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LATE-QUATERNARY ALLUVIAL FANS IN THE NORTHERN MARCHE APENNINES:
IMPLICATIONS OF CLIMATE CHANGES 

Olivia Nesci, Daniele Savelli , Francesco Troiani  
Dipartimento di Scienze dell’Uomo, dell’Ambiente e della Natura, Università “Carlo Bo”, Urbino 

Corresponding author: F. Troiani <francesco.troiani@uniurb.it

ABSTRACT: O. Nesci O. et al., Late Quaternary alluvial fans in the northern Marche Apennines: implications of climate changes. (IT
ISSN 0394-3356, 2010)
Alluvial fans, fan-like deposits, and piedmont aprons are widespread at mountain-front and foothill sectors of the Umbria-Marche
Apennines. They are currently regarded as significant geomophological features strictly dependent on either tectonic or climatic con-
trols. Close relationship with tectonics, that are usually stressed by the location of such landforms along fault scarps or other active
morphostructures, can be assessed only in the most internal areas of the Umbria-Marche Apennines, dissected by extensional tecto-
nics. Conversely, in the piedmont and foothill sectors of the chain, the climatic control on fan deposition and entrenchment become
dominant, whereas tectonic constrains can be only indirectly detected. Namely, within the Umbria-Marche Apennines, the late
Quaternary cyclical and systematic episodes of fan deposition and entrenchment at the mouth of tributaries, usually following the
main fluvial filling along the trunk valleys, are well known. Nonetheless, the main causes that have cyclically controlled the fluvial and
alluvial-fan deposition and their subsequent dissection have not been thoroughly investigated yet. In this work we report a general
overview on the geomorphological setting of the late Quaternary alluvial fans associated with the major fill-terraces that compose the
typical staircase of river terraces in the Northern Marche territory. In particular, for the aggradational suites of the late Quaternary fill-
terraces, we discuss the meaningful stratigraphic relations between the fluvial sediments of the trunk streams and the alluvial-fan
deposits originating from the tributaries. 
We also suggest a possible correlation between the cyclical recurrence of the principal episodes of fluvial aggradation/alluvial-fans
formation and  dissection and the principal late Quaternary climate fluctuations. 

RIASSUNTO: Nesci O. et al., Conoidi alluvionali tardo Quaternarie nell’Appennino Marchigiano settentrionale: implicazioni paleo-cli-
matiche. (IT ISSN 0394-3356, 2010)
Conoidi alluvionali tardo quaternarie (isolate e/o coalescenti) sono ampiamente diffuse lungo il fronte montuoso e l’area pedemontana
dell’Appennino Umbro-Marchigiano. Le conoidi alluvionali sono correntemente considerate come significativi elementi geomorfologici
in stretta connessione con la tettonica e/o con controlli di tipo climatico. Relazioni molto strette con la tettonica attiva, generalmente
evidenziate dalla localizzazione delle conoidi lungo scarpate di faglia o altre morfostrutture attive, sono riconoscibili solo nelle aree
interne dell’Appennino Umbro-Marchigiano, interessante da tettonica attiva di tipo estensionale. Al contrario, lungo i settori pedemon-
tani della catena è più evidente il controllo climatico sulla deposizione e successiva dissezione degli apparati di conoide alluvionale,
mentre il controllo da parte della tettonica può essere riconosciuto solo in parte e indirettamente. Lungo l’Appennino Marchigiano set-
tentrionale, dove è incentrato il presente lavoro, da molto tempo è nota in letteratura la ciclica e sistematica ripetizione, in corrispon-
denza delle foci dei tributari, di alterne fasi di deposizione e re-incisione di conoidi alluvionali, le quali seguono sistematicamente fasi di
aggradazione fluviale lungo i corsi d’acqua principali. Nonostante ciò, le cause principali che hanno ciclicamente controllato la deposi-
zione di ampi apparati di conoide e la loro successiva re-incisione, ancora oggi non sono state studiate nel dettaglio. Nel presente
lavoro viene descritto in alcune aree campione l’assetto geomorfologico delle conoidi alluvionali tardo quaternarie associate ai princi-
pali terrazzi deposizionali componenti la tipica successione di terrazzi fluviali all’interno delle principali valli marchigiane settentrionali. In
particolare, vengono descritti in dettaglio i rapporti stratigrafici esistenti all’interno dei principali corpi alluvionali, di età compresa fra il
Pleistocene medio e il Pleistocene superiore, fra le sequenze deposizionali di tipo fluviale appartenenti al corso d’acqua principale e
quelle di conoide alluvionali presenti alla foce dei principali tributari.
Gli episodi che hanno portato alla formazione di ampi sistemi deposizionali di conoide alluvionale nei bacini marchigiani settentrionali
sono ciclici e seguono sistematicamente le maggiori fasi di aggradazione fluviale lungo i corsi d’acqua principali. I depositi fluviali, fatta
eccezione per i settori a ridosso dell’attuale fascia costiera, sono preservati nei principali terrazzi vallivi e vengono generalmente consi-
derati come episodi deposizionali direttamente connessi con i principali cicli glaciali. Alla stessa maniera dei depositi fluviali lungo le
valli principali, anche la deposizione e successiva reincisione degli apparati di conoide in corrispondenza delle confluenze dei tributari
con il corso d’acqua principale sono da ritenersi strettamente connessi con le principali fluttuazioni climatiche tardo quaternarie.
Inoltre, quando all’interno di un corpo alluvionale terrazzato i depositi strettamente fluviali coesistono con quelli di conoide alluvionale,
fra le due tipologie di deposito esistono relazioni stratigrafiche precise e sistematiche. In particolare, i depositi di conoide seguono
sistematicamente quelli fluviali; normalmente la transizione fra i depositi di conoide e quelli fluviali consiste in una rapida (fino a 2-3 m
di spessore) interdigitazione di facies o, a volte, in limiti netti (anche di tipo erosivo). In ogni caso, i depositi di conoide giacciono gene-
ralmente sulla superficie non ancora rimodellata dei sottostanti depositi fluviali. Il ripetersi ciclico delle fasi deposizionali ed erosive, l’e-
sistenza di precise e sistematiche relazioni stratigrafiche fra i due depositi e la disponibilità in letteratura, almeno per i depositi più
recenti (Pleistocene superiore), di numerose età numeriche, hanno permesso di ipotizzare, tenendo anche in considerazione le analisi
già effettuata per aree limitrofe e disponibili in letteratura, alcune correlazioni con le principali fluttuazioni climatiche tardo quaternarie.

Parole chiave: River terraces, Alluvial fans, Climatic controls, Northern Marche Apennines.

Keywords: Terrazzi fluviali, Conoidi alluvionali, Controllo climatico, Appennino nord Marchigiano.

Il Quaternario
Italian Journal of Quaternary Sciences
23(1), 2010 - 145-156



146 O. Nesci, D. Savelli & F. Troiani

1. INTRODUCTION

Alluvial fans are regarded by current literature as
important geomorphological features in mountain-front
and foothill settings, usually hinting at alternate phases
of aggradations and entrenchment strictly dependent

on tectonic and/or climatic control (e.g., BULL, 1977;
HARVEY, 1984; HARVEY et al., 2005; SURESH et al., 2007
and reference therein). Tectonic controls are commonly
regarded as crucial to rule both sediment load and cat-
chment relief, promoting aggradation at the mountain-
front and foothills (e.g., DAVIS, 1905; BLISSEMBACH, 1954;

BULL, 1964; DE CELLES et al.,
1991; HARTLEY, 1993; VISERAS et
al., 2003). Equally, climate is
considered to play a fundamen-
tal role in setting the rate of
sediment supply, relief equili-
brium, and fan geometry (e.g.,
LUSTING, 1965; HARVEY, 1990,
1996; R ITTER et al ., 1995;
R OBERTS, 1995). Whether at
fronts of high-relief areas or at
tributary stream junctions, allu-
vial fans develop where a pro-
per accommodation space for
deposition exists, and high sedi-
ment loads encounter zones of
reducing stream power (HARVEY,
2004) because of gradient lowe-
ring and, above all, of dimini-
shed flow confinement (SCHUMM,
1977). Moreover, the rate of
both sediment supply and cat-
chment erosion is rather related
to stream-power which, in turn,
is generally a function of preci-
pitation intensity (SURESH et al.,
2007). Hence, the formation and
dissection of alluvial fans in a
given area is ruled by a complex
interlacement of climate-related
and tectonic-geologic factors,
whose mutual relationships and
timing are often hard to unravel.

This paper reports some
representative examples from
the mountain-front and foothill
sectors of the Adriatic side of
the northern Marche Apennines
(Fig. 1) in order to emphasize
the close relationships in this
area of systematic construction
and dissection of wide alluvial
fans with late Quaternary clima-
te changes.

2. RIVER TERRACES IN THE
MARCHE APENNINES

The Marche Apennines con-
sist of a NE-verging thrust-and-
fold belt involving a stratigraphic
succession characterized by
Mesozoic calcareous to marly-
calcareous terrains overlain by
Cenozoic dominantly terrige-
nous terms (D EIANA & P IALLI,
1994). A series of sub-parallel
ridges and topographic depres-

Fig. 1 - Location map. A) The study area in the morphostructural framework of the Marche
Region. B) Shaded relief map of the study area with location of sample areas described in the
text and outcrops shown in Figure 5.

Ubicazione dell’area e dei siti descritti nel testo . A) L’area studiata nel contesto morfostruttura-
le del territorio marchigiano. B) DTM dell’area analizzata con l’ubicazione delle aree campione
descritte e degli affioramenti illustrati in Figura 5.



sions (Fig. 1), resulting from crustal shortening and
extension driving the topographic emergence of the
chain over the last three million years, generally match,
respectively, the main calcareous anticlines and terrige-
nous synclines (CALAMITA et al., 1991). Since the Lower
Pleistocene the area underwent a generalized tectonic
uplift (BISCI & DRAMIS, 1991; DRAMIS, 1992; D'AGOSTINO et
al., 2001) gradually achieving its definitive emersion.

The modern trunk valleys, characterized by an
overall parallel pattern, perpendicular to the structural
grain (MAZZANTI & TREVISAN, 1978; ALVAREZ, 1999), began
to develop since the Messinian with the first stages of
emersion, but achieved a configuration quite similar to
the modern one in the lowermost part of the Middle
Pleistocene, with the definitive emersion of the area
(MAYER et al. 2003). 

147Late-Quaternary alluvial fans ...

The Marche region holds an excellent preserva-
tion of late Quaternary valley terraces and a large num-
ber of terrace-alluvium exposures, supported for a long
time by a great deal of scientific work (e.g., LIPPARINI,
1939; VILLA, 1942; SELLI, 1954; NESCI et al., 1995; COL-
TORTI et al., 1991; BISCI & DRAMIS, 1991; FANUCCI et al,
1996; WEGMANN & PAZZAGLIA, 2009). Particularly, in the
central and northern sector of the Marche region, cycli-
cal stages of alluvial fans and piedmont-aprons forma-
tion and dissection have been reported in close relation
(Fig 2) with the valley terraces development (e.g., NESCI
& SAVELLI, 1986; NESCI et al., 1995). The trunk valleys
show at least four “orders” of alluvial terraces, ranging
from Middle Pleistocene to Upper Pleistocene in age
(cf. fig. 6), and designated respectively, from the older
and higher one, as T1A, T1B, T2, and T3 (NESCI et al.,

Fig. 2 - Composite topographic profiles and cross sections transversal to the trunk-valley axis displaying the arrangement of the prin-
cipal alluvial-fan deposits in the frame of the major valley terraces in some selected areas of the northern Marche Apennines. The stra-
tigraphic relationships with the fluvial fills along the trunk valleys are also shown. Location of profiles in Figure 1B.
Profili compositi trasversali agli assi vallivi che evidenziano la posizione dei principali depositi di conoide alluvionale nel contesto dei
maggiori terrazzi vallivi in alcune aree campione dell’Appennino Marchigiano settentrionale. Sono evidenziati anche i rapporti stratigrafi-
ci dei depositi di conoide alluvionale con i sedimenti delle colmate fluviali degli assi vallivi principali. Ubicazione dei profili in Figura 1B.



148

1990, 1995; FANUCCI et al., 1996). They are characteri-
zed by thick alluvial covers, often exceeding 30 metres
in thickness for the only sediments supplied by the
trunk-valley, i.e. without the alluvial-fan additional com-
ponent which, in turn, varies in thickness from a few
metres (fine grained fans, NESCI & SAVELLI, 1991) up to
25-30 metres (pebbly fans). These terraces are prece-
ded by a complex suite of strath terraces, which, accor-
ding to genetic mechanisms already described by BULL
(1992), have been interpreted as related to tectonic fac-
tors (FANUCCI et al., 1996). Conversely, as regards the
T1A-T3 terraced alluvial suites with which this paper is
concerned, they are usually retained to be the result of
as many complex, for the most part climatically-driven,
aggradation episodes, alternating with likewise com-
plex stages of predominant stream downcutting (e.g.,
CALDERONI et al., 1991, 1992; COLTORTI et al., 1991; NESCI
& SAVELLI, 1990; 1991; NESCI et al., 1995; CILLA et al.
1996; COLTORTI, 1997; WEGMANN & PAZZAGLIA, 2009).
Being here T1A and T1B reported as two main distinct
terraces, it is worth emphasizing that this subdivision of
the traditional “first order of terraces” (cf. LIPPARINI,
1936; VILLA, 1942 and following Authors) in two distinct
main stages of terrace development -i.e. with the same
“hierarchic range” of the already distinguished 2nd and
3rd “orders of terraces” has been introduced by NESCI et
al. (1990) just for the Metauro and Foglia river basins
(the two principal catchments of
the northern Marchean area),
where the traditional “first
order” revealed to be unsuitable
to describe the altimetric distri-
bution of the oldest terrace-allu-
vium which, as a matter of fact,
accounts for two main, distinct
stages of terrace formation.

As regards the alluvial fill
stages related to the principal
terrace units, the four main
aggradation stages already
recognized by NESCI et al. (1990,
1995), match in a good way with
the principal stages already
described by WEGMANN & PAZZA-
GLIA (2009) (Fig. 6). The principal
episodes of aggradation took
place during the major stages of
late Quaternary climatic cooling
and, generally, they were not
continuous but often complica-
ted by repeated minor episodes
of cut-and-fill process (NESCI et
al., 1995; E LMI et al., 2003).
During the intervening late
Quaternary warmer stages, as
well as during the Holocene,
because of the effect of both
climate change and generalized
tectonic uplift, stream down-
cutting and entrenchment
exceeded valley aggradation
leading to the formation of well-
developed flights of alluvial ter-
races (e.g., NESCI et al., 1995; DI
BUCCI et al., 2003; WEGMANN &

PAZZAGLIA, 2009) which are often exposed along both
trunk and tributary valleys, up to 150 meters high above
the present valley-floors.

3. ALLUVIAL FANS IN THE MARCHE APENNINES:
OVERVIEW

The above delineated comprehensive framework
is thus inclusive of the late Quaternary alluvial fans of
the northern Marche area. Specifically, in this general
context, NESCI & SAVELLI (1986, 1990) stressed the
systematic recurrence in the cycles of valley-terrace
development of peculiar erosional-depositional steps.
These steps are repeated quite unvaried in the T1A-T3
cycles of aggradation-dissection, to such an extent that
NESCI & SAVELLI (1986 and following) called them “guide
stages”/“guide deposits” to signify something hinting at
a precise position in the cycle itself. Hence, the valley
fill resulted in a first aggradational step consisting of
coarse sediments of braided rivers, even though rather
complicated by subordinate cut-and-fill episodes (CAL-
DERONI et al, 1991) and/or by the local occurrence of dif-
ferent channel-patterns (CALDERONI et al, 1992). The
second step of the trunk-valleys aggradation consists,
in turn, just in a tributary-junction related construction
of alluvial fans (cf. Fig. 2, 3 and 5) above the previous

Fig. 3 - Block-diagram showing the of formation (2) and dissection (3) of a wide late
Pleistocene alluvial fan on the right side of the Metauro River valley, c.ca 1 km upstream
Fossombrone. Stages A1, A2, E1 as in Figure 6. Location in Figure 1B. After SAVELLI et al.
(1984), simplified.

Block-diagramma che illustra la formazione (2) e parziale smantellamento (3) di un’ampia conoi-
de alluvionale del Pleistocene superiore; versante destro della valle del Fiume Metauro, c.ca 1
km a monte di Fossombrone. Le fasi A1, A2. E1 si riferiscono agli eventi descritti in Figura 6.
Ubicazione in Figura 1B. Da: SAVELLI et al. (1984), semplificato.

O. Nesci, D. Savelli & F. Troiani



149

braided river plain or directly on the bedrock (NESCI &
SAVELLI, 1991). From this perspective, alluvial fan depo-
sits and related piedmont aprons – every so often mer-

ging erosional glacis (NESCI et al., 2002) - are spread
throughout the northern Marche foothills both in pied-
mont sectors (SAVELLI & BALLERINI, 1991; NESCI et al.

1993; SAVELLI et al., 1994) and at
the junction of tributary catch-
ments with the main valley
(NESCI & SAVELLI, 1986, 1991).
They are part of the depositional
suites of the principal alluvial-
terraces and have been inter-
preted as climatically-driven
landforms related to the late
Quaternary glacial stages (NESCI
et al ., 1995). Indeed, in the
Umbria-Marche Apennines
some close relationships
between alluvial fan develop-
ment and tectonics can be
stressed in correspondence of
either fault scarps or active
morphostructures only in the
most inner areas (CATTUTO et al.,
2004 and reference therein), dis-
sected by extensional tectonics
(LAVECCHIA, 1988 and references
therein). On the contrary, in the
external sectors of the area the
climate control on fan develop-
ment becomes dominant and
the tectonic constraints can only
be indirectly detected (SAVELLI et
al., 1994; NESCI et al., 2002).
It is worth underlying that the
term “alluvial fan” is used in this
paper for alluvial depositional
bodies which are directly con-
nected with a specific point of
water and sediment input and
limited in the downstream (axial)
direction. Clast lithology highli-
ghts a supply from local catch-
ments, while morphometric cha-
racteristics of pebbles underline
a relatively short travelling
distance (Fig 5B). As for other
places and settings, (e. g.,
KOCHEL, 1990; MUKERJI, 1990),
the typical fan-shape can be
developed or not. Most of the
fans of the study area do not
show the characteristic shape
consisting in a downslope radia-
ting segment of cone, because
of both the occurrence of confi-
ning adjacent fans and physio-
graphic constraints, e.g. narrow
valley troughs. In the same pla-
ce, a progressive confinement
of fans is apparent from the older
fans to the most recent ones,
accounting for an enhancing
rate of stream entrenchment
which, in turn, can be seen as
the result of an increased uplift-
rate (NESCI et al., 2002). The val-

Fig. 4 - Reconstruction of the uppermost middle Pleistocene (A) and late Pleistocene (B) allu-
vial fans at Isola del Piano, on the north-eastern foothills of Monti della Cesana calcareous
anticline ridge. A strong confinement of the most recent fans is obvious when compared to the
coalescing fan-glacis development during the previous cycle. Location in Figure 1B. After
NESCI et al. (1993), modified.

Ricostruzione delle conoidi alluvionali del Pleistocene medio finale (A) e del Pleistocene supe-
riore (B) nei dintorni di Isola del Piano, sulle pendici nord-orientali della dorsale anticlinalica cal-
carea dei Monti della Cesana. Il confronto fra i due diversi eveventi di formazione di conoidi
alluvionali mette in evidenza il forte confinamento che caratterizza il ciclo più recente.
Ubicazione in Figura 1B. Da NESCI et al. (1993), modificato.

Late-Quaternary alluvial fans ...



150

ley narrowing connected with the recent stream-net
entrenchment, can be locally so strong that in areas
where in earlier fan-formation cycles wide piedmont
aprons have formed, in more recent cycles alluvial fans
could not develop (SAVELLI et al., 1994).

As stated above, whatever the fan-shape, degree
of confinement and location, the major northern Marche
fans are cyclical and are part of the alluvial fill suites of
the principal valley terraces. However, this doesn’t
mean that a large number of minor alluvial fans cannot
form anytime and in any suitable place: widespread,
scattered formation of minor fans indeed occurs almost
everywhere. It is worth mentioning the large coastal-
fans (uppermost Pleistocene-lowermost Holocene)
which, with a sea level lower than today, developed
close to the modern river mouths because of the remo-
val of huge alluvial masses during the first dissection
stages of the upper-Pleistocene alluvial plains (DI BUCCI
et al., 2003; NESCI et al., 2008; CALDERONI et al., 2008).
Other examples can be observed, which consist of a
wide range of forms every so often active and frequen-
tly grading to scree cones (cf. Fig 3.3), which and are in
relation with both land use and ongoing deep-seated
slope gravitational deformations: an example of this lat-
ter is the San Lazzaro fan reported by FRANCAVILLA

(1976) (cf. Fig. 2 F-F’).
What follows is a synthetic description of some se-

lected sites, which can be regarded as representative for
the whole northern Marche sector of both piedmont
pediment areas and of tributary junctions with trunk val-
leys. The sites have been chosen in order to highlight
those cases where there are accounts in the same place
of a systematic repetition of alluvial-fan deposits in the
main fill sequence of each principal terrace, and where re-
lationships with the trunk-valley terrace-alluvium can be
easily assessed. The objective is to stress the cyclical re-
currence of wide alluvial fan depositional systems, highli-
ghting the stratigraphic relationships between alluvial-fan
deposits and fluvial fill of the trunk valleys, and to underline
the occurrence of a peculiar sequence of alluvial bodies
which can be retained as the result of late Quaternary cli-
matic-driven sedimentary and geomorphic processes.

4. ALLUVIAL FANS IN THE MARCHE APENNINES:
CASE STUDIES

4.1 Metauro River valley, Fossombrone site (Figs. 2 F-
F’, 3 and 4)

This site extends for a few kilometres just

Fig. 5 - The characteristic patterns of stratigraphic superposition of alluvial-fan deposits above fluvial sediments in a typical fill-terrace
of the northern Marchean area. A. Sketch displaying the stratigraphic relationships between fluvial (f) and fan (af). B-E. Some explicati-
ve outcrops and lithologic and morphometric differentiation between fluvial and alluvial fan deposits. Location of outcrop areas in
Figure 1B.

Le diverse modalità nella sovrapposizione stratigrafica dei depositi di conoide alluvionale sui sedimenti fluviali nella fase aggradazionale
di un tipico ciclo di terrazzamento vallivo principale dell’area marchigiana settentrionale. A. Schema dei rapporti stratigrafici fra i depo-
siti fluviali (f) e quelli di conoide alluvionale (af). B-E. Il contatto in alcuni affioramenti significativi e alcuni elementi di differenziazione fra
i depositi fluviali e quelli di conoide alluvionale. Ubicazione degli affioramenti in Figura 1B.

O. Nesci, D. Savelli & F. Troiani



upstream Fossombrone, where the Metauro River cros-
ses the Monti della Cesana anticline ridge (Fig. 1) cut-
ting a rather narrow valley-segment in the calcareous
Meso-Cenozoic units of the Umbria-Marche
Succession. Three different stages of alluvial fan forma-
tion can be observed, related to as many major terrace-
fill events, i.e. T3, T2 and T1 (cf. Fig. 6), and each cha-
racterized by a thickness ranging from 5 to 15 metres.
The late Pleistocene fans (T3 fill stage) are preserved at
the junction of the widest part of the tributaries with the
trunk valley, although a severe dismantling occurred
because of both a pronounced lateral erosion perfor-
med by the Metauro river during the downcutting stage
(cf. Fig. 3.3), and a strong gravitational instability of a
wide sector of the left valley-side. The wide and well-
formed Holocenic fan already described by FRANCAVILLA
(1976) can also be noticed on the left valley side, where
several scree cones and an important landslide accu-
mulation also occur, due to huge, slow deep-seated
gravitational movements (PERGOLINI et al., 2001).
Nonetheless, it is worth underlining that close to the
junction of the tributary valley from which this recent
fan takes origin, residual patches of an older fan are
found hanging on the flanks of the tributary valley in a
position clearly correlable with the late Pleistocene fan
deposits occurring in nearby sectors (e.g. the fan
shown in Fig. 3). The fans of the uppermost Middle
Pleistocene (i.e. T2 fill stage, cf. Fig. 6) are preserved in
some small patches on the right side of the Metauro
valley, resting above fluvial gravels of the T2 fluvial fill
and/or directly on bedrock. It is worth emphasizing that,

in a general way, fan deposits rest directly on bedrock
both upstream along the tributary valley which fed the
fan and/or in several internal sectors of the trunk valley,
where fill terraces are often substituted by strath terra-
ces. A patch of Middle Pleistocene alluvial-fan deposits
can be observed in a higher position on the right valley-
side (Fig. 2), resting above the fluvial gravels of the T1
(T1B according with the attribution of NESCI et al., 1990).
They have a scant morphological emphasis because of
strong remoulding, which is at least in part related to
the fine-grained nature of the deposit, supplied chiefly
by marly and marly-calcareous units.

4.2 Metauro River valley, Sant’Angelo in Vado site (Fig.
2 V-V’)

The site is set a few kilometres downstream of
Sant’Angelo in Vado, on the right side of the valley seg-
ment that crosses the north-western termination of the
Catria-Nerone anticline ridge (Fig. 1). Along the valley
reach enclosing the site, terraces are preserved at diffe-
rent heights above the modern valley floor which
account for four principal fill-stages, the oldest and
highest of which has been referred to the T1A (Monte
Proverso terrace, 210 m above the thalweg, according
to NESCI et al., 1990). The composite profile in Fig. 2
crosses the valley in an area where the oldest terrace
(T1A) is not preserved, but some previously unreported
T1B terraces occur (T1 in Fig 2), one of which consisting
of both fluvial and alluvial-fan deposits. These deposits,
more than 15 meters thick, lie on the top of fluvial
deposits at the most external fan-zone, whereas,

151

Fig. 6 - The principal stages in the development of the main valley terraces in the northern Marche Apennines: the position of principal
episodes of downcutting and aggradation, including alluvial fan formation stages, are shown. Plotting against the oxygen isotope
curve of LISIECKI & RAYMO (2005), after WEGMANN & PAZZAGLIA (2009), simplified.

Le principali fasi erosionali e aggradazionali, con i maggiori episodi di formazione di conoidi alluvionali, nell’evoluzione dei principali ter-
razzi vallivi dell’Appennino Marchigiano settentrionale. Riferimento alla curva isotopica dell’ossigeno di LISIECKI & RAYMO (2005), sulla
base del lavoro DI WEGMANN & PAZZAGLIA (2009), semplificato.

Late-Quaternary alluvial fans ...



toward the fan-apex zone, they generally overlay the
bedrock. The alluvial fan deposits show a well-preser-
ved top-surface, characterised by a very gentle dipping
towards the trunk-valley axis, and covered by a thick
decalcified, reddish-yellowish relict soil. More downslo-
pe, any patch of alluvial fan deposits related to previous
T2 terrace can be observed, likely because of erosional
removal, although remains of such deposits occur both
up- and down-valley. In this respect, it is worth
underlying that previous T1B related fan deposits could
be preserved because of their topographic location,
resting on a local wide divide. Conversely, deposits of
alluvial fans connected with the T3 fill stage are well
preserved in several wide terraces at the junction of tri-
butaries with the trunk valley.

4.3 Foglia River valley, Colbordolo site (Fig. 2 C-C’)
This site is located on the right flank of the Foglia

River valley, roughly between the villages of Colbordolo
and Montefabbri, where the trunk stream crosses an
anticline ridge made up mainly of Cenozoic marly-cal-
careous terrains (Fig. 1). Here, three main fill terraces
are preserved, namely T1B (T1 in Fig 2), T2, T3. Not so
different from the already described examples, the fill of
each principal terrace consists of both fluvial and allu-
vial-fan sediments, with preserved thicknesses of fan
deposits sometimes exceeding 20 metres.

4.4 Monti della Cesana piedmont area, Isola del Piano
site (Fig. 4) 

The site is located on the north-eastern foothills of
the Monti della Cesana anticline ridge consisting of
mainly calcareous Meso-Cenozoic terrains (Fig. 1). It is
an example of alluvial fans finding – at least during
some specific cycles of late Quaternary fan construc-
tion - their accomodation space not in an aggraded val-
ley floor, but in a piedmont area wide enough to allow
an erosional-depositional glacis to develop. Similar
examples are diffused in several areas of the central
and northern Marche region, both on authoctonous ter-
rains (SAVELLI & BALLERINI, 1991; NESCI et al., 1993, 1995,
2002) and in allochthonous ones (GUERRA & NESCI, 1999;
NESCI et al., 2002). The piedmont area around the villa-
ge of Isola del Piano shows wide late Pleistocene fill
terraces (Fig. 4B) characterised by mainly gravel allu-
vium, averaging 20-25 metres in thickness, supplied by
small catchments draining the Monti della Cesana ridge
to the north-east, which accounts for a narrow, SW-NE
elongated, confined alluvial fan (NESCI et al., 1993,
2002).

At higher elevations, several patches of terraced
alluvial-fans deposits are found, allowing (NESCI et al.,
2002) to reconstruct the depositional top-surface with
enough accuracy to assess the occurrence of an
ancient system of partially coalescent fans. These have
been correlated to several scattered remains of a wider
erosional surface, hinting at a rather smooth piedmont
area shaped in a wide glacis both by fan accretion and
by areal erosion (Fig 4A). On the basis of morpho-strati-
graphic correlation all along the piedmont area and
towards the Metauro River valley, a reliable attribution
to the uppermost middle Pleistocene (T2) events of ter-
races development can be made (NESCI et al., 2003).
The Isola del Piano piedmont is also an area where the
confinement of alluvial fans in narrow valley troughs

during the late Pleistocene is particularly clear, a fact
that – as mentioned above - has been related with an
increasing downcutting driven, in turn, by an enhancing
rate of uplift.

5. DISCUSSION AND CONCLUSIONS

During late Quaternary, a generalized crustal uplift
gradually diminishing in intensity to the north-east,
affected the northern Marche Apennines promoting the
formation of river terrace staircases which – including
the flights of erosional terraces already described by
FANUCCI et al. (1996) - along the main valley sides, rea-
ches heights of up to 300 meters above the present
valley-floors (DI BUCCI et al., 2003 and references the-
rein). In such a frame of progressive uplift the major late
Quaternary cyclic climatic fluctuations (i.e., glacials-
interglacials) can be retained to have driven temporary
depositional episodes that promoted the formation of
middle Pleistocene-upper Pleistocene fill-terraces,
namely the terrace units referred as T1A, T1B, T2, and T3
(cf. Fig. 6) according to FANUCCI et al. (1996). The flight
of valley terraces exposed along the flanks of the main
fluvial valleys, generally developed through a complex
series of fill and dissection processes, stand for the
most evident expression of the so called “rhythmical
succession of cycles”, already underlined by LIPPARINI
(1936). Such “rhythmical succession of cycles”, howe-
ver, also include other specific morphoevolutive episo-
des (both erosional and depositional); in particular,
among depositional events, the most outstanding and
diffuse features are the alluvial-fan deposits, wide-
spreading over the mountain-front and foothills of the
Umbria-Marche Apennines (NESCI & SAVELLI, 1986,
1990). Namely, alluvial fans are an integral part of the
alluvial valley-fillings, as they usually associate with flu-
vial deposits along the trunk valleys (i.e., fluvial sedi-
ments are systematically topped with alluvial-fan depo-
sits, cf. Fig. 2). On the other hand, at the foothills of the
major anticline ridges which characterize the most
internal areas, the alluvial-fan sediments/landforms are
the only significant alluvial contributors to terrace for-
mation (Fig. 4), often coalescing to form typical pied-
mont aprons (e.g., SAVELLI & BALLERINI, 1991; SAVELLI et
al., 1994; NESCI et al., 2002). In the examined areas, the
major alluvial fillings are currently considered as climate
driven events (COLTORTI et al., 1991; NESCI et al., 1995;
WEGMANN & PAZZAGLIA, 2009). At the same time, the
cyclical formation of large alluvial-fan depositional
systems at the junction of small tributaries with the
trunk-valley and at the foothills of the major anticline
ridges of the northern Marche Apennines, is to be
regarded as climate-controlled (NESCI et al., 1995).

In this context, the geomorphologic analysis of
the alluvial fans that directly connect to the major fill
terraces exposed within the study area has led to some
remarkable considerations, as follows.

- As shown in Figure 2, the formation of wide and
thick alluvial fans is systematic and cyclical and is
directly connected with the major fluvial fill stages along
the trunk valleys. In particular, where both fluvial and
fan depositional events occur, the fan deposits syste-
matically follow the fluvial ones, generally overlaying the
top of the fluvial fill belonging to the same depositional

152 O. Nesci, D. Savelli & F. Troiani



cycle (cf. Fig. 6). The most frequent boundaries
between the two depositional sequences belonging to
the same depositional events are either unconformably
erosional or sharp conformable as shown in Figure 5. In
several cases, however, the boundary results heteropic,
with alternation of typical fluvial coarse sediments and
locally-derived alluvial fan deposits. Where this typo-
logy of boundary occurs the thickness of deposits cha-
racterized by such alternation is rather low, usually less
than 2-3 metres (NESCI & SAVELLI, 1991) in a cumulative
thicknesses (i.e. fluvial + fan) every so often exceeding
40-50 m. Hence, notwithstanding the typology of the
stratigraphic boundary, the fan deposits always lie
above undissected tops of fluvial sediments (Figs. 2, 3).
This pattern highlights the occurrence of specific strati-
graphic relations (i.e., superposition), and a rather clear
chronological succession between the two distinct
depositional sequences. Namely, in a first time the
trunk valley experiences a fluvial filling by aggradational
behaviour of the main stream; afterwards, at the junc-
tion of the tributaries, alluvial fan systems develop.

- The T3 terrace has to be regarded as an unavoi-
dable key element to reconstruct the morphoevolutive
events in the study area. In fact, the T3 terrace is gene-
rally well developed along the northern Marche trunk
valleys, furthermore it is usually spatially continuous
and well constrained by several radiocarbon ages (CAL-
DERONI et al., 1991; NESCI et al., 1995; ELMI et al., 2003;
CALDERONI et al., 2008). These latter characteristics, in
particular, allow us to define a well constrained
morphoevolutive pattern and reasonably correlate the
late Pleistocene depositional/erosional events with the
main late Quaternary climatic fluctuations (Fig. 6). Since
a cyclically recurrent suite of peculiar depositional and
erosional events characterize each major fill terrace, it
is plausible to extrapolate the results obtained for the
late Pleistocene fill terrace to the older terrace levels
(middle Pleistocene and uppermost middle Pleistocene
terraces), as already indirectly demonstrated, for exam-
ple, in the detailed analysis proposed by WEGMAN &
PAZZAGLIA (2009). Namely, the T3 terrace becomes an
interpretative guide for the analysis of the older fill terra-
ces and, moreover, for the analysis of fill-terrace stair-
cases through the whole Umbria-Marche area. In this
frame, the most striking expression of the late
Quaternary cyclical depositional events is the cyclical
formation of alluvial-fan depositional systems.
Therefore, the interpretation of the alluvial fan develop-
ment as climate-driven depositional events - despite
some dating problems, as at the next point - actually
can be reasonably projected to the middle Pleistocene
(T1) and to uppermost middle Pleistocene (T2) terraces.
On the other hand, alluvial fans are not the only feature
fit for this purpose. Indeed, among the others, some
features that appear to support the assertion of an
effective usefulness of some repetitive facies and ero-
sional patterns in both the reconstruction and interpre-
tation of late Quaternary morphogenetic cycles, are, for
example: i) the systematic repetitiveness of the thick-
ness of both fluvial fills and overlying alluvial fan depo-
sits (cf. BULL, 1992); ii) the systematic pattern of the re-
incision that involve the alluvial fills and, at least in part,
the bedrock, promoting the formation of both strath ter-
races (Fig. 2) and ingrown meanders (cf. Fig. 3.3).
Furthermore, in the same perspective the cyclical for-

mation can be also interpreted - along the downstream
sector of the main northern Marche trunk valleys - of
typical coastal fans merging in a coeval coastal plain,
as already suggested by CALDERONI et al. (2008).

- It is necessary to underline that for alluvial fan
deposits in general, and even more so for those of the
alluvial fans of the piedmont sectors of the calcareous
anticline ridges - which hardly reveal peculiar, clarifying
stratigraphic relationships with the alluvial fills of the
trunk valleys - a very scant number of radiometric ages
is available both for the whole Marche Apennines and
for the studied areas. Hence, any chronological attribu-
tion and/or correlation with other deposits rests more
on circumstantial evidence than on analytical data.
Indeed, CALDERONI et al. (1991) stressed how the
Cesano River deposits – but such consideration is
equally reliable for the other northern Marche rivers -
only the lower half of the terrace-fill hold wood frag-
ments suitable for dating, since the upper section was
lacking in any appropriate materials. On account of this,
they performed an indirect computation of the expec-
ted age for the upper part of the alluvial suite, reaching
an estimate that today sounds quite near to the ages
reported by WEGMANN & PAZZAGLIA (2009). Furthermore,
some available radiometric ages of alluvial deposits of
the Marche Apennines which have been retained
“other” than alluvial fans (e.g. uncorrected 14C ages of
23,500±400 of CALDERONI et al., 1992 for the upper
Esino River basin, and 23,500±1200 of MENCUCCI et al.
2003 for the lower Foglia River basin) could instead be
reasonably referred to fan deposits. As a matter of fact,
much work is to be done to achieve – every so often
through expensive analytical procedures - a larger
amount of numeric ages able to detail the chronological
attribution and to provide a further advance in genetic
explanation of these deposits. However, as targeted by
this paper, a detailed field work and the reconstruction
of mutual relationships between different sedimentary
bodies, between them and certain peculiar erosional
events, and between them and specific diagnostic
landforms is essential to depict a morpho-sedimentary
correlative and evolutive frame as that shown in Figure
6, which is capable of eventually being adjusted by
further analytical data and/or in which such data can be
suitably set.

- Based on the above considerations on the scant
availability of numeric chronological constraints for both
the upper part of the trunk-stream fills and alluvial fan
deposits, a major question regards the fans and aprons
of the piedmont areas around the major carbonate anti-
cline ridges. In fact besides lacking in numeric ages,
they hardly display obvious stratigraphic relationships
with trunk-valley fills. Indeed, if their correlation with the
fans occurring at the junction of the tributaries on the
trunk-valleys were effective, a diachronism with respect
to the same trunk-valley fill should result (cf. Figs. 2, 5,
6). Actually, in certain areas where the downstream ter-
mination of some wide piedmont aprons reaches the
trunk-valley, a superposition on valley trough fill-depo-
sits is still well recognisable. As an example, the depo-
sits of the coalescing fans of Acquaviva, at the foothills
of Catria-Nerone anticline ridge (Fig. 1), whose down-
stream termination reaches the trunk-valley (Burano
River). Here the fan deposits overlay the fluvial valley-fill
sediments (SAVELLI & BALLERINI, 1991), thus hinting at a

153Late-Quaternary alluvial fans ...



downstream extension of the piedmont alluvial-system
that expands upon the already formed alluvial-plain of
the trunk valley. It is worth emphasizing that the same
piedmont alluvium of Acquaviva displays a complex
evolution which, starting with alluvium supplied from
the south-east (i.e. from longitudinal streams), conti-
nues with the deposition of huge amounts of alluvium
sourced from the south-west (i.e. from the Catria-
Nerone carbonate anticline ridge) and thus distributed
in an overall transverse direction (SAVELLI & BALLERINI,
1991). This seems to account specifically for a transi-
tion from along-valley aggradation, possibly correlated
with the ongoing trunk valley filling-up, to a huge depo-
sition by overburden tributary streams, which joined
trunk streams no longer capable and competent to
transport the huge sedimentary load supplied from the
minor catchments. It is exactly the case of the alluvial
fans observed at the junction of tributary streams on
the trunk valleys (Figs. 2, 3, 5 and 6). Similar beha-
viours, indeed, indicating significant variations in func-
tional interaction between the trunk-stream and its tri-
butaries, also from a conceptual standpoint could
strengthen the idea of a chronologic shifting of alluvial
sedimentation loci towards the piedmont zones, thus
accounting for the stages of generalized development
of coalescing fans observed on the foothills of the car-
bonate ridges.

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156

Ms. ricevuto il 18 giugno 2009
Testo definitivo ricevuto il 5 ottobre 2009

Ms. received: June 18, 2009
Final text received: October 5, 2009

O. Nesci, D. Savelli & F. Troiani