GeolCarp_Vol62_No1_17

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA

, FEBRUARY 2011, 62, 1, 17—26 doi: 10.2478/v10096-011-0002-2

Introduction

In recent decades, the interest of geomorphologists in long-
term  and  regional  landscape  reconstructions  has  opened  up
new  perspectives  for  the  study  of  the  relationship  between
tectonics  and  exogenous  dynamics  over  geological  times
(Summerfield  1991;  Cinque  et  al.  1993;  Westaway  1993;
Ollier & Pain 1996; Amato & Cinque 1999; Bartolini 1999;
England & Molnar 1999; Amato 2000; Burbank & Anderson
2001;  Schiattarella  et  al.  2003;  Robustelli  et  al.  2009).  The
geomorphic  markers  traditionally  used  for  this  purpose  are
marine terraces and paleosurfaces. According to Widdowson
(1997),  the  term  paleosurface  indicates  “a  topographic  sur-
face  of  depositional  or  erosional  origin,  recognizable  as  a
part  of  the  geological  record,  or  otherwise  of  demonstrable
antiquity and of regional significance, which displays the ef-
fects of surface alteration resulting from a prolonged period
of weathering, erosion or non-deposition”. Although hard to
date  with  respect  to  marine  terraces,  paleosurfaces  are  fre-
quently  used  in  tectonic  studies  due  to  their  large  surface

New morphostratigraphic and chronological constraints for

the Quaternary paleosurfaces of the Molise Apennine

(southern Italy)

PIETRO P.C. AUCELLI

, VINCENZO AMATO

, MASSIMO CESARANO

, GERARDO PAPPONE

CARMEN M. ROSSKOPF

, ELDA RUSSO ERMOLLI

3,4

and FABIO SCARCIGLIA

Dipartimento DiSAm, Universit degli Studi di Napoli Parthenope, Centro Direzionale, 80100 Napoli, Italy;

pietro.aucelli@uniparthenope.it; gerardo.pappone@uniparthenope.it

Dipartimento S.T.A.T., Universit degli Studi del Molise, Contrada Fonte Lappone, 86090 Pesche (IS), Italy;

vincenzo.amato@unimol.it; cesarano@unimol.it; rosskopf@unimol.it

Dipartimento di Arboricoltura, Botanica e Patologia vegetale, Universit di Napoli, Federico II, via Universit 100, 80055 Portici, Italy;

ermolli@unina.it

Département de Préhistoire du Muséum National d’Histoire Naturelle, USM103–MNHN, UMR7194, CNRS, Institut de Paléontologie

Humaine, rue René Panhard 1, 75013 Paris, France

Dipartimento di Scienze della Terra, Universit della Calabria, Via P. Bucci, Cubo 15B, 87036 Arcavacata di Rende (CS), Italy;

scarciglia@unical.it

(Manuscript received May 27, 2010; accepted in revised form November 5, 2010)

Abstract: The Molise Apennines feature numerous relicts of paleosurfaces, mostly of erosional origin, which represent
the remnants of gently-rolling ancient landscapes now hanging at different altitudes above the local base-levels of
erosion. Their genesis can be related to prolonged periods of relative tectonic stability alternating with periods of uplift,
or to the interplay between steady tectonic uplift and climatic fluctuations. Four orders of paleosurfaces were recog-
nized: I ( > 1,100 m a.s.l.), II (900—1,000 m a.s.l.), III (750—850 m a.s.l.), IV (600—720 m a.s.l.). The most ancient orders
(I and II) are cut into the bedrock and are located at the top of the Matese and Montagnola di Frosolone massifs. The
youngest paleosurfaces (III—IV), partially cut into Quaternary deposits, are found along the valley flanks of the main
river systems and within the Boiano, Carpino, Isernia and Sessano intramontane basins. The present study deals with
the dating of the Sessano Basin Paleosurface (SBP) which is related to the IV order and is cut into the basin infill. The

Ar/

Ar age of a tephra layer (437 ± 1.9 ka), intercalated at the top of the succession, supported by archaeo-strati-

graphic, palynological and paleopedological data, allowed the SBP surface to be constrained to 350—300 ka. The SBP
chronological position represents an important morphostratigraphic marker: it is the first ante quem and post quem date
that allows the chronological position of the other orders of paleosurfaces to be better constrained.

Key words: Quaternary, Italy, Molise Apennine, paleosurfaces, paleopedology, morphostratigraphy.

area,  which  allows  geomorphic  correlations  over  long  dis-
tances and facilitates the recognition of differential tectonic
movements.  Successful  application  of  stratigraphic  tech-
niques  may  be  achieved  when  it  is  possible  to  date  the  de-
posits immediately underlying or covering the paleosurface.
Provided that they have a well-documented age, paleosurfac-
es may play a fundamental role in reconstructing the tempo-
ral sequences of geomorphological and tectonic events.

In the central and southern Apennines, several morpho-

stratigraphic  studies  have  managed  to  obtain  age  estimates
for  many  paleosurfaces,  cut  both  in  the  chain  and  foredeep
domains (e.g. Brancaccio et al. 1988; Bosi et al. 1996; Ama-
to  &  Cinque  1999;  Basili  et  al.  1999;  Coltorti  &  Pieruccini
2000; Bartolini et al. 2003, D’Alessandro et al. 2003; Boenzi
et  al.  2004;  Gioia  &  Schiattarella  2006;  Schiattarella  et  al.
2006). These paleosurfaces represent the remnants of gently-
rolling ancient landscapes, generated by fluvio-denudational
processes,  which  are  preserved  at  different  altitudes  above
the local base levels of erosion. In general, their genesis took
place during more or less prolonged periods of relative tec-

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GEOLOGICA CARPATHICA, 2011, 62, 1, 17—26

tonic  stability  that  alternated,  during  Neogene  times,  with
periods of uplift (Cinque et al. 1993). The most ancient pa-
leosurfaces,  often  in  summit  positions  (e.g.  Paleosuperficie
Auct.;  Cinque  et  al.  1993;  Bosi  2002),  are  polygenic  forms
which  unconformably  cut  the  deformed  units  of  the  Apen-
nine orogene and are found at high altitudes, generally above
1,000 m a.s.l. Other paleosurfaces are much younger and are
located along valley flanks or in tectonic depressions at vari-
ous altitudes above the present local base levels of erosion.

The sector of the Apennine chain located in the Molise re-

gion (hereinafter Molise Apennine, Fig. 1) is also character-
ized  by  numerous  relicts  of  paleosurfaces  both  within  the
mountain belt and along its margins, as well as within the in-
tramontane basins. The areas that preserve various orders of
paleosurfaces  are  typically  characterized  by  a  distinct  step-
like landscape. Even if this pattern clearly testifies to a com-
plex tectonic evolution, it is currently constrained by few –
and  uncertain  –  chronological  data  (i.a.  Brancaccio  et  al.
1979; Brancaccio et al. 2000; Coltorti et al. 2005; Di Bucci
et  al.  2005).  In  particular,  recent  studies  by  Amato  et  al.
(2010) and Russo Ermolli et al. (2010) have added some new
chronological  constraints  for  the  Middle  Pleistocene  paleo-
surface of the Sessano intramontane basin located along the
northwestern margin of the Montagnola di Frosolone massif
(Fig. 1).

In this paper, we summarize the results of a geomorphologi-

cal study in the Molise Apennine focusing on the major relicts
of  paleosurfaces  with  a  regional  significance  in  order  to  at-
tribute a relative age to them and thus to reconstruct the main
steps of the landscape evolution in the area. In this regard, a
fundamental  contribution  was  provided  by  the  multidisci-
plinary  approach  used  to  date  one  such  paleosurface,  the
Sessano  Basin  (hereinafter  SBP).  Our  study  combined  strati-
graphic and geomorphic methods, and was supported by pollen

and paleopedological analyses, tephrostratigraphy,

Ar/

dating and geoarchaeological contributions.

Geological setting

The Molise Apennine (Fig. 1A) rise in the junction zone

between the southern and the central-northern arcs that form
the  Apennine  chain  (Patacca  et  al.  1992).  In  this  zone,  the
pre-Quaternary bedrock comprises a Meso-Cenozoic carbon-
ate platform and slope-to-basin deposits, cropping out on the
Matese and on the Montagnola di Frosolone massifs, as well
as Meso-Cenozoic basin deposits of the Sannio Unit and by
Miocene  foredeep  and  piggy-back  basin  deposits  (Fig. 1B).
The  structural  setting  of  the  area  is  the  result  of  a  complex
deformation due to compressive tectonics from the Miocene
to  Pliocene  (Corrado  et  al.  1997a;  Scrocca  &  Tozzi  1999;
Antonucci et al. 2002). Subsequently, transtensional and ex-
tensional tectonics acted, from the Early Pleistocene, mainly
along NW-SE and NE-SW oriented alignments, respectively.
During  extensional  tectonics,  from  the  Middle  Pleistocene
onwards (Corrado et al. 2000; Di Bucci et al. 2002; Amato et
al.  2010),  several  intramontane  basins  of  variable  size
(Carpino-Le  Piane,  Isernia,  S.  Massimo,  Boiano  and  Ses-
sano) developed within the Molise Apennine chain and were
gradually  filled  up  by  huge  Quaternary  successions  com-
posed  of  fluvial  to  lacustrine  and  volcaniclastic  deposits
(Brancaccio et al. 1979; Corrado et al. 1997a; Corrado et al.
2000; Di Bucci et al. 2002; Coltorti et al. 2005; Di Bucci et
al. 2005; Russo Ermolli et al. 2010).

The Sessano Basin, in particular, characterized by a huge

and  partially  outcropping  fluvio-lacustrine  succession,  was
only  affected  by  extensive  tectonics  during  the  Middle
Pleistocene  which  caused  the  tilting  of  the  infilling  and  ex-

Fig. 1. A – Structural map of Italy and location of the study area; B – Geological scheme of the Matese-Frosolone area. Legend: 1 – Al-
luvial and volcaniclastic deposits (Quaternary); 2 – Foredeep and piggy-back siliciclastic deposits (Miocene); 3 – Clays, marls and lime-
stones of the Sannio Unit (Upper Cretaceous-Miocene); 4 – Limestones, dolomites and marls of the inner carbonate platform (a) and
carbonate slope deposits (b) (Triassic—Miocene); 5 – Main thrusts, dashed where inferred; 6 – Main extensional faults, dashed where
inferred.

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tinction of the paleomarsh. After this tectonic event the top
of the Middle Pleistocene succession mainly underwent ero-
sion by fluvio-denudational processes, which led to the for-
mation of a wide erosional surface (the SBP), now hanging
about 25 m above the present base level (Amato et al. 2010;
Russo Ermolli et al. 2010).

The paleosurfaces of the Molise Apennine

The paleosurfaces were studied through field surveys, aerial

photos and topographic maps. As shown by Bosi et al. (1996),
the main problem in analysing paleosurfaces is the correlation
and ordering of the remnants in altitudinal ranges. The criteria
adopted in the present study are the following: 1) the geomet-
ric  relationship  and  continuity  of  the  paleosurface  remnants;
2) the possible correlation on the basis of altitude, bearing in
mind the possible gradients of the original surfaces, their posi-
tion within the local sedimentary sequences and their relation-
ship  with  local  successions  that  are  well  correlated;  3)  their
relationship  with  geological  formations  of  known  chronos-
tratigraphic  position  and,  finally,  4)  similarity  criteria  based
on the state of preservation and origin of the single remnants.

Generally, the distinguished paleosurface remnants are gen-

tly sloping surfaces ( < 5°) covering an area ranging between
some hundreds and some thousands of m

. Most of them have

an erosional origin, either on carbonate or terrigenous rocks,

while  those  originated  by  deposition,  genetically  related  to
Quaternary continental deposits, are only present at lower alti-
tudes  within  the  main  fluvial  valleys  and  the  major  tectonic
depressions. Even if the pre-existing litho-structural rock fea-
tures  have  sometimes  influenced  the  extent  and  regularity  of
the  surfaces,  more  frequently  a  clear  unconformity  between
the bedding and the surfaces confirms their origin by erosion.
The paleosurfaces are limited by scarps linked to direct tecton-
ic  control  or  generated  by  base  level  variations  and  conse-
quent  downcutting  due  to  uplift  and/or  climatic  influence.
Alternating phases of dominant planation and downward ero-
sion then generated a typical “terraced” landscape which char-
acterizes wide areas of the Molise Apennine.

The following four orders of paleosurfaces were identified

in the Matese and Montagnola di Frosolone massifs, in the up-
per portion of the Biferno and Trigno valleys (Fig. 2) and in
the sector including the Sessano and Carpino Basins and their
surroundings (Fig. 3).

I order ( > 1,100 m a.s.l.)

The I order of paleosurfaces are widespread within the

Matese and Montagnola di Frosolone massifs (Figs. 2, 4a and
4b), where they reach up to 2,000 m and 1,400 m a.s.l., re-
spectively. These paleosurfaces, the most ancient of the
Molise Apennine, are generally cut into carbonate rocks. Their
origin is related to fluvio-denudational processes which inter-

Fig. 2. Distribution of the four orders of recognized paleosurfaces and location of the intramontane and fluvial basins of the Molise Apennine.

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acted at times with karst and glacial erosion. This interaction
results in polygenic landforms often preserving more than one
erosional  cycle  and  partially  affected  by  tectonic  fragmenta-
tion. The difference in altitude among the I order surfaces can
be related to differential vertical tectonic movements that af-
fected the Matese and Montagnola di Frosolone massifs dur-
ing  the  Apennine  formation  process.  Some  geomorphic
indicators, such as hanging paleovalleys, provide evidence of
the  hydrographic  network  that  characterized  the  chain  while
the paleosurface was being shaped.

II order (900—1,000 m a.s.l.)

The II order of paleosurfaces are well represented along the

carbonate border slopes of the Matese and Montagnola di

Frosolone  massifs  and  within  the
upper  mature  sectors  of  the
Volturno  and  Trigno  valley  sys-
tems  (Figs. 2,  4a  and  4b).  Some
of  them  are  derived  from  tectoni-
cally lowered I order paleosurfac-
es,  later  affected  by  further
modelling and erosion. Within the
hilly  to  low-mountainous  sectors,
located  on  the  terrigenous  depos-
its of the Sannio and Molise Basin
units,  strong  downfaulting  and
erosion  led  to  their  fragmentation
and  progressive  reduction  into
small  crests  and  isolated  heights.
As part of the main water divides,
they  mainly  occur  in  the  upper
sector  of  the  Biferno  valley
system.

III order (750—850 m a.s.l.)

The III order of paleosurfaces

are also well represented along the
northern  slope  of  the  Matese  and
the  border  slopes  of  the  Montag-
nola  di  Frosolone  mountains
(Fig. 4a  and  4b),  as  well  as  along
the  borders  of  the  Sessano  and
Carpino  Basins  (Figs. 3  and  4d).
They are also well preserved with-
in the upper portions of the Bifer-
no and Trigno Valleys both in the
summit  position  and  along  the
valley flanks. Generally, these pa-
leosurfaces  are  cut  into  the  bed-
rock, apart from the San Massimo
paleosurface. The latter, located at
ca.  800 m  a.s.l.  along  the  north-
western  slope  of  the  Matese
Mountains  and  hanging  about
300 m  above  the  Boiano  Plain,
unconformably  cut  fluvio-palus-
trine deposits (Fig. 4c).

Ar /

Fig. 3. Detail of the four orders of paleosurfaces in the Sessano-Carpino intramontane basin area.

ages after Brancaccio et al. (1979) and Di Bucci et al. (2005)
allowed two interbedded volcaniclastic levels to be con-
strained to 1.0—1.1 Ma and 0.6 Ma.

IV order (600—720 m a.s.l.)

The IV order of paleosurfaces are widespread in the Molise

Apennine.  Numerous  remnants  are  located  along  the  south-
ern slopes of the Boiano Plain (Fig. 4a) and in the upper sec-
tors of the Biferno and Trigno Valleys where they are often
part  of  the  water  divide  (Fig. 2).  Within  the  Sessano  Basin
and along its borders (Figs. 3 and 4d), this order is also well
represented, at 700—720 m a.s.l., by remnants with a certain
areal  continuity,  cutting  both  the  pre-Quaternary  bedrock
and  the  Middle  Pleistocene  fluvio-palustrine  filling.  One  of

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Fig. 4. Views of the paleosurfaces of the Molise Apennine: a – remnants along the north-eastern slopes of the Matese Mountains; b – rem-
nants along the south-eastern slopes of the Montagnola di Frosolone massif; c – top of the fluvio-palustrine succession cropping out near the
village of San Massimo at 800 m a.s.l. and referred to the III order of paleosurface; d – remnants around and within the Sessano Basin.

Fig. 5. Chronostratigraphic scheme of the uppermost portion of the Sessano infilling. The soil profiles (P1 and P2) and related micro-mor-
phological characters are showed in Fig. 6. On the basis of the dated tephra layer (437.9±1.9 ka BP, outcropping at the base of the soil pro-
files, and on the basis of the Levallois artifacts (200 ka BP), discovered at the top of the soil profiles, the P1 and P2 paleosols can be
referred to Oxigen Isotopic Stage 12 (OIS 12) and 11 (OIS 11, respectively).

these surfaces, the SBP, located in the central-northern part
of  the  basin  at  700 m  a.s.l.,  provided  very  important  chro-
nostratigraphic  constraints  through  the  analysis  of  tephra
layers, pollen and paleosols interbedded in the upper part of
the Middle Pleistocene fluvio-palustrine succession (Fig. 5).
Along the borders of the adjacent Carpino Basin, this order
is represented by remnants at about 600 m a.s.l. and lying at
about 100 m above the plain. They cut both the pre-Quater-
nary bedrock and the Quaternary deposits. Measurements of
the local gradients characterizing the paleosurfaces of the Ses-
sano  and  Carpino  areas  support  their  correlation  and  allow
them to be referred to a generic Middle Pleistocene Tyrrhen-

ian dipping paleolandscape (Di Bucci et al. 2002 and Amato
et al. 2010).

Other paleosurfaces (below 500 m a.s.l.)

Other relicts of erosional and depositional surfaces are

present  in  the  study  area  below  500 m  a.s.l.  They  were  as-
cribed  to  the  Middle  Pleistocene  by  Brancaccio  et  al.  (2000)
and  Coltorti  et  al.  (2005).  Such  surfaces  generally  represent
stripped fluvial terraces hanging a few tens of meters over the
valley floors; they are mainly located in the upper part of the
Volturno River catchment area. It is difficult to give these sur-

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faces  a  regional  significance  (according  to  the  criteria  of
Widdowson 1993) due to their limited presence in the upper-
middle  Volturno  Basin  which  prevents  any  correlation  with
the surfaces located along the valley flanks of the Trigno and
Biferno Rivers. The Volturno surfaces were generated by the
interaction between the local tectonic and the Late Quaterna-
ry  climatic  fluctuations  (Brancaccio  et  al.  2000;  Coltorti  et
al.  2005).  They  probably  developed  after  the  formation  of
the IV order of paleosurfaces or could represent the remnants
of tectonically lowered IV order paleosurfaces.

Morphochronological constraints from the Sessano-

Carpino area

As previously described, all the recognized orders of pa-

leosurfaces are present within the Sessano-Carpino area, al-
ternatively cut into carbonate and/or siliciclastic rocks, or in
Quaternary deposits (Fig. 3). Thanks to this circumstance
and the fact that the Sessano Basin features a well-dated
Middle Pleistocene filling, the Sessano-Carpino area is a key
site to understand the tectonic and related geological evolu-
tion of the Molise Apennine.

occurred before the planation phase which shaped the IV order
SBP, the latter being cut into the tilted succession.

The chronological position of this uppermost portion of

the Sessano infill is clearly established by the

Ar/

Ar age

of  the  tephra  layer  that  outcrops  at  its  base  (437 ± 1.9 ka;
Russo Ermolli et al. 2010). Chemical analysis by Russo Er-
molli et al. (2010) allowed its correlation with the High Po-
tassium  Series  (HKS)  explosive  volcanic  activity  of  the
Roccamonfina  volcano,  namely  with  the  Rio  Rava  Plinian
eruption, dated by Rouchon et al. (2008) to 439 ± 9 ka. An-
other  important  chronological  constraint  is  represented  by
the discovery, at the top of the SBP, of various Paleolithic
artefacts  ascribed  to  the  Levallois  Culture  (A.  Minelli,
Molise  University,  personal  communication).  Their  age  of
ca.  200—150 ka  indicates  that  the  extinction  of  the  paleo-
marsh, the tilting of the sedimentary succession and the gen-
esis of the SBP occurred after 437 ka and before 200 ka.

Paleopedological and pollen data

The pedostratigraphic succession overlying the dated tephra

layer was subdivided into two soil profiles, P1 and P2, repre-

Fig. 6. Pedostratigraphic succession of the uppermost portion of the Sessano infill subdivided into
soil profiles P1 (a) and P2 (b) and micrographs in plane polarized light of Fe-Mn segregations
from horizon 2Btss (c) and clay coatings from horizon Bt (d). For location see Fig. 5.

Chronostratigraphic data

In the Sessano Basin, a Middle

Pleistocene  pedosedimentary  fill
provides  important  evidence  on
paleoenvironmental,  climatic  and
tectonic  events  that  governed  its
evolution  and  extinction.  These
features were investigated in detail
using  an  integrated  archaeo-teph-
ro-stratigraphic,  palynological  and
pedological  approach.  The  upper-
most part of the fill, ca. 11 m thick,
crops out along the scarps of sever-
al artificial trenches. It is made up
of parallel sand, clay and soil lay-
ers,  often  separated  by  abrupt
boundaries,  indicating  discontinu-
ous fluvial and marshy sedimenta-
tion alternating with soil formation
and erosional phases. This succes-
sion  is  characterized  by  the  pres-
ence  of  abundant  volcaniclastic
material  which  is  generally  re-
worked,  except  for  a  35 cm-thick
primary  tephra  layer  which  crops
out at its base (Fig. 5) and mainly
consists  of  white  pumices  (O

/ max

= 1 cm).  The  outcropping  portion
of  the  fill  is  characterized  by  a
N6°E strike and a strata dip of 17
degrees  toward  east  (Fig. 5).  It  is
locally  affected  by  high-angle
faults with vertical throws not ex-
ceeding 0.3 m. This tectonic phase

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senting  its  upper  and  lower  portion,  respectively  (Figs. 5,  6a
and b). The reworked volcaniclastic ash layers represent CBt
horizons,  white  to  greyish  in  colour,  alternating  with  well-
structured, brown to yellow and yellowish-brown buried soils
(B horizons). In particular, above the basal soil horizons (Bg)
showing redox concentrations (pseudogley, i.e. temporary hy-
dromorphic features; IUSS Working Group WRB, 2006; Soil
Survey  Staff,  2010)  there  is  a  series  of  argillic  (Bt)  horizons
with illuvial clay coatings, also showing other distinct genetic
features:  various  horizons  (Bss)  at  different  stratigraphic
depths  exhibit  vertic  properties  (shiny  faces  and  slickensides
due to shrink-swell dynamics), whereas intermediate horizons
are characterized by calcium carbonate concretions (Bk). Pre-
liminary  SEM-EDS  microprobe  analyses  were  performed  on
vesicular  glass  fragments  (subangular  micropumices,  30  to
400 µm in size) identified in two ash layers (horizons CBt and
4CBt) in the upper and lower portion of the succession. Glass
shards show a trachytic composition (with a dispersal of data
towards  the  phonolite  field),  which  is  not  so  dissimilar  from
those  analysed  and  dated  in  the  underlying  core  succession
(Russo  Ermolli  et  al.  2010).  These  results  suggest  the  same
provenance and a cyclical reworking of the same tephra prod-
ucts within the basin infill, as supported by sedimentary evi-
dence,  where  the  dominant  trachytic  over  phonolitic
composition  may  indicate  a  decrease  in  alkali  as  a  conse-
quence of chemical weathering and leaching. Besides, the lat-
er  HKS  products  of  other  Middle  Pleistocene  explosive
eruptions from the Roccamonfina volcano (cf. Rouchon et al.
2008) should also be taken into account.

With the aid of micromorphological analysis of thin sec-

tions  obtained  from  undisturbed  soil  samples,  coupled  with
the field features, the main environmental conditions through-
out  the  pedostratigraphic  succession  may  be  assessed.  What
emerges is, on the whole, a rather humid environment. How-
ever, some changes can be identified from bottom to top, with
an overall trend from moderately humid to slightly drier con-
ditions followed, in turn, by more humid conditions. In partic-
ular,  in  soil  profile  P2  a  poorly-drained  (marshy)  humid
environment is indicated at the base by its redoximorphic fea-
tures, with some seasonal contrast and further dryness. This is
also indicated in the upper horizons by vertic features, moder-
ate clay translocation, the latter being typical of Quaternary in-
terglacials  or  mild  interstadials  within  glacial  periods  in
mid-latitude  areas  (e.g.  Catt  1989;  Kemp  et  al.  2004;  Scar-
ciglia  et  al.  2006),  and  secondary  CaCO

precipitation. The

modest extent of clay illuviation, the occurrence of carbonate
concretion and the complete lack of rubification better support
drier (and possibly colder) conditions of glacial phases rather
than interglacials. A progressive return to more humid condi-
tions is clearly shown in soil profile P1 and mainly in its upper
horizons, where a weak change to a redder hue (10YR) of the
matrix is observed, coupled with many reddish-black iron-
manganese segregations (Fig. 6c). The very abundant laminat-
ed clay coatings (different generations), observed in thin
sections (Fig. 6d), suggest a clear transition towards warm and
humid (interglacial-like) climatic conditions.

Pollen analysis of the trench section (Fig. 5) was not suc-

cessful, since all the collected samples were barren or very
poor in pollen (with a very advanced state of oxidation to-

wards  the  top  of  the  succession),  only  allowing  a  qualitative
approach to be adopted. Some considerations can nevertheless
be attempted on the basis of the pollen data from the underly-
ing  cored  succession  where  two  climatic  cycles  were  recog-
nized and ascribed to Oxygen Isotope Stages (OIS) 15 to 12
(Russo Ermolli et al. 2010). The warm and humid period rec-
ognized in the upper part of the core (OIS 13) shows a transi-
tion towards a subsequent glacial period which is announced
by the decline in deciduous forest elements. This deteriorat-
ing climatic trend seems confirmed by the qualitative analy-
sis of the trench samples where a dominance of herbaceous
elements  is  documented.  Therefore,  at  least  the  base  of  the
trench  section  of  Fig. 5  should  record  the  glacial  stage 12
which  represents,  together  with  stage 16,  the  most  severe
cold  period  of  the  Middle  and  Late  Pleistocene  (Lisiecki  &
Raymo  2005).  This  glacial  period  has  never  been  fully  rec-
ognized  in  Italian  pollen  records.  A  few  levels  at  Vallo  di
Diano  and  Acerno,  in  the  southern  Apennines,  were  doubt-
fully ascribed to OIS 12 on the basis of climatostratigraphy
(Russo  Ermolli  &  Bertini  2009)  and  tephrostratigraphy
(Di Donato et al. 2009), respectively.

In synthesis, the main environmental changes depicted in

the two soil profiles of the trench section highlight a transi-
tion from moderately humid (lower soil profile P2) to slightly
drier  and  colder  conditions  (upper  soil  profile  P2  to  lower
P1), followed by warmer and more humid conditions (upper
soil profile P1). Similar evidence is indicated by pollen data,
which  are  the  image  of  a  glacial  period  at  the  base  of  the
trench  section,  following  a  deterioration  trend  recorded  to-
wards  the  top  of  the  underlying  core  stratigraphy.  Soil  fea-
tures show that this glacial period is followed by a possible
further  climatic  amelioration.  According  to  the  above  chro-
nostratigraphic  position,  the  soil  and  pollen  analyses  of  the
trench section suggest that this portion of the Sessano infill
probably  recorded  a  later  interglacial  imprint  (possibly
OIS 13) or an interstadial phase during OIS 12, followed by
full  glacial  conditions  in  the  intermediate  portion  (OIS 12),
up  to  real  interglacial  conditions  towards  the  top,  presum-
ably related to the subsequent OIS 11.

Discussion

Given the above morphostratigraphic and chronological

data the main morphosedimentary changes recorded in the up-
permost portion of the Sessano fill may reasonably be attribut-
ed  to  the  Middle  Pleistocene,  in  particular  to  OIS 12  and
OIS 11 (Fig. 5). After this period, a phase of extensional tec-
tonics, acting on N-S oriented faults, caused the E-SE tilting
of  the  Sessano  succession  and  the  extinction  of  the  paleo-
marsh  (Amato  et  al.  2010).  The  truncation  of  the  previously
tilted succession and the formation of the Tyrrhenian-ward dip-
ping IV order paleolandscape (SBP) started immediately after.

We believe that this phase of paleosurface formation, which

is clearly constrained to the period between 437.9 ± 1.9 ka and
200 ka (see section: Morphochronological constraints from
the Sessano-Carpino area – Chronostratigraphic data), can be
even better defined in chronological terms on the basis of the
following considerations:

AUCELLI, AMATO, CESARANO, PAPPONE, ROSSKOPF, RUSSO ERMOLLI and SCARCIGLIA

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2011, 62, 1, 17—26

The tephra layer dated to 438 ka is overlain by 11 m of

fluvio-marshy  and  volcaniclastic  deposits  alternating  with
several  paleosols.  Both  the  discontinuous  sedimentation  and
the development of soils correspond to an additional time span
that may include one or more climatic cycles (from the end of
OIS 12 to OIS 11). This is also supported by the main changes
in  soil  features  (and  related  environmental  conditions)  along
the pedostratigraphic succession, coupled with the dominance
of  herbaceous  pollen  taxa  and  their  severe  state  of  oxidation
towards the top.

After this additional time interval, tectonic deformation

(tilting) occurred, which corresponds to another time interval
to be added before the genesis of the SBP surfaces within the
Sessano Basin. Also this time interval may have covered one
or more climatic cycles, from the end of OIS 11 onwards. We
cannot exclude the occurrence of further exposure of the pa-
leosurface to pedogenetic processes after the extinction of the
above  pedosedimentary  cycle  and  its  tectonic  deformation
during more recent times. In fact, the abundant clay coatings
of surface soil horizons (in profile P1) may have been super-
imposed throughout various interglacials younger than OIS 11
(OISs 9 to 7 or 5). Another major erosion surface is indicated
by  the  truncation  of  the  upper  paleosol  in  question,  as  high-
lighted  by  the  lack  of  organic-mineral  or  albic  horizons  and
the exposure of typical deep (argillic) ones at the topographic
surface (Kemp et al. 2004; Robustelli et al. 2009).

On the basis of these considerations, the beginning of the

planation phase leading to SBP formation can be chronologi-
cally constrained to a time interval that spans from ca. 350 to
ca. 300 ka, in agreement with the age of the Carpino Basin in-
fill (Di Bucci et al. 2002).

Conclusions

The chronostratigraphic data obtained for the SBP surface

represent a new morphochronological marker for the Molise
Apennine: they are the first ante quem and post quem dates,

and enable the evolution of the Molise Apennines to be better
defined. In synthesis, the IV order paleosurfaces can be as-
cribed to the Middle Pleistocene, and most likely to the time
interval spanning from 350 to 300 ka.

Using this chronological marker, supported by data from the

literature, we were able to fix some further temporal thresholds
to  the  various  orders  of  paleosurfaces  identified  in  the  Molise
Apennines (Fig. 7). The III order paleosurfaces are part of a pa-
leolandscape  already  hanging  above  the  fluvio-lacustrine  Ses-
sano Basin before its extinction and then before 438 ka. Within
the Boiano Basin, the paleosurface that cuts the San Massimo
lacustrine deposits, located at ca. 800 m a.s.l., post-dates the top
of the deposits that are dated to ca. 600 ka. It is therefore repre-
sentative  of  a  paleolandscape  that  evolved  during  the  Middle
Pleistocene between 600 and 350 ka.

No chronological data are available for the I and II orders

of  paleosurfaces.  However,  morphostratigraphic  regional
correlations, the presence of Upper Miocene flysch deposits
cropping out on top of the Montagnola  di Frosolone massif
and the total lack of Pliocene deposits in the whole area may
suggest that the genesis of these orders most likely occurred
between  the  Early  Pliocene  and  the  Early  Pleistocene,  in
agreement with what is known for other sectors of the Apen-
nine  chain  (e.g.  Paleosuperficie  Auct.,  Brancaccio  et  al.
1986;  Ascione  &  Cinque  1999,  2003).  On  the  other  hand,
given the age of the IV order of paleosurfaces, the other pa-
leosurface remnants of local significance, located at altitudes
below  500 m  a.s.l.,  must  have  been  generated  after  300 ka
from the interplay between local tectonic and Late Quaterna-
ry climatic fluctuations.

In conclusion, the results of our study show that a multi-

disciplinary approach integrating several tools and analytical
techniques can be successfully applied to obtain important
and reliable data for reconstructing landscape evolution in a
young orogenic chain.

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