Geomorphology 115 (2010) 67–77
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Geomorphology
j o u r n a l h o m e p a g e : w w w. e l s ev i e r. c o m / l o c a t e / g e o m o r p h
Reconstructing the Roman topography and environmental features of the Sarno River
Plain (Italy) before the AD 79 eruption of Somma–Vesuvius
Sebastian Vogel a,⁎, Michael Märker b,c
a
b
c
German Archaeological Institute, Germany, Podbielskiallee 69-71, D-14195 Berlin, Germany
Heidelberg Academy of Sciences and Humanities, University of Tübingen, Rümelinstraße 19-23, D-72070 Tübingen, Germany
Department of Soil Science and Plant Nutrition, University of Florence, Italy
a r t i c l e
i n f o
Article history:
Received 10 June 2009
Received in revised form 9 September 2009
Accepted 18 September 2009
Available online 1 October 2009
Keywords:
Sarno River plain
Somma–Vesuvius
Paleo-topography
Paleo-environment
Modeling
Landscape reconstruction
a b s t r a c t
A methodology was developed to reconstruct the Roman topography and environmental features of the
Sarno River plain, Italy, before the AD 79 eruption of the Somma–Vesuvius volcanic complex. We collected,
localized and digitized more than 1800 core drilling data to gain a representative network of stratigraphical
information covering the entire plain. Besides other stratigraphical data including the characteristics of the
pre-AD 79 stratum, the depth to the pre-AD 79 surface was identified from the available drilling
documentations. Instead of a simple interpolation method, we used a machine based learning approach
based on classification and regression trees to reconstruct the pre-AD 79 topography. We hypothesize that
the present-day topography reflects the ancient topography and related surface processes, because volcanic
deposits from the AD 79 eruption coated the ancient landscape. Thus, ancient physiographic elements of the
Sarno River plain are still recognizable in the present-day topography. Therefore, a high-resolution, presentday digital elevation model (DEM) was generated. A detailed terrain analysis yielded 15 different primary
and secondary topographic indices. Subsequently, a classification and regression model was applied to
predict the depth of the pre-AD 79 surface combining present-day topographic indices with other
physiographic data. This model was calibrated with the measured depth of the pre-AD 79 surface. The
resulting pre-AD 79 DEM was compared with the classified characteristic of the pre-AD 79 stratum,
identified from the drilling documentations. This allowed the reconstruction of pre-AD 79 environmental
features of the Sarno River plain such as the ancient coastline, the paleo-course of the Sarno River and its
floodplain.
To the knowledge of the authors, it is the first time that the pre-AD 79 topography of the Sarno River plain
was systematically reconstructed using a detailed database and sophisticated data mining technologies.
© 2009 Elsevier B.V. All rights reserved.
1. Introduction
The Plinian eruption of the Somma–Vesuvius volcanic complex in
AD 79, which completely buried the Roman settlements of Herculaneum, Oplontis, Stabiae and Pompeii belongs to the most well-known
eruptions in history. During this eruption the pumice lapilli fallout
was dispersed by stratospheric winds predominantly in southeastern
directions up to a distance of more than 70 km from the vent
(Sigurdsson and Carey, 2002). Thus, almost the entire Sarno River
plain was covered by approximately 3.6 km3 of dense rock equivalent
of volcanic deposits (Sigurdsson et al., 1985) showing a specific and
therefore easily identifiable stratigraphy. Since these deposits are
distinctive and laterally extensive, they can be considered as an ideal
chronostratigraphic marker. According to the phase of the eruption
and the chemical composition and density of the magma, the Plinian
⁎ Corresponding author. Tel.: +49 30 187 711 358; fax: +49 30 187 711 168.
E-mail address: sv@dainst.de (S. Vogel).
0169-555X/$ – see front matter © 2009 Elsevier B.V. All rights reserved.
doi:10.1016/j.geomorph.2009.09.031
volcanic deposits of AD 79 consist of white phonolitic pumice and grey
tephritic–phonolitic pumice fallout deposits, interrupted as well
as overlain by six ash layers of pyroclastic surge and flow deposits
(Lirer et al., 1973; Sigurdsson et al., 1985; Carey and Sigurdsson, 1987;
Civetta et al., 1991; Cioni et al., 1992; Pescatore et al., 1999, 2001;
Sigurdsson and Carey, 2002; Luongo et al., 2003; Pfeiffer et al., 2005).
Fig. 1 illustrates the approximate dispersion of the volcanic material
during the eruption AD 79 as modeled by Pfeiffer et al. (2005)
presuming a northwestern wind profile.
The AD 79 eruption covered a wide area of the Sarno River plain
nearly isochronously (within 19 h time) with volcanic deposits of
some meters. This not only caused a caesura in the existence of an
entire landscape, but also contributed to the excellent preservation of
the paleo-surface and the ancient paleo-environmental conditions
before the eruption of AD 79 (Foss et al., 2002). Consequently, almost
2000 years later, this paleo-surface still remains in situ and is
accessible for stratigraphical investigations. In the following the
term pre-AD 79 refers to the conditions before the AD 79 eruption of
Somma–Vesuvius.
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S. Vogel, M. Märker / Geomorphology 115 (2010) 67–77
Fig. 1. Isopachs of the thickness [cm] of the white (A) and grey (B) pumice fallout, deposited during the eruption of Somma–Vesuvius AD 79. Modeled by Pfeiffer et al. (2005)
(RUN V1).
Preliminary geoarchaeological studies in the Sarno River plain
were carried out in the 19th century (Ruggiero, 1879). However, it is
only since the 1980s that more standardized methodologies of
geoarchaeological investigation have developed. Since then there
have been several attempts to reconstruct the paleo-landscape before
AD 79, among them Cinque and Russo (1986), Livadie et al. (1990),
Furnari (1994), Pescatore et al. (1999), Di Maio and Pagano (2003)
and Stefani and Di Maio (2003). These studies mostly dealt with the
delineation of the coastline before AD 79 and the paleo-course of the
Sarno River and its estuary mouth using data from stratigraphical
drilling and archaeological excavations.
As Pescatore et al. (1999) state about previous coastline reconstructions, the results are sometimes rather different (Fig. 2). That is
why the position of the paleo-coastline and the course of the paleoSarno cannot yet be clearly defined from today's state of research.
Barra et al. (1989) and Livadie et al. (1990) used about 50
stratigraphical drillings between Torre Annunziata and the Sarno
River and archaeological data from Roman and pre-Roman times to
reconstruct the pre-AD 79 topography. According to them the ancient
coastline was situated approximately 1 km inland, parallel to the
modern coast with lagoons that were protected from the sea. There
they also assume the location of the ancient marine harbour of
Pompeii. Moreover, they predicted the ancient sea level to be
approximately 4 m below the modern one. In the hinterland of the
ancient coastline they discovered fossil littoral dune deposits of preRoman times (Messigno, 5600–4500 years BP and Bottaro/Pioppaino,
3600–2500 years BP; Cinque, 1991). Furthermore they related
predominantly fluvio-palustrine deposits to the paleo-course of the
Sarno River whose estuary they assumed southeast of the present-day
mouth between Masseria and Resinaro (Barra et al., 1989; Livadie
et al., 1990).
Furnari (1994) carried out 51 stratigraphical drillings and used
some data from archaeological excavations to reconstruct the pre-AD
79 topography. After identifying the pre-AD 79 stratum underneath
the volcanic deposits of AD 79 in 39 of 51 drillings, he characterized it
using micropaleontologic and granulometric analyses and categorized
it according to its origin into four classes: (i) palustrine, (ii) alluvial,
(iii) littoral and (iv) Roman paleosol. According to the location of the
S. Vogel, M. Märker / Geomorphology 115 (2010) 67–77
69
Fig. 2. Past reconstructions of the pre-AD 79 coastline of the Sarno River plain, before (A) and after (B) 1990 (Iacono, 1913; Malandrino, 1988).
drillings he could delineate the approximate position of the paleocoastline, the paleo-Sarno and terrestrial areas of the mainland.
Pescatore et al. (1999, 2001) utilized data from 66 drillings and
known archaeological sites for studying the pre-AD 79 environment
around Pompeii. The stratigraphical data derived from own drillings,
past construction projects, from Ruggiero (1879) and Furnari (1994).
They state that the ancient shoreline may have run more or less
parallel to the modern coast approximately 1 km southwest of the
ancient city of Pompeii and 1 km landwards of the present-day coast.
The mouth of the paleo-Sarno River they presume to be located south
of the modern estuary (Pescatore et al., 1999, 2001).
Di Maio and Pagano (2003) used 15 drillings, as well as five
archaeological sections and data from archaeological excavations to
illustrate a 2.5 km long section of the pre-AD 79 coastline near the
ancient town of Stabia (Fig. 3) north of the Lattari Mountains.
According to them the coastline before AD 79 followed the terrace of
San Marco at a distance of 100 to 200 m, whereas it is possible that, at
this location, the Lattari Mountains represented an active cliff. The
interpretation of the drilling data showed strong variation in the
thickness of the AD 79 eruptive material, especially between the
slopes and the adjacent Sarno River plain. Hence, they argue that
shortly after their deposition, the volcanic sediments must have been
mobilized by heavy rainfall and slope water, moved downslope as a
mudflow and were re-deposited as an alluvial fan delta within the
plain. Thereby parts of the ancient coastline propagated to the NW.
Stefani and Di Maio (2003) used a total of 78 drillings including
new ones and those of Furnari (1994) as well as an extensive dataset
of past archaeological excavations. They state that the eruption AD
79 coated the ancient topography with volcanic deposits up to a
thickness of 3 to 6 m. Consequently the present-day topography more
or less reflects the ancient topography. Despite the volcanic deposits,
main physiographic elements of the Sarno River plain such as the
volcanic hill of Pompeii, the prehistoric dune ridge of Bottaro/
Pioppaino and the terrace of San Marco are still recognizable. Thus,
the present-day topography provides valuable clues in reconstructing
the ancient topography.
As these past studies mostly dealt with separate aspects of the
ancient landscape pre-AD 79, there exists as yet no geoarchaeological
study covering and investigating the paleo-geomorphology and
paleo-environmental conditions of the entire Sarno River plain.
Consequently this research project focusses on the reconstruction of
the paleo-topography of the Sarno River plain before the eruption of
Somma–Vesuvius in AD 79. Therefore we use a methodology that
combines stratigraphical information from former and self conducted
core drillings, present-day topographical data, and classification and
regression methods. With this approach we expect to gain more
detailed information concerning paleo-environmental features such
as the position of the ancient coastline and the course of the paleoriver network before AD 79.
2. Study area
The Sarno River plain situated south of the Somma–Vesuvius
volcanic complex is a cultural landscape characterized by continuous
anthropogenic activity since the Middle Bronze Age. It stretches across
an area of 210 km2 and is drained by the Sarno River and its
tributaries. In the west it opens to the Tyrrhenian Sea, whereas in the
south and in the east, the plain is flanked by the Mesozoic calcareous
rocks of the Lattari and Sarno Mountains that are part of the Southern
Apennine chain (Fig. 3). The Sarno River plain belongs to the great
graben structure of the Campanian Plain which was formed during
Plio-Pleistocene extensional tectonic phases at the end of the
Apennine orogenesis and is filled with marine, alluvial and volcanic
deposits lying on a carbonate platform (Cinque et al., 1987; De Vita
and Piscopo, 2002; Cella et al., 2007).
During the last 25,000 years of Somma–Vesuvius' eruptive history,
several Plinian eruptions have occurred, each one marking the
beginning of a new eruptive cycle after a period of quiescence ranging
from 1400 to 4000 years, such as Mercato/Ottaviano (7070–6770 BC),
Avellino (1890–1630 BC) and Pompeii (AD 79) (Delibrias et al., 1979;
Santacroce, 1987; Rolandi et al., 1993a,b; Andronico et al., 1995;
Civetta et al., 1998; Sigurdsson, 2002; Cella et al., 2007). Among them
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S. Vogel, M. Märker / Geomorphology 115 (2010) 67–77
Fig. 3. Present-day digital elevation model (DEM) and fluvial network of the Sarno River plain with the location of more than 1800 stratigraphical core drillings. Letters indicate sites
of interest. The small scale map of Italy shows the Campanian plain, the Sarno River plain and the Apennine mountain ridge.
the eruption of AD 79 is the most well-known thanks to the detailed
written records of Pliny the Younger.
3. Materials and methods
Since today the Sarno River plain is one of the most densely
populated and urbanized areas in Italy, there are many constraints in
comprehensively applying methods of stratigraphical research over
the entire plain. Consequently it is very important to use a rather noninvasive or minimally-invasive scientific approach. Stratigraphical
core drillings have become a well-established and standardized
method of geoarchaeological prospection in this region since it can
be carried out with comparatively minimal technical and bureaucratic
effort and costs.
To reconstruct the pre-AD 79 geomorphology and paleo-environmental features of the Sarno River plain, the documentation of more
than 1800 drillings from construction works, as well as from past
archaeological and geological studies, were collected to gain a
representative network of stratigraphical information for the entire
Sarno River plain. The drillings were localized and digitized using
geographic information systems (GIS) (Fig. 3). Furthermore, 20 new
core drillings were conducted south and northwest of Pompeii at
Moreggine and Boscoreale (Fig. 3). The drillings were carried out
mechanically to a maximum depth of 10 to 18 m to extract a core of
approximately 15 cm in diameter. By means of the drilling cores the
stratigraphy was determined, the volcanic deposits of AD 79 and the
pre-AD 79 surface underneath were identified, and the pre-AD 79
stratum was characterized.
For this project the most relevant data taken from the drilling
documentation were:
(i)
(ii)
(iii)
(iv)
x–y-coordinates of each drilling point,
elevation of the present-day surface,
thickness of the volcanic deposits related to AD 79 eruption,
depth to the pre-AD 79 surface which is the difference between
the present-day surface and pre-AD 79 surface, and
(v) characteristics of the pre-AD 79 stratum underneath the
volcanic deposits of the AD 79 eruption.
The characteristics of the pre-AD 79 stratum allow the reconstruction of the paleo-environmental conditions. The pre-AD 79
stratum was characterized on the basis of lithofacies distinguishing
five different classes:
(i)
(ii)
(iii)
(iv)
(v)
terrestrial deposits,
fluvial deposits,
palustrine deposits,
littoral deposits, and
marine deposits.
S. Vogel, M. Märker / Geomorphology 115 (2010) 67–77
In case the pre-AD 79 stratum could not be clearly related to one of
these five classes, mixed classes were proposed to comprise intermediate forms of deposits.
Instead of using simple interpolation methods as in former studies,
we reconstruct the pre-AD 79 topography with a sophisticated
geostatistical methodology based on a high-resolution present-day
digital elevation model (DEM). This methodology considers the
statement by Stefani and Di Maio (2003) that the AD 79 eruption
caused a coating of the ancient topography of the Sarno River plain
which left ancient physiographic elements still recognizable in the
present-day topography. Consequently the present-day topography
provides valuable hints for reconstructing the ancient conditions. The
following hypotheses can be outlined:
(i) geomorphic transport processes are related to topographic
terrain characteristics (slope, curvature, etc.),
(ii) the pre-AD 79 topography controlled volcanic deposition,
erosion and transport processes,
(iii) For pre-AD 79 and today, similar relief-forming processes have
been active, and
(iv) tectonic activities and resulting landforms before AD 79 are
taken into account in this modeling approach. Recent tectonic
activities are considered via pre-AD 79 stratigraphic information (e.g. elevation of the ancient coastline).
Since the recent topography will be utilized to deduce the pre-AD
79 topography, a hydrologically correct present-day DEM of the Sarno
River plain was generated using the interpolation method ‘Topo to
Raster’ by Hutchinson (1988, 1989) implemented in ArcGIS 9.2. The
DEM is based on digitized topographic points and contour lines in
vector format of the SIT 1:5000 (Sistema Informativo Territoriale)
(Provincia di Napoli, by courtesy of S.I.A.V., Soprintendenza Archeologica di Pompei). The resulting present-day DEM was postprocessed
to eliminate all evident man-made structures such as dams, motorways, quarries and embankments of the Sarno River which was
regulated in the 1850s (Stefani and Di Maio, 2003). After the sink
drainage route detection and sink removal of the present-day DEM, 15
different primary and secondary topographic indices were delineated
using the terrain analysis module of SAGA GIS (Table 1).
Based on the hypotheses stated above, a classification and
regression tree approach was used to reconstruct the pre-AD 79
Table 1
Predictor variables used for the modeling process in TreeNet (Salford Systems).
Predictor variables
Method/reference
Elevation
Altitude above
channel network
Aspect
Catchment area
Channel network
Channel network
base level
Convergence index
Curvature
Curvature
classification
Plan curvature
Profile curvature
LS-factor
Slope
Stream power
Watershed
subbasins
Wetness index
Geology
Topo to Raster (ArcGIS 9.2)/SIT 1:5000
SAGA terrain analysis module (Olaya and Conrad, 2008)
SAGA terrain analysis module (Zevenbergen and Thorne, 1987)
SAGA terrain analysis module (Olaya and Conrad, 2008)
SAGA terrain analysis module (Olaya and Conrad, 2008)
SAGA terrain analysis module (Olaya and Conrad, 2008)
SAGA terrain analysis module (Köthe and Lehmeier, 1993)
SAGA terrain analysis module (Zevenbergen and Thorne, 1987)
SAGA terrain analysis module (Dikau, 1988)
SAGA terrain analysis module (Zevenbergen and Thorne, 1987)
SAGA terrain analysis module (Zevenbergen and Thorne, 1987)
SAGA terrain analysis module (Olaya and Conrad, 2008)
SAGA terrain analysis module (Zevenbergen and Thorne, 1987)
SAGA terrain analysis module (Olaya and Conrad, 2008)
SAGA terrain analysis module (Olaya and Conrad, 2008)
SAGA terrain analysis module (Olaya and Conrad, 2008)
Digitized geological map 1:10,000 (Autorità di Bacino
del Sarno, 2003)
Land use
CORINE land cover 2000 (Autorità di Bacino del Sarno)
Mean annual ground Interpolated (kriging) water well data (Autorità di
Bacino del Sarno)
water table
71
topography. Classification and Regression Trees (CARTs) is an
algorithm used for exploratory data analysis and predictive modeling
to discover features and understand structural patterns in large
databases by describing the correlation between predictor variables
and a response variable (Breiman et al., 1984; Myles et al., 2004). This
algorithm can handle nominally scaled (categorical) data as well as
continuously scaled (metric) data by applying either classification or
regression trees. CARTs are based on binary recursive partitioning, i.e.
a decision tree is generated by partition of a dataset into two subsets
(binary) where each of the subsets is the basis for a further partition
(recursive). This process is carried out until a partition of a subset is no
longer reasonable, i.e. the elements of a subset are homogenous with
respect to the response variable or if the number of elements of a
subset has become too small. Eventually CARTs generate a model
taking into account the combination of predictor variables with the
highest correlation to explain the response variable (Dannegger,
1997; Schillinger, 2002).
The software that was applied in the present study using the CARTs
algorithm is TreeNet by Salford Systems. We utilized 16 present-day
topographic indices and other physiographic data as predictor
variables (Table 1) and the depth to the pre-AD 79 surface as
response variable to predict the pre-AD 79 topography. TreeNet is
based on Friedman's stochastic gradient boosting (Friedman, 1999).
Gradient boosting constructs additive regression models by sequentially fitting a simple parameterized function to current ‘pseudo’
residuals by least squares at each iteration. The pseudo residuals are
the gradient of the loss function being minimized, with respect to the
model values at each training data point, evaluated at the current step
(Friedman, 1999). Practically, the method derives several hundreds to
thousands of small trees each typically containing six nodes. Each tree
is devoted to contributing a small portion of the overall model
whereas the final model prediction is constructed by adding up each
of the individual tree contributions. This methodology has a variety of
advantages:
(i) it is not sensitive to data errors in the input variables,
(ii) it is resistant to overtraining, and
(iii) it is very fast even with large sets of trees.
For the modeling process we used a TreeNet regression model
with the Huber-M loss function. The maximum number of trees to use
is 3000. Internal model validation is performed by selecting a sample
of cases at random from the model data. Here we selected a fraction of
0.2 of the entire dataset (N = 1811) to train the regression tree at each
iteration.
The model is subsequently used to regionalize the depth to the
pre-AD 79 surface for the entire Sarno River plain. To get the absolute
elevation above sea level of the pre-AD 79 surface, the predicted depth
is thereafter subtracted from the present-day DEM. For additional
external model validation we compare the resulting pre-AD 79 DEM
with the stratigraphical point type information taken from the drilling
data, which is not included in the model. To specify the paleogeomorphological and paleo-environmental characteristics of the
study area and its dynamics, we perform a terrain analysis with SAGA
GIS on the resulting pre-AD 79 DEM. The approximate location of the
ancient coastline, the paleo-Sarno and its flood plain were already
predefined by the littoral and the fluvial/palustrine deposits of the
Roman stratum, respectively. We expect a more precise approximation of the ancient coastline and the paleo-Sarno from the adaptation
of the existing drilling data to the modeled pre-AD 79 topography by
deducing contour lines and depth contours from the pre-AD 79 DEM.
4. Results and discussion
Table 2 shows the predictor variables used for the generation of
the model arranged according to their particular importance to
predict the pre-AD 79 surface. For the final model not all of the
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S. Vogel, M. Märker / Geomorphology 115 (2010) 67–77
Table 2
Ranking of importance of predictor variables used for the model generation.
Variable
Importance [%]
Elevation
Watershed subbasins
Aspect
Channel base level
Stream power
Depth groundwater table
Slope
Altitude above channel network
Elevation groundwater table
Curvature classification
Wetness index
Curvature
LS-factor
Catchment area
Convergence index
Profile curvature
Plan curvature
Channel network
100.0
98.1
78.3
66.9
66.5
58.4
57.3
56.0
55.8
49.7
48.4
47.5
46.3
45.0
42.5
41.2
40.7
22.2
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available predictor variables were entered into TreeNet. The categorical variables geology and land use turned out to be of rather minor
suitability for the modeling process since preliminary results showed
that their areal distribution had a strong artificial impact on the
regionalized pre-AD 79 surface. Fig. 4A illustrates the model
performance with an attained minimum mean absolute error of the
training dataset of 0.92 m and of the test dataset of 1.64 m. The
smallest test mean absolute deviation is based on 2115 grown trees.
The overall performance of the regression model on the given dataset
is reported in Fig. 4B. The gain chart illustrates the percentage of
population (x-axis) in relation to the percentage of the target variable
(y-axis). The higher the percentage of the target variable with
respective low population percentages, the better the model. In this
case the model performance shows a fairly good correlation.
Fig. 5 illustrates the modeled depth to the pre-AD 79 surface of the
Sarno River plain which shows a distinct spatial distribution of the
volcanic deposits since the AD 79 eruption. The modeled depth to the
pre-AD 79 surface ranges from >0 to 15 m whereas the average depth
is 5.7 m. In this study the Sarno River plain was only reconstructed
northwards up to the modern town of S. Giuseppe Vesuviano (Fig. 3).
From that location the drilling cores no longer contained AD 79
volcanic material which means that the pre-AD 79 surface could not
be clearly identified anymore.
The importance of the predictor variables illustrates that the
spatial distribution of volcanic deposits since and including the AD 79
eruption is most notably controlled by the absolute elevation being
the result of all relief-forming geomorphic processes. Of secondary
importance are the aspect and hydrological variables such as
watershed subbasins, channel base level and stream power. The
aspect represents the direction in which the volcanic material was
spread over the territory during the eruption. Originating from the
Somma–Vesuvius volcanic complex, the pumice lapilli fallout was
dispersed concentrically towards the southeast which fits well with
the dispersion of the volcanic material during the AD 79 eruption as
modeled by Sigurdsson and Carey (2002) and Pfeiffer et al. (2005)
(Fig. 1). Consequently, on the southeastern flanks of Somma–
Vesuvius, near the source of the eruption the volcanic deposits are
thicker.
The hydrological parameters represent the redistribution of the
volcanic deposits after the eruption by erosion, transport and
accumulation processes. Thus, greater thicknesses of the volcanic
deposits along the Tyrrhenian coast most likely indicate re-deposited
material that was mobilized by the Sarno River and its tributaries and
transported towards the Tyrrhenian Sea. This corresponds with
thinner deposits in the central part of the Sarno River plain.
It is striking that along the southeastern foot slopes of Somma–
Vesuvius the volcanic deposits are much thicker than in the river
plain. Three main reasons may be responsible for the spatial
distribution of the deposits:
(i) As mentioned above the deposition of volcanic material is
generally thicker close to the vent of Somma–Vesuvius being
the source of the eruption.
(ii) Apart from the white and grey pumice lapilli fallout the slopes
of Somma–Vesuvius were also subject to pyroclastic surge and
flow deposits of AD 79. They are concentrated at the foot slopes
of Somma–Vesuvius since they did not reach far into the plain
(Di Vito et al., 1998; Di Maio and Pagano, 2003).
(iii) On the slopes of Somma–Vesuvius the volcanic deposits of AD
79 are overlain by pyroclastic material and lava flows from
more recent eruptions that were less powerful to reach more
distant areas. Thickest deposits most notably could be related
to the eruptions of 1631, 1742–1761 and 1944 (see geological
map 1:10,000, Autorità di Bacino del Sarno, 2003).
An accumulation of volcanic deposits at the foot of the Lattari and
Sarno Mountains may result from slope deposits being mobilized by
mountain torrents or lahars after intense rainfall events. Debris flows
or hyperconcentrated flows are known phenomena in the mountain
areas adjacent to the Sarno River plain. The mountains are mantled by
irregular layers of pyroclastic materials such as tephra and pumice
fallout deposits which are intercalated with buried soils. Especially
due to the presence of allophane, volcanic soils generally have a high
water retention and low bulk density, which means that the weight of
retained water can exceed the dry weight of the soil (Terribile et al.,
2007). Due to this irregular cover of different strata which is
characterized by a strong vertical variability of physical–mechanical
properties, intense rainfall events can trigger slope instabilities, mass
movements and thick submontane accumulations. These processes
are still active today as the catastrophic landslide events of Sarno in
1998 have shown (Rao, 1995; Terribile et al., 2000; De Vita and
Piscopo, 2002; Crosta and Dal Negro, 2003; Fiorillo and Wilson, 2004;
Zanchetta et al., 2004; Terribile et al., 2007).
Slightly thicker deposits in the southwestern area of Pompeii
running NW–SE fit well with the ancient dune ridge of Bottaro–
Fig. 4. Mean absolute error [m] of the depth to the pre-AD 79 surface versus number of trees of the training and test dataset (A) and gain chart of the training dataset (B) (TreeNet).
The minimum mean absolute error of the training dataset of 0.92 m and of the test dataset of 1.64 m was attained at 2115 grown trees.
S. Vogel, M. Märker / Geomorphology 115 (2010) 67–77
73
Fig. 5. Modeled depth to the pre-AD 79 surface of the Sarno River plain.
Pioppaino. This may result from the fact that the dune ridge itself
shows a slightly higher elevation than the surrounding terrain. Thus,
the effects of fluvial and coastal erosion processes are limited.
Moreover, the surface of the dune ridge is relatively flat, for instance
in comparison to the Pompeiian hill, with low slope gradients and
related erosion processes. Rather thin deposits on the Pompeiian hill
on the other hand indicate that after deposition AD 79 volcanic
material was eroded from the ridge and accumulated in the adjacent
plain due to higher slope gradients.
Fig. 6A and B compares the present-day topography with the
predicted pre-AD 79 topography. Even though main physiographic
elements appear on both DEMs, several differences can be identified.
Most evident is that the pre-AD 79 surface is approximately 5.7 m
deeper than the modern surface. Consequently the entire coastal area
is lying below the recent sea level.
Comparing the present-day Sarno River (Fig. 6A) with the modeled
fluvial network before AD 79 (Fig. 6B) it is striking that the main
elements seem to have preserved over time and are still visible in the
present-day river network, i.e. the streams from the slopes of Somma–
Vesuvius, the stream from Nocera and the intersections near the Sarno
Mountains. However, in comparison to the canalized present-day
Sarno River, the paleo-Sarno River, which follows the depth contours
of the pre-AD 79 DEM, shows meander type fluvial patterns.
In the southern section of the Tyrrhenian coast at the base of the
Lattari Mountains a big fan delta can be clearly identified on both the
present-day DEM and the pre-AD 79 DEM (Fig. 6). In the present-day
geomorphological map of Cinque (1991) it is called ‘conoide
Muscariello’. It is orientated towards the main discharge of this part
of the Lattari Mountains, the ‘Fosso di Gragnano’. The fan delta on the
modeled pre-AD 79 DEM indicates that this landform already existed
in Roman times. This corresponds with Cinque (1991) and Cinque
et al. (1987, 1997) who identified fan deltas of a first and second
generation which they dated to the Middle and Late Pleistocene,
respectively. Di Maio and Pagano (2003) also detected strong
variations in the thickness of the AD 79 eruptive material between
the slopes and the adjacent Sarno River plain which they related to the
formation of fan deltas due to heavy rainfall after the AD 79 eruption.
However, in their reconstruction of the paleo-coastline near the
ancient town of Stabia, they state that the fan delta did not exist at the
moment of the AD 79 eruption. Consequently they delineated the
coastline between 100 and 200 m parallel to the terrace of San Marco
(Fig. 2).
The external validation of the pre-AD 79 DEM was performed
using the stratigraphical information from the core drillings (see
Materials and Methods). Furthermore by comparing the categorized
character of the pre-AD 79 stratum with the pre-AD 79 DEM we
reconstructed some paleo-environmental features before AD 79
(Fig. 7A and B).
The results show that the littoral deposits before AD 79 are
distributed nearly parallel to the present-day coastline at a horizontal
distance of 1000 to 1500 m (Fig. 7A). In the north of the Tyrrhenian
coast, most of the littoral deposits are located between the −3 and
−2 m contour lines, and near the Sarno River and in the south of the
bay, between the − 1 and 0 m contour lines. This matches with
findings of Sigurdsson et al. (1985) and Livadie et al. (1990) who state
that after AD 79 a northwards dipping subsidence of the Roman
littoral deposits to approximately −4 m occurred. Near the mouth of
the Sarno River the same deposits could be found at − 1 m. Pescatore
et al. (2001) state that a more rapid subsidence appears near Somma–
Vesuvius in comparison with more distant areas. This subsidence is
related to the collapse of the graben structure of the Campanian plain
of approximately 2 mm year− 1 during the entire Quaternary. In the
Sarno River plain subsidence is compensated by the constant
accumulation of volcanic deposits due to the activity of Somma–
Vesuvius which finally resulted in a westward propagation of the
coastline (Cinque et al., 1987; Livadie et al., 1990; Cinque, 1991).
Converging contour lines at the foot of Somma–Vesuvius, the
Lattari Mountain and the Pompeiian hill that are orientated towards
74
S. Vogel, M. Märker / Geomorphology 115 (2010) 67–77
Fig. 6. Present-day DEM (A) and modeled pre-AD 79 DEM (B) of the Sarno River plain with 5-m contour lines and fluvial network.
the sea reveal escarpments that may have derived from abrasion
action of the sea related to previous coastlines (Fig. 8). The
protohistorical dune ridges of Messigno and Bottaro/Pioppaino
could be delineated by confronting their location from the geological
map (Autorità di Bacino del Sarno, 2003) with both the modeled preAD 79 topography and the distribution of marine/littoral deposits
from the drilling data that were found inland from the ancient
shoreline (Figs. 7 and 8).
The distribution of fluvial/palustrine deposits taken from the
drilling data correlates well with the modeled paleo-river network.
Especially around the mouth of the paleo-Sarno River and near
Longola–Poggiomarino, these deposits are characterized by the 1 to
2 m isolines of the ‘vertical distance to channel network’ index from
the SAGA terrain analysis module. This area contains 71% of all
fluvial/palustrine deposits found in the drilling data. Consequently,
this area can be identified as the flood area in which the paleo-Sarno
River most likely had its ancient riverbed. Near Pompeii the paleoSarno River bends southwards, approximately 1 km away from its
present-day river bed to flow around the more elevated protohistorical dune ridges of Messigno and Bottaro/Pioppaino. This agrees
S. Vogel, M. Märker / Geomorphology 115 (2010) 67–77
75
Fig. 7. Pre-AD 79 DEM with the drilling data on the pre-AD 79 stratum (A) and inferred reconstruction of pre-AD 79 environmental features (B).
well with the paleo-Sarno River of Stefani and Di Maio (2003) and
the geological map (Autorità di Bacino del Sarno, 2003). Due to the
plain relief, this area will most likely be characterized by meanders,
backwaters and an extensive flood area. The approximate mouth of
the paleo-Sarno can be localized around 1500 m east of its presentday mouth which coincides with a noticeable inland propagation of
the − 3 and − 2 m contour lines. This location corresponds well with
the findings of Barra et al. (1989) and Livadie et al. (1990) stated
above.
Based on deeper littoral deposits in the northern coastal area, the
pre-AD 79 DEM revealed an elevation discontinuity southwest of the
excavation of Pompeii (Figs. 5 and 8). The discontinuity is more than
3 km long and oriented N–S. It includes several elevation levels from 1
to − 5 m a.s.l. and has a vertical offset from east to west of − 0.5 to
76
S. Vogel, M. Märker / Geomorphology 115 (2010) 67–77
Fig. 8. Pre-AD 79 environmental reconstruction of the Tyrrhenian coast of the Sarno River plain.
−1.5 m. Thus, relative to the western part, the eastern part of this
discontinuity is displaced towards the south indicating a horizontal
transversal fault. Neotectonic deformations of the Apennines are
predominantly oriented SW–NE or NW–SE. However, reactivated
faults of an E–W or N–S orientation can sometimes be found (Nicotera
and Civita, 1969a,b; Ortolani and Aprile, 1978; Aprile and Ortolani,
1979; Cinque et al., 1987). This discontinuity seems to be overprinted
by recent deposition as it cannot be identified on the present-day
DEM. This implies that it was formed before AD 79 possibly associated
with the seismic activity preceding the AD 79 eruption, such as the big
earthquakes of AD 62 and AD 64. Marturano (2008) and Marturano et
al. (2009) proposed a ground uplift of Pompeii of around 2 m prior to
the AD 79 eruption which fits well with the modeled discontinuity.
The crustal deformations are presumably caused by the inflation of
magma bodies underneath the Somma–Vesuvius volcanic complex.
drillings. The pre-AD 79 DEM will be utilized to determine potential
locations of Pompeii's marine or fluvial harbour, whose exact location
is still debated (e.g. Stefani and Di Maio, 2003). Moreover, the
combination of the pre-AD 79 DEM with archaeological findings
enhances the paleo-environmental reconstruction of the Sarno River
plain.
In the next project phase the pre-AD 79 DEM will be used to
determine the paleo-topographic setting of the known ‘villae rusticae’
of the Sarno River plain (Casale and Bianco, 1979; Kockel, 1985, 1986).
In addition to paleo-pedological analyses, we will use the pre-AD 79
topography to reconstruct soil and land use characteristics. These data
will help us to simulate the ancient cultural landscape of the Sarno
River plain. In summary, the modeled pre-AD 79 DEM has a great
potential for future geoarchaeological investigations.
Acknowledgments
5. Conclusions
The pre-AD 79 topography and paleo-environmental features of
the entire Sarno River plain were reconstructed for the first time using
sophisticated geostatistical methods. The estimated pre-AD 79
topography and the derived paleo-river network fit well with the
stratigraphical data from the drilling documentation. In addition to
the internal validation, the semantic validation also yielded good
results. Nevertheless this reconstruction is only a model of the pre-AD
79 conditions based on the hypothesis stated above. Consequently the
modeled paleo-river network is only approximate and cannot be
considered as the exact paleo-course of the Sarno River before AD 79,
since it is derived from the regionalized pre-AD 79 DEM. However, the
deduced contour lines enclosing the fluvial/palustrine and littoral
deposits from the drillings data more reliably indicate the approximate location of the paleo-Sarno and the paleo-coastline, respectively.
In future studies the pre-AD 79 DEM will be used to identify zones
of particular interest for carrying out additional stratigraphical
This study is part of the geoarchaeological research project entitled
‘Reconstruction of the ancient cultural landscape of the Sarno River
plain’ undertaken by the German Archaeological Institute in cooperation with the Heidelberg Academy of Sciences and Humanities. It was
initialized by Florian Seiler and partly funded by the German
Archaeological Institute, Berlin Head Office (Cluster 3) and the
Deutsche Forschungsgemeinschaft (German Research Foundation).
We would like to thank our local project partners and all their
collaborators for their cooperation, particularly the Autorità di Bacino
del Sarno, the Soprintendenza Speciale per i Beni Archaeologici di
Napoli e Pompei, the Soprintendenza per i Beni Archaeologici di
Salerno e Avellino. We also thank Giovanni Di Maio, Giovanni
Patricelli and Gaetana Saccone for various supports and Andrew
Kandel for reviewing the English manuscript. Finally, we would like to
thank Carmen Rosskopf, Jean-Paul Bravard and Takashi Oguchi for
reviewing and substantially improving the paper with constructive
comments and suggestions.
S. Vogel, M. Märker / Geomorphology 115 (2010) 67–77
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