four  straight-line  segments  have  been  inferred  from
the  Casale  and  Rifreddo  fans,  three  from  the  Alli  one,  and
only  two  segments  from  the  Molinara  and  Galaino  fans
(Fig. 8). There is a decrease in the slope angle between two
adjacent  segments  of  the  fan  profile  in  a  downward  direc-
tion. Moreover, this break-in-slope profile can also be drawn
as  a  curve  in  plan  view,  along  the  topographic  contour-line
of fans (Fig. 5a,b), and may be interpreted as a depositional
fan surface. The occurrence of stratigraphic markers (i.e. ero-
sion surface, weathered profile and/or paleosols) on the top-
surface  of  fans  also  suggests  the  interpretation  of  the
straight-line segment as the top of the sedimentary fans.

Since similar coarse-grained sedimentation characterized

fan systems I to V, a comparable angle of the straight-line seg-
ments forming the slope profile of the fan could be expected
(Fig. 8).  The  discrepancy  between  the  angles  of  the  straight-
line  segments  observed  from  the  fan  slope  profile  (Fig. 8)
could  be  attributed  to  the  rate  of  Quaternary  uplift  of  the
mountain front during the long-term tectonic stages (Schiatta-
rella et al. 2003; Boenzi et al. 2004). In particular, a fast tec-

tonic episode could be responsible for the high-gradient slope
profiles  of  fan  systems I,  IV,  and  V  (Fig. 8).  Conversely,  a
slow  tectonic  episode  could  produce  the  low-gradient  slope
profiles  of  fan  systems II  and  III  (Fig. 8).  Therefore,  the
straight-line segments observed from the fan slope profile can
be  interpreted  as  tectonically  controlled  depositional  fan  sur-
faces (Fig. 8).

Discussion and conclusions

Although tectonics and climate are the primary factors in

controlling  alluvial  fan  evolution  (Bull  1977;  Frostick  &
Reid 1989; Silva et al. 1992; Ritter et al. 1995; Viseras et al.
2003; Harvey 2004; Robustelli et al. 2009), it is often more
difficult  to  determine  their  relative  roles.  Harvey  et  al.
(2005)  suggest  that  fan  evolution  is  controlled  by  both  cli-
matic  change  and  tectonic  processes  over  different  times-
cales  of  10

—10

years and in excess of 10

years,

respectively. However, it should also be considered that the
magnitude of tectonic activity is not constant over time and

Fig. 8. Fan slope profiles and straight-line segments represent-
ing the superimposed depositional fan surfaces. All the deposi-
tional fan surfaces are tectonically controlled by faulting activity
of the eastern mountain front of Agri basin.

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Fig. 9. Synoptical scheme showing the morpho-sedimentay features
(on the left column) and the tectonic/climatic control (on the right
column) of the development of the Agri basin fan systems.

space, and thus alternating periods of fast and slow short-
term deformation occur during a longer term tectonic stage.
In this way, the magnitude of the short-term tectonic defor-
mation could interact with climate at the same timescale
(10

—10

years), and thus the interplay between climate and

rapidity of deformations could be observed and compared by
means of morphosedimentary analysis of fans.

In the Quaternary Agri basin (Di Niro et al. 1992; Di Niro &

Giano 1995; Giano et al. 2000; Schiattarella et al. 2003; Boenzi
et al. 2004; Zembo et al. 2009; Carbone et al. 2010), a com-
parison between slow/fast tectonic activity of a mountain front
versus  climatic  control  on  the  fan  system  development  has
been  carried  out  (Fig. 9).  All  sedimentary  fan  bodies  of  the
study  area  are  characterized  by  coarse-grained  deposits
(Figs. 3 and 4) that seem to reflect a strong tectonic control on
their evolution (Frostick & Steel 1993; Kumar et al. 2007). In
particular,  the  debris-flow-dominated  fans  (Type I  fan,  sensu
Blair & McPherson 1994) of fan systems I, IV, and V indicate
rapid  sedimentation,  linked  to  a  fast  tectonic  episode  of  the
mountain front, whereas both the debris-flow- and sheetflood-
dominated fans (Type II fan, sensu Blair & McPherson 1994)
of  fan  systems II  and  III  suggest  lower  sedimentation  pro-

duced  during  a  slow  tectonic  episode  of  the  mountain  front.
On  the  contrary,  unconformities  within  the  fan  systems  sug-
gest that sedimentation decreased and fan head entrenchment
likely occurred. Moreover, weathered horizons and paleosols
indicate a lack of sedimentation in the basin and different cli-
matic  conditions  during  their  evolution.  Morphological  fea-
tures  (plan  view  extension  and  slope  profile)  of  the  alluvial
fans indicate that a slow tectonic deformation was responsible
for  the  growth  of  large  fan  systems,  including II  and  III
(Figs. 5a,b  and  8),  whereas  a  fast  tectonic  deformation  con-
trolled smaller systems, such as the I, IV, and V fans.

A first tectonic stage (Early Pleistocene) affected the study

area, causing a regional uplift rate of about 0.8 mm/yr that was
not constant over time (Schiattarella et al. 2003; Boenzi et al.
2004). In fact, within a regional tectonic stage, the magnitude
of uplift varies from fast to slow tectonic episodes. This uplift
marked  both  the  initial  asymmetrical  basin  opening  and  the
creation of accommodation space for deposition of the coarse-
grained  fan  system I  (Di  Niro  &  Giano  1995;  Giano  et  al.
2000). Fans were deformed and uplifted by tectonic episodes
(Giano et al. 1997), and consequently the present-day fan sur-
face  does  not  approximate  classical  concentric  fan  circles
(Fig. 5a), and shows a high fan slope gradient (Fig. 8). A fast
tectonic  episode,  included  in  the  Early  Pleistocene  tectonic
stage of the southern Apennines, directly controlled fan-shape,
fan-slope profile, and sediment yield, having greater influence
than climatic control during the same time interval (Fig. 9). In
fact,  coarse-grained  deposits  and  a  reduced  fan  extension
show that fast deformation occurred during this tectonic stage.
In contrast, a break in the tectonic uplift and a decrease in the
sedimentation  rate  produced  a  development  of  a  reddish  pa-
leosol (P1 in Fig. 4) on the top of the Brecce di Galaino Units.
This paleosol could be indicative of the dominance of climatic
factors in the tectonic deformation of fan system I.

Since the Middle Pleistocene, the regional uplift rate of the

southern Apennine chain has been about 0.6 mm/yr on aver-
age (Amato 2000; Schiattarella et al. 2003). In the Agri ba-
sin,  the  long  wavelength  tectonics  (i.e.  regional  uplift  rate)
punctuated  by  local,  shorter-term  faulting  rates  (about
0.5 mm/yr: Schiattarella et al. 2003; Boenzi et al. 2004), pro-
duced  the  accommodation  space  for  the  deposition  of  fan
system II.  Furthermore,  the  non-concentric  and  evenly
spaced  circles  deduced  from  fan  system IV  (Fig. 5b,c)  also
indicate  this  tectonic  activity,  but  they  do  not  provide  data
about  the  tectonic  rates.  Very  large  cone-shaped  fans  with
low-gradient  slopes  developed  and  coarse-  to  fine-grained
deposition took place from the fan head to the fan toe. The
fan  deposits,  interpreted  as  type II  fans  (sensu  Blair  &
McPherson  1994),  migrated  downstream  to  the  lacustrine
and  fluvial  plain  environments,  testifying  a  good  degree  of
organization of the paleo-depositional setting and steady tec-
tonics. In contrast to the major uplift rate which occurred in
the  Agri  basin  during  the  Middle  Pleistocene,  the  morpho-
logical and sedimentary features of the fans suggest that they
were influenced by a slower tectonic episode, included in the
Middle Pleistocene tectonic stage of the southern Apennines.

Moreover, the occurrence of lacustrine facies of the Gru-

mento Synthem (Fig. 2) suggests the existence of climatic
control in fan development which exceeded the influence of

QUATERNARY ALLUVIAL FAN SYSTEMS OF THE AGRI INTERMONTANE BASIN (SOUTHERN ITALY)

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GEOLOGICA CARPATHICA, 2011, 62, 1, 65—76

the tectonic episode (Fig. 9). The occurrence of a pedogenic
calcrete horizon on the top surface of fan system II (P2 in
Fig. 4) indicates the end of the fan system formation. A tec-
tonic quiescence and a low sedimentation rate probably took
place at this moment.

Active faulting during the late Middle to Late Pleistocene

tectonic stage of the southern Apennine chain produced a lo-
cal uplift rate of about 0.7 mm/yr (Boenzi et al. 2004), caus-
ing  the  widening  of  the  Agri  basin  and,  consequently,  the
development  of  fan  system III.  The  Upper  Pleistocene  red-
dish  paleosol  which  developed  on  the  top  surface  of  fan
system III (P3 in Fig. 4) corresponds to the fersiallitic paleo-
sol assigned to MIS5 from Zembo (2010). This dating leads
to a consideration of these fan deposits as older than 125 kyr.
Morphological (large cone-shaped fans in plan view and low
fan slope profile) and sedimentary (Type II fans, sensu Blair
&  McPherson  1994)  evidence  suggests  that  a  slow  tectonic
deformation  episode  took  place  during  the  development  of
fan system III. A good degree of internal organization of the
proximal  and  distal  sedimentary  facies  suggests  significant
climatic control in the development of fan system III. There-
fore,  morpho-sedimentary  features  indicate  that  climate  is
the  primary  controlling  factor  on  fan  evolution  rather  than
tectonics (Fig. 9).

A Late Pleistocene tectonic stage produced a new uplift of

the Agri basin’s eastern margin (Giano et al. 2000) generating
the development of fan system IV. Absolute dating of this sys-
tem fixes between 56 ± 4 ka and  ~ 32 ka (Zembo 2010) as the
age of its development. Coarse-grained deposits, produced by
colluvial slope failure processes, characterized the deposits of
fan  system IV,  interpreted  as  debris-flow-dominated  fans
(Type I fan, sensu Blair & McPherson 1994). These fans are
also  characterized  by  a  reduced  plan  view  extension  and  a
high-angle slope profile (Figs. 5a,b,c,d and 8). These morpho-
sedimentary  features  are  an  indication  of  a  fast  tectonic  epi-
sode  which  occurred  during  the  Late  Pleistocene  tectonic
activity  ( ~ 24 kyr).  Accordingly,  it  is  suggested  that  a  rapid
tectonic  episode  had  more  significant  consequences  than  cli-
matic  conditions in the evolution of fan system IV. The deep-
ening  of  the  Agri  basin  fluvial  network  and    fluvial  back
wearing began at the end of the deposition of fan system IV.

Late Pleistocene to Holocene tectonic activity of the eastern

Agri basin margin was characterized by a strongly decreasing
fault  slip  rate  down  to  0.1 mm/yr  (Schiattarella  et  al.  2003;
Boenzi et al. 2004). Therefore, a lower and local rate of tec-
tonic displacement controlled the development of fan system
V during the Holocene. On the contrary, debris-flow-dominat-
ed  fans  (Type I,  sensu  Blair  &  McPherson  1994),  associated
with reduced plan view fan extension and not concentric cir-
cles with high-angle profiles indicate a quicker tectonic defor-
mation  episode.  This  apparent  discrepancy  between  a  low
uplift rate and a fast tectonic deformation could be explained
by a high sedimentation rate probably related to a momentary
increase in the fluvial discharge produced by a strong sudden
tectonic episode. Therefore, if this hypothesis is true then also
in the case of fan system V, the tectonic signal has greater in-
fluence than that of climatic control.

In conclusion, within the framework of the Quaternary tec-

tonic stages affecting the southern Apennines, both the mag-

nitude (fast or slow rate) of the tectonic episodes and the cli-
matic conditions were responsible for the development of the
alluvial fan systems of the Agri basin (Fig. 9).

Acknowledgments:  I  would  like  to  thank  M.  Schiattarella
for his helpful suggestions in the field, S. Longhitano for im-
provements in the English of the text, and Rosalind Innes for
revision  of  the  English  language.  Author  also  thank  G.  Ro-
bustelli  and  J.  Minár  for  their  precious  comments  and  con-
structive revision of the manuscript.

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