AMQ82 Mancini et al ProofCopy f


   

 Available online http://amq.aiqua.it 
ISSN (print): 2279-7327, ISSN (online): 2279-7335 
 
 

Alpine and Mediterranean Quaternary, 31 (2), 2018, 171 - 194 

STRATIGRAPHY OF THE PALATINE HILL (ROME, ITALY): 
A RECORD OF REPEATED MIDDLE PLEISTOCENE-HOLOCENE  

PALEOVALLEY INCISION AND INFILL 
 

Marco Mancini1, Mattia Marini2, Massimiliano Moscatelli1, Francesco Stigliano1, 
Gian Paolo Cavinato1, Cristina Di Salvo1, Maurizio Simionato1  

 
1 Consiglio Nazionale delle Ricerche, Istituto di Geologia Ambientale e Geoingegneria, Rome, Italy 
2 Università degli Studi di Milano, Dipartimento di Scienze della Terra “A. Desio”, Milan, Italy  

 
Corresponding author: M. Mancini <marco.mancini@igag.cnr.it>  

 
ABSTRACT: The Palatine Hill in Rome (Italy) represents a key site for better understanding the Middle Pleistocene-Holocene 
continental deposits of the Rome basin that could be investigated by the numerous boreholes drilled during the last few decades 
for archeological and cultural heritage conservation. In this study, 12 cores selected for their excellent recovery rate and strati-
graphic coverage are described in detail discriminating 23 lithofacies. The stratigraphic data, used in combination with the informa-
tion from nearby outcrops and additional boreholes provide insights into the depositional architecture of multiple incised fluvial 
valley infills developed in response to sea-level fluctuations occurred between Marine Isotope Stages (MIS) 16 and 1. These infills 
comprise a range of fluvial deposits of the Tiber River system which interfinger with accurately dated pyroclastites from the Alban 
Hills and Sabatini Mts., thus providing important time constraints on the formation of paleovalleys. The paleovalleys correlated to 
MIS 14-13, 12-11 and 5d-1 have particularly well-preserved infills constituting useful analogues of trunk and tributary paleovalleys. 
Because the recognized lithofacies represents the building blocks of the lithostratigraphic, synthemic and sequence stratigraphic 
units currently in use at basin-scale, we believe their accurate field and core description complemented by graphical logs and pho-
tographic plates is important for identifying similar facies in future investigations on nearby paleovalley infills. 
 
Keywords: fluvial paleovalleys, Middle Pleistocene, Holocene, Rome, facies analysis   

1. INTRODUCTION 
 

Urban geology requires thoughtful integration of 
geognostic data (borehole lithology, geotechnical tests, 
geophysics) and information from nearby outcrops, 
which are often sparse due to cover by man-made de-
posits and structures. In sedimentary successions, this 
requires a hierarchical approach entailing prior recogni-
tion of key stratigraphic surfaces bounding genetically-
linked deposits, followed by detailed borehole lithology 
correlation. Implementing such an approach is particu-
larly challenging in superimposed unconformity bounded 
stratigraphic units (USBU), such as multiple fluvial in-
cised valleys lacking a robust stratigraphic reference 
model.  

Fluvial incised valleys, or paleovalleys (sensu 
Blum et al., 2013) develop in the lower reach of fluvial 
systems as a result of readjustment of the equilibrium 
profile following base level changes driven by eustasy, 
tectonics or a combination of the two. During Quater-
nary, the dynamics governing paleovalley incision and 
sedimentary infill is primarily modulated by glacio-
eustatic sea-level fluctuations (Wright & Marriott, 1993; 
Shanley & Mc Cabe, 1994; Blum et al., 2013), with for-
mation of a basal high-relief unconformity deeply eroded 
into older deposits (or the bedrock) during base level 
falls and low-stands, and subsequent backfilling during 
base level rises and high-stands. 

Understanding the subsurface stratigraphy of ur-

ban areas characterized by the presence of paleovalleys 
is made even more challenging by the poor quality and/
or detail consistency of the typically available subsurface 
data, which are in general compiled from different 
sources (technical reports, geological maps, research 
papers) over time spans of a few to several tens of 
years. However, several study cases exist where physi-
cal-stratigraphy, facies analysis and sequence stratigra-
phy concepts are used to guide interpretation and mod-
elling of subsurface datasets from urban areas (Ellison 
et al., 2004; Sarti et al., 2012; Amorosi et al., 2013; 
Bridgland et al., 2013; Tanabe et al., 2015; Milli et al, 
2016; Van Dinter et al., 2017; Marini et al., 2018, among 
the others). 

The present contribution reports on the sedimen-
tary facies from Middle Pleistocene to Holocene fluvial 
paleovalley infills from the Palatine Hill of Rome (Italy), a 
world-class archeological site whose subsurface was 
deeply investigated over the last decades for cultural 
heritage preservation purposes (Cecchi, 2011). Based 
on detailed logging of cores from 12 boreholes with ex-
cellent recovery and stratigraphic record and ancillary 
observations from nearby outcrops (some of which tem-
porary), this work intends to: i) give insights into the 
facies architecture of excellent examples of paleovalley 
infills with a well-established stratigraphic framework 
owing to intercalation of dated volcanics; ii) refine the 
existing models of subsurface geology (Moscatelli et al., 
2012, 2014a, 2015; Mancini et al., 2013, 2014), and iii) 

 

https://doi.org/10.26382/AMQ.2018.11 



   

 

 
 
172 

 

Fig. 1 - a) Location of the Palatine Hill within the historical center of Rome; the inset is referred to Fig. 1b. b) Topographic map of the Pala-
tine and surrounding areas. 

 
 

Mancini M. et al. 



   

 

 
 

173 

A key element of the volcano-sedimentary complex 
is the stack of paleovalley infills (Blum et al., 2013), or 
fluvial incised valleys, and related interfluves resulting 
from cyclic, syn-uplift phases of fluvial sedimentation 
and erosion by the Tiber River and tributaries (Conato et 
al., 1980; Alvarez et al., 1996; Milli 1997; Karner & 
Marra, 1998; Marra et al., 1998, 2008, 2016; Milli et al., 
2008, 2016; Mancini et al., 2013). At present, the Upper 
Pleistocene-Holocene drainage network of the Tiber 
River is deeply incised into older deposits as a result of 
the sea-level fall of Marine Isotope Stages (MIS) 5d-2 
and hosts up to 65 m of Upper Pleistocene-Holocene 
(MIS 2-1) fluvial sediments forming the present-day flu-
vial plain (Bozzano et al., 2000; Milli et al., 2016). Fi-
nally, an almost continuous cover of anthropogenic de-
posits is present in the whole urban area, with thick-
nesses up to 20 m (Ciotoli et al., 2015, with references). 

 
3. MATERIAL AND METHODS  

 
In this work we adopt the high-rank Unconformity 

Bounded Stratigraphic Units (UBSU), or synthems, and 
the lithostratigraphic units that compose them (i.e. for-
mations) of the Geological Map of Italy (map sheet 374 
‘Rome’; Funiciello & Giordano, 2008). Bounded by 5 
major basal unconformities (Unconformities I to V in Fig. 
3) corresponding to as many phases of fluvial erosion 
forced by sea level fall and low-stand (even-numbered 
Marine Isotopic Stages, MIS), the above mentioned 
synthems partly correspond to paleovalleys infills devel-
oped during phases of sea level rise and high-stand, 
which could be correlated with some of the high-
frequency low-rank depositional sequences of the com-
posite Ponte Galeria Sequence (Fig. 3a; Milli, 1997; Milli 
et al., 2008, 2016) well defined W of Rome. An addi-
tional composite surface (Surface VI in Fig. 3), locally 
erosive or depositional, is at the base of the anthropo-
genic deposits.  

A sub-set of 12 (most of which double-tube cored) 
out of 25 continuous-core boreholes (Fig. 1) drilled in the 
2010 (Cecchi, 2011) was selected for their excellent 
core recovery, stratigraphic record and proximity to key 
outcrops, and logged in detail recording all relevant sedi-
mentologic, petrographic and pedogenetic information 
across most of the Middle Pleistocene-Holocene suc-
cession. This allowed the distinction of a total of 23 litho-
facies (Table 1) described in detail in paragraph 4 and 
illustrated in Figs. 4-9 and Plate I-III. After integration 
with lithostratigraphy from other boreholes and ancillary 
observations made on nearby key outcrops, including 
temporary outcrops from archeological excavations and 
construction sites, the selected core logs were corre-
lated across adjacent sites based on stratigraphic mark-
ers (e.g. ignimbrites, fluvial lag deposits, lignite seams, 
tephras) and used for facies analysis (Miall, 1996; Orton, 
1996; Retallack, 2001; Amorosi, 2006). 

 
4. RESULTS: STRATIGRAPHY AND SEDIMENTARY 
FACIES 
 

The stratigraphy of the Palatine (Figs. 3b, 4) in-
cludes five of the USBU introduced by Funiciello & 
Giordano (2008), namely the Flaminia (LMN), Villa Glori 

provide detailed descriptions and iconographic material 
useful for identifying similar facies in future investiga-
tions in nearby areas and similar deposits.  
 
2. GEOLOGICAL AND STRATIGRAPHIC SETTING  

 
The Palatine (Fig. 1a) is one of the world-renown 

“Seven Hills” of Rome, onto which the city was founded 
(De Angelis D’Ossat, 1956; Heiken et al., 2005; Fu-
niciello et al., 2006). It is a 25-ha wide flat-topped hill 
with an elevation of ca. 50 m a.s.l. composed by a com-
plex stack of sedimentary and pyroclastic rocks. To NW, 
SW and SE the Palatine is bounded by the relatively 
narrow Velabro, Murcia and Labicano alluvial valleys, 
which separate it from the Capitoline, Aventine and 
Caelius Hills, respectively (Fig. 1b).  

Because the Palatine hosted the first settlement of 
ancient Rome (Brocato & Terrenato, 2016), the present-
day landscape records a long-lasting history of anthro-
pogenic modifications, witnessed by several superim-
posed archaeological ruins of different ages. The Pala-
tine is bounded to NE by the Fori Imperiali-Roman Fo-
rum, a mixed natural and anthropogenically-modified 
depression separating the Palatine from the nearby 
Oppius Hill. In this specific place, the small former Velia 
Hill was present until the 30s of the 20th century (Fig. 
1b), when it was cut away for the construction of Via dei 
Fori Imperiali (De Angelis D’Ossat, 1956; Palombi, 
1997, 2016; Lanzini, 2008; Leone et al., 2009). The 
morphology of the Palatine itself was modified. Origi-
nally, it, featured two culminations to the SE and the W 
of the present-day hilltop referred to by historians as 
Palatium and Germalus, respectively (Castagnoli, 
1980). 

The Seven Hills are located at the periphery of the 
volcano-sedimentary plateau of the Alban Hills and Sa-
batini Mts Volcanic Districts, whose deposits were in-
cised by the Tiber River and its tributaries (Fig. 2) (Del 
Monte et al., 2016). The Pliocene-Quaternary succes-
sion of the area represents part of the infill of the Rome 
Basin, an extensional basin developed since the earliest 
Pliocene as a result of back arc extension in the Tyrrhe-
nian Sea (Patacca et al., 1990; Cavinato & De Celles, 
1999; Mattei et al., 2010). 

The geological bedrock of this succession consists 
of up to 900 m-thick Pliocene marine sediments 
(comprising the clayey Monte Vaticano Formation), 
which overlay with angular unconformity the Mesozoic-
Cenozoic carbonate and siliciclastic successions of the 
Central Apennines (Funiciello & Parotto, 1978; Fu-
niciello & Giordano, 2008; Giordano & Mazza, 2010). 
The Pliocene sediments are in turn overlain by 
Calabrian shallow marine sediments and by a 30-150 m
-thick suite of latest Early Pleistocene-Holocene vol-
canic and sedimentary deposits (Conato et al., 1980; 
Milli, 1997; Marra et al., 1998, 2008, 2009; Giordano et 
al., 2003, 2006; Funiciello & Giordano, 2008, 2010; 
Cosentino et al., 2009; Luberti et al, 2017). This volcano
-sedimentary succession recorded complex phases of 
syn-uplift, climate-eustatically forced and volcano-
controlled basin infill, with pyroclastites and lavas 
sourced from the Sabatini Mts and Alban Hills Districts 
(Fig. 2). 

 
 
Stratigraphy of the Palatine Hill 



   

 

 

 
 
174 

Fig. 2 - a) Simplified geological map of the Rome Basin. Legend: 1) continental and coastal deposits (late Early Pleistocene-Holocene); 2) 
pyroclastic deposits and lavas of the Sabatini Mts and Alban Hills Volcanic Districts (Middle-Late Pleistocene); 3) marine terrigenous clay 
and sands (Pliocene-Early Pleistocene); 4) lavas and lava domes of the Ceriti Mts-Tolfa Volcanic District (Pliocene); 5) marine terrigenous 
successions of the Liguride Units, sandstones and marlstones (Cretaceous-Paleogene); 6) limestone, marls and cherts of the pelagic Um-
bro-Sabina succession (Trias-Miocene); 7) normal fault; 8) buried normal fault. CAA is the Central Archeological Area of Rome. b) Geologi-
cal map (modified, after Mancini et al., 2014) showing the distribution of lithostratigraphic units below the anthropogenic deposits with loca-
tion of cross-sections of Fig. 4, outcrops pictured in Figs. 5 and 6, and borehole stratigraphies detailed in Figs. 7-9. 

 
 

Mancini M. et al. 

(Florindo & Marra, 1995) 



   

 

(VGL), Torrino (TNO), Quartaccio (QTA) and Fiume 
Tevere (SFT) Synthems, which correspond to as many 
incised paleovalleys infills and stack spatially to form the 
volcano-sedimentary multilayer superimposed onto the 
Pliocene marine bedrock. This stack is covered by a 

thick layer of man-made deposits. In the following para-
graphs, the component lithofacies (Table 1) and geo-
metrical characters of these units, including the bedrock 
and the man-made cover, will be described in detail and 
illustrated with a rich iconographic documentation from 

 
 

175 

Fig. 3 - a) Chronostratigraphic reference scheme for the Palatine Hill and surrounding areas reporting correlation between (1) sequence 
stratigraphic units (Milli, 1997), (2) lithostratigraphic and unconformity bounded stratigraphic units (Funiciello & Giordano, 2008) and (3) 
marine isotope stages (MIS; after Shackleton et al., 1990). b) Simplified sketch of the stratigraphic and facies architecture of the Palatine 
Hill and the surrounding Labicano and Velabro Valleys (see a in this figure and text for lithostratigraphic and facies codes). In both figures, 
stratigraphic surfaces I to V are the unconformities bounding the synthems of Funiciello & Giordano (2008), and surface VI is at the base of 
the man-made deposits. 

 
 
Stratigraphy of the Palatine Hill 



   

 

selected core intervals (Plates I-III) and key outcrops 
(Figs. 5, 6). 

 
4.1 Pliocene marine bedrock: the Monte Vaticano 
Formation (MVA)   

In the study area this formation does not crop out 
but was encountered in numerous boreholes and drilled 
throughout a total thickness of 500 m by the Circo Mas-
simo well (cfr with LPa unit in Funiciello & Giordano, 
2008). The formation is represented by a single lithofa-
cies (MVA) composed of structureless blue-grey silty 
clay (Plate I a), with rare burrows and marine shells 
(Corbula gibba, Venus sp.) and with interbedded dm-
thick sets of organic-rich cross laminated sands (Plate I 
b). 
Interpretation. The clays of MVA are interpreted as the 
product of fall-out and, subordinately, traction plus fall-
out deposition by gravity flows in outer shelf to slope 

offshore marine settings. 
 

4.2 Flaminia Synthem (LMN) 
Bounded below and above by Unconformities I and 

II (Fig. 3b), respectively, the Middle Pleistocene syn-
volcanic Flaminia Synthem (Funiciello & Giordano, 
2008) can be correlated with MIS 16-15 and with the 
PG3 depositional sequence (Milli, 1997). In the study 
area LMN only comprises the fluvial Santa Cecilia For-
mation (CIL) introduced by Marra et al. (1998) and geo-
chronologically constrained by Karner & Marra (1998). 

 
4.2.1 Santa Cecilia Formation (CIL) 

The Santa Cecilia Formation (cfr. with 
‘Maremmano’ in De Angelis D’Ossat, 1956) is up to 20 
m thick in the study area and includes two lithofacies, 
namely channel gravel (CIL A) and sand (CIL B), occur-
ring respectively below and above a sharp and rather 

 
 
176 

Tab. 1 - Correlation scheme among depositional sequences, synthems, formations and lithofacies. 

 
 

Mancini M. et al. 

 
>>>>> 

 

Fig. 4 - Geological cross-sections (see Fig. 2b for location) with distribution of clustered lithofacies described in the text (modified after 
Mancini et al., 2014). The buried normal fault on cross sections 2 and 3 is inferred from the displacement of stratigraphic horizons at the 
base of and within the Fosso del Torrino Fm; its activity ended before the deposition of the Villa Senni Formation (see Mancini et al., 2014, 
for further details). 



   

 

 
 

177 

 
 
Stratigraphy of the Palatine Hill 

Capitoline Hill 

Capitoline Hill 

Palatine Hill 

Palatine Hill 

Velabro Valley 
Labicano Valley 

Labicano Valley Velabro Valley 

Aventine Hill 

Circo Massimo 
(Murcia Valley) 

Domus Tiberiana 

Roman Forum 

 



   

 

flat intra-formational surface (Figs. 8, 9). 
 

Channel gravel (CIL A) 
This lithofacies is represented by well-sorted, 

coarse to medium-grained pebbles in a sandy matrix 
(Plate I c) and, subordinately, by sands forming dm-thick 
lenses with low (m-scale) lateral continuity. Clasts are 
calcareous and subordinately siliceous (up to 10-15%) 
and typically well-rounded with mainly blade and disc 
shape. The sandy matrix is fine grained and mainly 
composed of quartz, feldspar, calcite and, subordi-
nately, volcanic ferro-magnesian minerals. 

In the study area, CIL A forms an 8-20 m-thick 
wedge-shaped depositional body thickening toward the 
NW (Fig. 4). 
Interpretation. CIL A can be interpreted as a stack of 

longitudinal and transversal bars and bedload sheets 
infilling the channels of a gravelly braided-type river. 
Major grain-size breaks between pebbles and sands can 
be interpreted as either bedset boundaries within individ-
ual bars and gravel-sand sheets or reflect auto-cyclical 
reorganization of the channel-network. 

 

Channel sand (CIL B) 
This facies is composed of silty fine-medium sands 

(Plate I d), typically of a yellow-orange hue, showing 
either faintly planar-parallel or ripple-drift cross lamina-
tion. The mineralogical composition of CIL B is the same 
as the matrix of CIL A including relatively abundant chert 
fragments. Locally, dm-thick, normally and inversely 
graded lamina-sets are observed, which suggests flow 
velocity fluctuations. In most localities, these sands 

 
 
178 

Fig. 5 - Pictures of key outcrops discussed in the text (see Fig. 2b for reference and location). a) Roman walls and foundation structures 
along the north-western side of the Palatine. Note how these ruins sit directly on top of outcrop 1 (see details in this figure). b) Detail of the 
lowermost part of outcrop 1 showing pedogenized floodplain mud (VGU C) capped by cross-laminated levee sand (VGU B) from the fluvial 
Valle Giulia Formation. c) Detail of outcrop 1 showing cross-laminated levee deposits with a well-developed paleosol on top (VGU B litho-
facies) overlain with a sharp but non-erosive contact by the massive ignimbritic Palatino Unit (PTI). Note the presence of tree moluds in 
PTI, previously described by De Rita et al. (2002). d) From base to top, carbonate-rich silts and concretions (VGU C lithofacies) and the 
PTI and the Villa Senni Formation (VSN) ignimbrites exposed in outcrop A (Via della Consolazione, southern hillslope of the Capitoline 
Hill). e) Detail of the PTI ignimbrite in outcrop A showing a sub-angular, carbonate lithic fragment, most likely a xenolith (see e.g. Funiciello 
& Parotto, 1978). 

 
 

Mancini M. et al. 



   

 

 
 

179 

Fig. 6 - a) The superimposed Palatino Unit (PTI), Prima Porta Unit (PPT) and Villa Senni Formation - Tufo Lionato (VSN1a) pyroclastic 
deposits in outcrop B (Via della Consolazione). b) Detail of outcrop B showing the paleosol separating the Palatino Unit (PTI) from the 
Prima Porta Unit (PPT). c) Epiclastite of the Fosso del Torrino Formation (FTR G) located between the pyroclastites of the Prima Porta 
Unit (PPT) below and the Villa Senni Formation - Tufo Lionato (VSN1a) above in outcrop 2 (San Teodoro Church). Note the faintly lami-
nated ashy character as well as the pedogenized top of PPT. d) Detail of outcrop 3, temporary exposed in April 2015 during the Under-
ground Line C excavations, showing the fluvial channel sand (FTR B) of the Fosso del Torrino Formation, topped by the Villa Senni Forma-
tion - Tufo Lionato (VSN1a) ignimbrites. e) Detail of outcrop 4, temporary exposed in May 2018 during the Underground Line C excava-
tions, showing trough-cross bedded and cross laminated sands (FTR B) of the fluvial Fosso del Torrino Formation. Outcrops 3 and 4 are 
remnants of the former Velia Hill, cut away in the 30s of the XX century for the construction of Via dei Fori Imperiali (De Angelis D’Ossat, 
1956; Lanzini, 2008; Leone et al., 2009). f) Detail of outcrop 2 showing a columnar gas pipe from the Tufo Lionato ignimbrite (VSN1a). 

 
 
Stratigraphy of the Palatine Hill 



   

 

 

 
 
180 

grade upward into massive sandy silt (Figs. 7-9) bearing 
rare root traces and mm-to-cm-scale nodules of Mn/Fe 

oxides. Similar fine-grained facies were reported by 
Florindo & Marra (1995) and Florindo et al. (2007) from 
the Colosseum core A (Fig. 9), which were attributed to 
the Brunhes magnetic chronozone. CIL B forms an up to 
8 m thick tabular body with an observed minimum lateral 
continuity of 250 m. 
Interpretation. CIL B can be interpreted as a channel-
fill deposit resulting from amalgamation of subsequent 
bars and bedload sheets in a sand-dominated river. 
Root traces and nodules can be interpreted to reflect 
prolonged subaerial exposure and pedogenisation of 
bar tops. The silty deposits may be related to upper bars 
and/or abandoned channels. 

 
4.3 Villa Glori Synthem (VGL) 

The syn-volcanic Villa Glori Synthem (VGL; Fu-
niciello & Giordano, 2008) is bounded below and above 
by Unconformities II and III (Fig. 3b) which record the 
sea level falls occurred between MIS 15 and MIS 14 
and MIS 13 and MIS 12, respectively. As a result, there 
is general agreement in correlating VGL with MIS 14-13 
and the PG4 depositional sequence (Milli, 1997; Fu-
niciello & Giordano, 2008). In the study area, VGL com-
prises the Valle Giulia Formation (VGU), composing the 
most of the synthem (Figs. 3b, 7), and the Palatino (PTI) 
and the Prima Porta (PPT) pyroclastic units. These units 
collectively represent of the infill of a NW-SE trending 
paleovalley (Mancini et al., 2014). 

 
 
 

4.3.1 Valle Giulia Formation, VGU 
The fluvial Valle Giulia Formation is up to 15 m 

thick and includes three lithofacies, namely channel 
gravel (VGU A), channel margin-levee sand (VGU B) 
and pedogenized floodplain and channel-abandonment 
silt (VGU C). 

 

Channel gravel (VGU A) 
This facies consists of medium to coarse well-

rounded blade-shaped pebbles (Plates I e, II a) with an 
abundant sandy matrix. Clast lithology includes lime-
stone, chert and volcanic scoria, whereas the matrix is 
very rich in calcite, quartz, charcoal debris and volcanic 
ferro-magnesian minerals (clinopyroxene, biotite and 
magnetite), which imparts VGU A a dark hue and makes 
it easily distinguishable from similar lithofacies (e.g. CIL 
A and FTR A). Importantly, in the subsurface of the 
north-eastern hill slope of the Palatine, VGU A is interca-
lated by the pyroclastic Palatino Unit (PTI) (log 11 MS in 
Fig. 7). 

VGU A exclusively occurs at heights below 15 m 
a.s.l., infilling the deeper part of Unconformity II (Figs. 3 
and 4). Because of later erosion of Unconformity III, it 
forms depositional bodies with presumably small lateral 
continuity and slightly convex erosive base. 
Interpretation. Channel-fill fluvial deposits, formed by 
amalgamation of bars and bedload sheets in a braided-
type river (Fig. 7). The abundance of volcanic clasts as 
well as intercalation of PTI testifies syn-volcanic deposi-
tion. 

 

Channel margin-levee sand (VGU B) 
This facies is represented by light brown to pale 

Fig. 7 - Correlated sedimentary logs from selected boreholes and key outcrops along the Velabro Valley and in the north-western Palatine 
(see Fig. 2b for location). 

 
 

Mancini M. et al. 



   

 

grey, cross-laminated silty fine sand (Plates I f, II b), 
dominantly composed of quartz, feldspar, muscovite 
and volcanic ferro-magnesian minerals. VGU B form m-
thick beds sets (Figs. 5 b, c), whose base is locally 
marked by lags of very fine to fine pebbles. On outcrop, 

cross bedding and ripple-drift laminations indicate pa-
leoflow direction toward the W (Fig. 5 b, c; log 13 MS in 
Fig. 7). Locally, root traces and peds are present atop 
VGU B beds (Fig. 5 c). 

VGU B was encountered at a few sites only (e.g. 

 
 

181 

Fig. 8 - Correlated sedimentary logs from selected boreholes from central Palatine Hill (see Fig. 2b for location). Legend as in Fig. 7. 

Fig. 9 -. Correlated sedimentary logs from selected boreholes in the eastern Palatine Hill and Oppius Hill (see Fig. 2b). Note the internal 
facies variability of the Fosso del Torrino Formation (FTR) reflecting intercalation of crevasse sandy deposits within floodplain muds. Leg-
end as in Fig. 7. 

 
 
Stratigraphy of the Palatine Hill 



   

 

Fig. 5 b, c; log 13 MS in Fig. 7) at elevation above 5 m 
a.s.l., suggesting it forms laterally discontinuous bodies 
up to 5 m thick. 
Interpretation. Deposition by sand-laden waning flows 
in channel margin and levee settings. The levee depos-
its, particularly well exposed along man-made cuts on 
the NW flank of the Palatine Hill (Fig. 5b), can be differ-
entiated from channel margin deposits based on vertical 
association with underlying floodplain deposits (i.e. litho-
facies VGU C, see log 13 MS in Fig. 7) and presence of 
pedogenic features. 

 

Pedogenized floodplain and channel-abandonment 
silt (VGU C)  

VGU C consists of pale to dark grey-brown, partly 
calcite-cemented, massive sandy silt (Plate I e; Figs. 5 
b,d), interbedded with dm-thick beds of detrital freshwa-
ter tufa and lignite. As previously described for VGU A 
and B, the sandy fraction is very rich in volcanic ferro-
magnesian minerals (clino-pyroxene and biotite). In few 
localities, well-developed clayey paleosols is found atop 
VGU C (e.g. log 13 MS, see Figs. 5 b and 7) containing: 
prismatic and angular blocky peds (up to 5 cm long) 
typical of Bt soil horizon (illuvial clay, see Retallack, 
2001), dark brown cutans (Fe/Mn oxides), calcium car-
bonate depleted horizons, root traces and abundant 
shells of the terrestrial gastropod Pomatias elegans.  
Interpretation. This facies derives from suspension and 
traction-fall out processes, characterized by low energy 
waning flows related to overbanking in floodplains (log 
13 MS in Figs. 5 b and 7) and abandoned channels (log 
11 MS in Fig. 7, Plate 1 e). Pedogenetic characters 
suggest the establishment of partly drained and oxidiz-
ing conditions. The prismatic and angular blocky peds 
may, in fact, reflect repeated swelling and shrinking 
resulting from alternation of wetting-drying conditions 
(Retallack, 2001). Coarsening upward facies sequences 
including interbedded VGU C and VGU B (e.g. log 13 
MS in Fig. 7; Figs. 5 b, c) can be interpreted to reflect 
lateral shifts of the fluvial system axes resulting in pro-
gradation of levees onto floodplain mud (Brierly et al., 
1997; Hornung & Aigner, 1999). 

 
4.3.2 Palatino Unit (PTI) 

The Palatino Unit is an ignimbrite marker-bed rep-
resenting the product of a single pyroclastic flow 
sourced from the Alban Hills (Funiciello & Giordano, 
2008). It partly corresponds to the “Cappellaccio” and 
“Tufo granulare” described by De Angelis D’Ossat 
(1956) and yielded a 40Ar/39Ar age of 528 ± 1 ka (Karner 
et al., 2001) and 520 ± 8 ka (Karner & Renne, 1998). 

In the study area PTI crops out along the Velabro 
Valley (Figs. 5a; 6a, b), where intercalates into VGU 
fluvial deposits. It is represented by a dark grey, mas-
sive tuff (Figs. 5c-d) with a weakly pedogenized top (Fig. 
6b; Plate II c), made of an ash matrix with floating crys-
tals (leucite, biotite, clino-pyroxene), black scoriae 
(Plates I f, II a-c), poorly-rounded lithics (Fig. 5e) inter-
preted as xenoliths (Funicello & Parotto, 1978), and tree 
moulds (Fig. 5d). At some sites (log 13 MS in Fig. 7), 
the lowermost few cm of PTI contains abundant well-
rounded fine pebbles of limestone and chert (Plate II b).   

Though occurring at different elevations, PTI 

shows small thickness changes (c. 5 m) suggesting 
mantling of the pre-existing topography. 
Interpretation. PTI character suggest deposition by a 
high density pyroclastic flow onto an articulated topogra-
phy including interfluves. The lithic pebbles in the lower-
most part of PTI (Fig. 5e) likely represents clasts ripped 
up from the channel floor and re-deposited in off-axes 
locations of the VGL valley (log 13 MS in Fig. 7). Tree 
moulds represent casts of burned tree trunks and 
branches (De Rita et al., 2002). 
 
4.3.3 Prima Porta Unit (PPT) 

The pyroclastic Prima Porta Unit crops out along 
the western flank of the Palatine and the south-eastern 
flank of the Capitoline (Figs. 6 a-c), overlaying PTI and 
VGU. It corresponds to the “Tufo granulare” pro parte in 
De Angelis D’Ossat (1956) and to the “Tufo Giallo di 
Prima Porta” in Karner et al. (2001) and Luberti et al. 
(2017). Sourced from the Sabatini Mts Volcanic District, 
this unit yielded 40Ar/39Ar radiometric ages of 514 ± 3 ka 
(Karner et al., 2001) and 514 ± 6 ka (Marra et al., 2014). 
The outcrop of PPT on the Capitoline Hill (Figs. 6 a, b) 
was attributed to the Fosso del Cavaliere Unit by De 
Rita & Fabbri (2009). 

In the study area, PPT is represented by green-
grey tuffs composed of well-sorted, fine ashes (Plate II 
c; Figs. 6 a-c) with faint planar-parallel lamination, con-
taining scattered sub-centimetric pumice. The top of the 
unit is marked by a yellowish clayey paleosol with root 
traces. The unit is composed of two superimposed later-
ally continuous bodies, each up to 4 m thick, separated 
by a planar amalgamation surface. Observed thickness 
changes of PPT are very small, suggesting tabular ge-
ometry over short lengths. 
Interpretation. PPT can be interpreted as the distal 
product of two pyroclastic flows, originated from highly 
fragmented magma of phreato-magmatic origin. Planar-
parallel lamination testifies deposition under upper re-
gime conditions by low-density flows. 

 
4.4 Torrino Synthem (TNO) 

The Torrino Synthem (Funiciello & Giordano, 2008) 
is correlated with MIS 12-11 and PG5 depositional se-
quence (Milli, 1997), and is bounded at the base by the 
high relief Unconformity III. In the study area TNO com-
prises only the Fosso del Torrino Formation (FTR) and 
represents the infill of a NW-SE (north-eastern hillslope 
of Palatine and Fori Imperiali) to N-S (eastern hillslope 
of Palatine and Labicano Valley) (Figs. 2 and 10) di-
rected paleovalley (Mancini et al., 2013, 2014; Mosca-
telli et al., 2015). 

 
4.4.1 Fosso del Torrino Formation (FTR) 

The Fosso del Torrino Formation (FTR) is up to 40 
m thick and comprises several facies including channel 
gravel (FTR A) and sand (FTR B), poorly and well-
drained floodplain mud (FTR D and F, respectively), 
buried colluvia (FTR E) and epiclastites (FTR G). This 
formation partly corresponds to the San Cosimato For-
mation (Conato et al., 1980) and to the San Paolo For-
mation, with the latter reported from the subsoil of the 
nearby Quirinale (Marra & Rosa, 1995) and Capitoline 
Hills (Corazza et al., 2004). It is noteworthy that the 

 
 
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183 

 
 
Stratigraphy of the Palatine Hill 

Examples of lithofacies from selected cores (bottoms and tops in the lower left and upper right, respectively; core box is 1 m-long), with 
main facies boundaries marked in red. a) Over-consolidated marine clay of The Monte Vaticano Formation (MVA; Pliocene) overlain by 
fluvial channel gravel (FTR A) of Fosso del Torrino Formation (Middle Pleistocene) in borehole 22 P (depth interval 40-35 m); b) dm-thick 
cross laminated sands intercalating the clays of MVA (detail from core of borehole 8 MS). Santa Cecilia Formation (Middle Pleistocene): c) 
channel gravel (CIL A) from borehole 2 MS (depth interval 15-10 m) and d) cross-laminated channel sand (CIL B) from borehole 16 MS 
(depth interval 30-25 m). e) The Valle Giulia Formation (Middle Pleistocene) in borehole 11 MS (dept interval 20-15 m): channel gravel 
(VGU A) passing upward to channel-abandonment fines of VGU C. Note the dark-grey hue of the VGU A sandy matrix, rich in ferro-
magnesian minerals; f) channel sand of the Santa Cecilia Formation (CIL B), overlain by grey overbank sand of VGU B lithofacies and by 
structureless ignimbrite of the Palatino Unit (PTI; Middle Pleistocene) from borehole 1 MS (depth-interval 30-25 m). 

Plate I 



   

 

sand of FTR B represents the matrix of a vertebrate 
fossil assemblage (including Elephas antiquus, Bos 
primigenius, Cervus elaphus, Hippopotamus amphibi-
ous) unearthed during the excavation of Via dei Fori 
Imperiali (De Angelis D’Ossat, 1956). 

 

Channel gravel (FTR A) 
This facies is represented by poorly sorted, coarse

-medium gravels in an abundant sandy matrix (Plates I 
a and II d), frequently intercalated with dm-thick beds of 
beige cross-laminated sands. Clasts are carbonate, 
chert and tuff lithics, generally well-rounded and blade-
shaped. The sandy-silty matrix, reddish to dark grey in 
colour, is very rich in volcanic ferro-magnesian minerals 
and chert. 

FTR A occurs at elevations below -2 m a.s.l., infill-
ing the deepest part of Unconformity III and forming a 
flat-topped channel-fill body up to 10 m-thick and at 
least 200 m-wide across. 
Interpretation. FTR A represents a stack of longitudinal 
bars and bedload sheets infilling the channels of a grav-
elly-sandy braided river. 

 

Channel and crevasse-splay sand (FTR B) 
FTR B is represented by yellow to light brown 

cross-laminated and through-cross bedded sands with 
quartz, feldspar and muscovite and volcanic ferro-
magnesian minerals (augite, biotite, magnetite), inter-
bedded with dm-thick beds of silt (Plate II d; Fig. 6d-e). 
Sand and silt are vertically arranged to form meter-thick 
bed-sets with alternated fining- and coarsening-upward 
patterns (e.g. logs 9 MS, 18 MS and 22 MS on Figs. 8 
and 9); the coarsening-upward pattern typifies those 
FTR B bed-sets interbedded as isolated lenses within 
floodplain mud (FTR D, see below), in the subsurface of 
the eastern Palatine. Apart from these lenses, FTR B 
forms a main depositional body up to 30 m thick, which 
can be tracked from N to S for at least 500 m where the 
base of FTR is most deeply incised (Roman Forum and 
Labicano Valley, Fig. 4). Toward the W, FTR B inter-
fingers with mud-prone floodplain deposits (FTR D). 
Interpretation. Bedding pattern, sedimentary structures 
and large-scale geometry suggest that the main deposi-
tional body of FTR B might represent the result of a 
multistorey-multilateral stack within a fluvial channel-
belt, composed of sandy bed-load sheets and bars re-
ferred to a mixed bed/suspended-load meandering flu-
vial system. Lenticular FTR B bed-sets within floodplain 
muds are interpreted as crevasse splay deposits 
(Basilici, 2000). 
 

Poorly-drained floodplain mud (FTR D) 
This lithofacies is represented by blue-grey to tur-

quoise structureless clay (Plate II e, f), locally interlay-
ered with cm-thick beds of muscovite-rich very fine silty 
sands with faint planar-parallel lamination. Pale grey to 
yellowish mottles and white-yellow small micritic carbon-
ate nodules (Plate II e) are commonly observed in the 
clays, especially in the lower part of FTR D (logs 22 P 
and 9 MS; Fig. 9). Plant debris is scattered throughout 
the upper part of FTR D but is particularly abundant at 
about 20 m a.s.l., forming laterally continuous lignite 
seams traceable across adjacent boreholes (Fig. 8; 
Plate II f).  

This lithofacies is up to 25 m thick and can be 

traced laterally for at least 300 m in the subsoil of the 
eastern portion of the Palatine, before it passes laterally 
to FTR B north- and east-ward. 
Interpretation. Lateral association with channel facies 
suggests that FTR D represents the product of suspen-
sion fall-out and, subordinately, traction-fall out deposi-
tion by repeated overbanking in a floodplain environ-
ment (Davies & Gibling, 2003; North & Davidson, 2012). 
Structureless mud may represent the deposit of either a 
shallow flood-basin ponds or distal floodplain setting (cfr 
with Fm lithofacies of Miall, 1996), whereas thin sand/
mud alternations might reflect weak tractional waning 
flows in more proximal setting (cfr facies Fl by Miall, 
1996, and lithofacies association SL by Ghinassi et al., 
2005). The abundance and preservation of plant frag-
ments suggests waterlogged conditions typical of poorly 
drained floodplain, which might have favoured lignite 
seams formation via accumulation of reotrophic peat in 
low-lying swamps (Mc Cabe, 1984; Fielding, 1985). 
Conversely, mottles and carbonate nodules are pe-
dogenic hydromorphic features (gleying) best interpreted 
to reflect ground-water oscillations (Kraus & Aslan, 
1993) in a partially waterlogged environment.  
 

Colluvium (FTR E) 
This facies consists of yellow-brown to grey, poorly 

sorted and massive silt and fine sand with abundant tuff 
fragments and ferro-magnesian minerals. It fills two SW-
NE trending gullies underneath the Domus Tiberiana 
(Fig. 4) cutting older pyroclastic rocks. 

Interpretation. FTR E is interpreted as the deposit 
of multiple gravity-driven mass flows along the flanks of 
local gullies. 

 

Well-drained floodplain mud (FTR F) 
This facies is composed of pale yellow to brown, 

structureless silty clay with cm-scale sub-spherical iron 
oxides mottles, calcium carbonate concretions and root 
traces, intercalated with planar-parallel laminated silts 
and sands with a typical yellow-reddish hue (Plates II f, 
III a-d). Particularly noteworthy are two cm-thick tephra 
occurring in the uppermost part of FTR F (logs 2 A and 3 
A in Fig. 9; Plate III b).  
Interpretation. As previously discussed for similar mud-
prone facies, FTR F reflects floodplain deposition. Wide-
spread oxidation and pedogenic elements, such as mot-
tles, glaebules and root traces (Davis & Gibling, 2003) 
would testify more drained conditions compared to the 
underlaying FTR D.  
 

Epiclastite (FTR G) 
This is a crudely stratified heterometric deposit with 

coarse-tail normal grading, composed of coarse sand 
and very fine poorly rounded pebbles (Fig. 6c; Plate III 
a) in a silty matrix with a dark yellow to brown hue. Clast 
composition comprises abundant pyroclastic material 
with ferro-magnesian juvenile crystals and a range of 
juvenile to accidental lapilli, including fragmented clasts 
of violaceous-reddish un-welded ash (pozzolan), chert 
and carbonate. FTR G intercalates to FTR F facies (Figs 
8 and 9) forming an up to 4.5 m thick body with a sharp, 
but not erosive base and a pedogenically modified top, 
which contains root traces, mottles and terrestrial gas-
tropods (Vallonia sp.). 
Interpretation. The features of FTR G, along with its 

 
 
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185 

 
 
Stratigraphy of the Palatine Hill 

Examples of lithofacies from selected cores (bottoms and tops in the lower left and upper right, respectively; core box is 1 m-long), with 
main facies boundaries marked in red. a) The Palatino Unit (PTI) ignimbrite interbedded to the fluvial channel gravels of the Valle Giulia 
Formation (VGU A) from borehole 11 MS (depth interval 25-20 m). b) Very fine-to-fine limestone well-rounded pebbles embedded within 
the lowermost part of the Palatino Unit (PTI) and the overlaying ripple-drift laminated levee sand (VGU B) of the Valle Giulia Formation from 
borehole 13 MS (depth interval 13-15 m). These pebbles occur mostly in off-valley axis settings and are interpreted to reflect entrainment of 
fluvial deposits by the PTI pyroclastic flow from the substrate. c) Green-grey, faintly laminated pyroclastic deposit of the Prima Porta Unit 
(PPT; Middle Pleistocene), overlaying the dark-grey PTI ignimbrite in borehole 16 MS (depth interval 20-15 m). Fosso del Torrino Forma-
tion (Middle Pleistocene): d) channel gravel (FTR A) with heterometric pebbles in an abundant sandy matrix overlain by cross-laminated 
fluvial sand of FTR B lithofacies from borehole 22 P (depth 35-30 m); e) pale grey, structureless, silty clay with sparse carbonate nodule 
(red arrow) interpretable as poorly drained floodplain deposit (FTR D) from borehole 22 P (depth interval 25-20 m); f) blue-grey, structure-
less, organic-rich clay with a lignite seam on the top interpretable as the deposit of poorly drained flooplain (FTR D) followed upward by 
yellowish clayey deposits of a well-drained floodplain (FTR F) in borehole 9 MS (depth interval 30-25 m). 

Plate II 



   

 

association with FTR F, suggest deposition by massive, 
hyper-concentrated and out-of-channel flows (North & 
Davidson, 2012) in floodplain environment. The clast 
composition, dominated by volcanic particles, suggests 
a syn- to slightly post-eruptive epiclastic origin, as well 
as en-route entrainment of fluvial pebbles from the sub-
strate. 
 
4.5 Quartaccio Synthem (QTA) 

The Quartaccio Synthem (Funiciello & Giordano, 
2008) is correlated with MIS 10-9 and the PG6 deposi-
tional sequence (Milli, 1997). In the study area it corre-
sponds to the pyroclastic Villa Senni Formation - Tufo 
Lionato ignimbrite (VSN1) and to the overlaying fluvial 
Aurelia Formation (AEL). The Quartaccio Synthem is 
bounded at the base by the IV Unconformity, recording 
the sea level fall occurred between MIS 11 and MIS 10. 
This surface, corresponding to the base of the Villa 
Senni Formation - Tufo Lionato ignimbrite (VSN1), is flat 
on top of the Palatine Hill and deeply incised in the 
nearby Capitoline Hill. 

 
4.5.1 Villa Senni Formation, Tufo Lionato (VSN1) 

The Tufo Lionato is an ignimbrite sourced from the 
Alban Hills (De Rita et al., 1995; Watkins et al., 2002; 
Giordano et al., 2006; Giordano and the CARG team, 
2010) which belongs to the Villa Senni Formation and 
was 40Ar/39Ar dated to 355 ± 2 ka using samples from 
the Palatine outcrops (Karner & Renne, 1998; Karner et 
al., 2001). Well-exposed along the Velabro Valley (Figs. 
6 a, c), VSN1 is a dark red-orange, massive tuff (Figs. 7
-9; Plate III c;) with an ash matrix and sparse crystals 
(leucite, biotite, clino-pyroxene), lithics (small and rare 
limestone clasts), and grey to black scoriae, and locally 
with columnar gas escape pipes up to 40-50 cm long 
and a few centimeters wide (Fig. 6 f). The deposit may 
be either welded (VSN 1a) as a result of cementation by 
zeolite minerals or un-welded (VSN 1b), consisting of 
scoriaceous reddish to dark grey pozzolan (Plate III d). 
Locally, an up to 50 cm thick bed of lapilli occurs below 
the tuff suggesting that the ignimbrite was preceded by 
the fall-out of lapilli (Plate III c; logs 14 MS, 9 MS and 3 
A, in Figs. 8 and 9). Tabular with flat base and mean 
thickness of c. 10 m on the Palatine Hill top and the 
orographic left of the Velabro Valley, the VSN1 rapidly 
thickens to up to 45 m in the subsurface of the Capito-
line Hill (Alvarez et al., 1996; Corazza et al., 2004) sug-
gesting it partially fills a NE-SW trending incised valley 
(see also cross section 1 on Fig. 4; Fig. 7). 
Interpretation. Deposition of a large volume, very hot 
and dense pyroclastic flow, infilling the pre-existing to-
pography. Large-scale geometry suggests the presence 
of a fluvial paleovalley, located NW of the Capitoline Hill, 
related to the Quartaccio Synthem (Fig. 10) and flanked 
by to the southeast by an interfluve (the present-day 
Palatine Hill) superelevated by at least 20 m above the 
valley floor. 
 
4.5.2 Aurelia Formation (AEL) 

In the study area this unit (cfr. with the Formazione 
Fluvio-Lacustre of De Angelis D’Ossat, 1956) crops out 
limitedly to the Palatino and Capitolino hilltop and is 
represented by a few metres of pale yellow clayey silt 

with a range of pedogenic features. These include mot-
tles, orange-red Fe3+ oxides cutans, sparse sub-
spheroidal carbonate nodules, root traces and CaCO3-
depleted horizons (Plate III d). 
Interpretation. AEL sediments exposed on the Palatine 
hilltop might represent floodplain mud-prone deposits 
which have undergone intense pedogenization and illu-
vial clay enrichment under highly oxidizing conditions. 
 
4.6 Fiume Tevere Synthem (SFT) 

The post-volcanic Fiume Tevere Synthem 
(Funiciello & Giordano, 2008) is correlated with MIS 5d-
1 and the PG9 depositional sequence (Milli, 1997; Tiber 
Depositional Sequence of Milli et al., 2016). It comprises 
only the Alluvial deposits (SFTba) sensu Funiciello & 
Giordano (2008), and is bounded at the base by the 
deeply incised V Unconformity, recording the last glacio-
eustatic sea level fall (MIS 5d- MIS 2).  

In the study area, the Alluvial deposits (SFTba) 
mainly consists of poorly consolidated fine-grained sedi-
ments forming the Upper Pleistocene-Holocene (MIS 2-
1) infill of the left-bank tributary valleys of the Tiber 
River, namely the Velabro, Murcia and Labicano valleys 
(Bozzano et al., 1995; Ammerman et al., 2000; Cam-
polunghi et al., 2007; Carpentieri et al., 2015; Marra et 
al., 2018). 

 
Gravel lag (SFTba A) 

This facies is represented by sub-angular to well-
rounded very fine to medium pebbles (Plate III e) of 
limestone, chert and tuff in an abundant dark grey silty 
sandy matrix rich in ferro-magnesian minerals and plant 
fragments. 
Interpretation. SFTba A forms a coarse basal lag up to  
about 5 m thick infilling the lower part of the Tiber tribu-
tary paleovalleys. It represents an early-stage deposit 
resulting from local erosion and deposition of older grav-
elly-sandy deposits (e.g. CIL A-B, VGU A-B and FTR A-
B) cut by Unconformity V. 
 

Channel sand (SFTba B) 
This facies is comprised of grey to brown, fine-

medium silty sands, with quartz, feldspar, muscovite, 
ferro-magnesian minerals of volcanic origin and scat-
tered peat fragments. SFTba B forms lens-shaped bod-
ies up to 8-10 m thick and less than 100 m wide, which 
pass laterally to mud-prone deposits of facies SFTba D-
F (see below). 
Interpretation. SFTba B can be interpreted as a chan-
nel-fill deposit of streams with a sandy bed-load. 
 

Organic-rich mud (SFTba D) 
This facies represents most of the infill of SFT pa-

leovalleys reaching thickness up to 35 m (e.g. Murcia 
Valley, Fig. 4). It is composed of dark grey, structureless 
silty clay (Plate III f), typically plastic and poorly consoli-
dated, interbedded with cm-thick beds of sand composi-
tionally similar to SFTba B. The dark grey hue is im-
parted by the abundance of plant fragments, which in 
some cases can be concentrated to form dm-thick peat 
layers. 
Interpretation. SFTba D reflects fall-out and, subordi-
nately, traction-fall deposition by fluvial overbanking in 
an undrained floodplain environment with ponds and 

 
 
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187 

 
 
Stratigraphy of the Palatine Hill 

Examples of lithofacies from selected cores (bottoms and tops in the lower left and upper right, respectively; core box is 1 m-long), with 
main facies boundaries marked in red. a) The Fosso del Torrino Formation (Middle Pleistocene): pale yellow, faintly laminated sandy silt 
(FTR F) interpreted as a well-drained floodplain deposit, interbedded with grey-brown, reworked coarse pyroclastic sand (FTR G) (borehole 
9 MS, depth interval 20-15 m). b) Detail of a tephra layer from FTR F (borehole 3 A; depth 16.40 m). c) Villa Senni Formation - Tufo Lionato 
(Middle Pleistocene): orange-red massive ignimbrite (VSN 1a) with a 40 cm thick basal fallout deposit, composed of dark grey lapilli and 
coarse ashes. VSN 1a covers overbank silt (FTR F) of the Fosso Torrino Formation (borehole 9 MS; depth interval 15-10 m); d) Villa Senni 
Formation - Tufo Lionato: reddish pozolan (VSN 1b) overlaying FTR F. VSN 1b is in turn overlain by yellowish, intensely pedogenized clay 
of the Aurelia Formation (AEL; Middle Pleistocene) and by anthropogenic landfill material (h) (borehole 2 A; dept interval 15-10 m). e) 
Fiume Tevere Synthem - Alluvial deposits (Late Pleistocene-Holocene): dark brown-grey, sandy rich, very fine to fine pebbles of SFTba A 
overlaying the sand of the Fosso del Torrino Formation (FTR B) in borehole 18 P (depth interval 25-20 m); f) Fiume Tevere Synthem - 
Alluvial deposits: grey, organic-rich, poorly drained floodplain mud (SFTba D lithofacies), overlain by pale brown, pedogenized sandy silt 
(SFTba F) in borehole 18 P (depth interval 20-15 m). 

 

Plate III 



   

 

marshes. 
 

Pedogenically modified mud (SFTba F) 
This facies can be differentiated by SFTba D 

based on its stiffness, its reddish to dark brown-hue and 
mottled texture reflecting oxidization of abundant plant 
fragments (Plate III f). At some sites, scattered fine-
pebble sized clasts of limestone and brick fragments are 
found embedded within the topmost part of SFTba F, 
witnessing man-made excavation and dumping of land-
fill materials, likely from Roman times.  
Interpretation. SFTba F is widespread within SFT pale-
ovalleys, forming a laterally continuous body up to 7 m 
thick overlaying SFTba D. It can be interpreted to reflect 
overbank deposition in a drained floodplain environment 
subject to intense root mottling and pedogenization. 
 
4.7 Anthropogenic cover (h) 

This unit is represented by an almost continuous 
layer of backfill material (lithofacies hb), and remnants 
of buildings (lithofacies hm) from the Roman age, reach-
ing maximum thickness of 15-20 m. The backfill (hb) is 
constituted by sand-pebble sized clasts in a silty-clayey 
matrix of pozzolanic composition, while masonry (hm) is 
mainly composed by hard concrete and rocky blocks 
(travertine, lava rocks, marble, etc.). The anthropogenic 
layer mantles the pre-existing morphology and reaches 
its maximum thickness in correspondence of buried 
valleys (Moscatelli et al., 2014b). 

  
5. DISCUSSION  
 

Owing to the availability of numerous subsoil in-
vestigations carried out over the last few decades 
mostly for archeological, geotechnical and cultural heri-
tage preservation purposes (De Angelis D’Ossat, 1956; 
Alvarez et al., 1996; Corazza et al., 2004; Cecchi, 2011; 
Moscatelli et al., 2012; Calabresi et al., 2013; Mancini et 
al., 2014), the Palatine Hill represents a key site for 
unfolding the stratigraphic architecture of the volcano-
sedimentary succession of the Rome Basin (Conato et 
al., 1980; Milli, 1997; Karner & Marra, 1998; Marra et al., 
1998, 2008, 2016; Giordano et al., 2003; Milli et al., 
2008; Marra & Florindo, 2014; Luberti et al., 2017, 
among the others). Based on a few classical and well-
studied outcrops (Figs. 5 and 6 a, b; see also Marra & 
Rosa, 1995; Corazza et al., 2004; De Rita et al., 2002; 
De Rita & Fabbri, 2009), temporary outcrops from ar-
cheological excavation and construction sites (Figs. 6 c-
e) and selected boreholes recently drilled in the study 
area (Figs. 7-9), this contribution is aimed at describing 
the sedimentary facies making up the infills of multiple 
incised paleovalleys (sensu Blum et al., 2013) of the 
Tiber River, developed in response to the Middle Pleis-
tocene to Holocene high-frequency sea level fluctua-
tions affecting the Rome Basin. The following discussion 
aims to: 1) show the significance of the Palatine Hill 
case study as a depositional analogue for paleovalley 
development, and 2) comment best practices in geology 
of urban areas. 

 
 

5.1 The Palatine Hill as an analogue for paleovalley 
development 

The paleovalley infills preserved in the subsurface 
of the Palatine Hill and surrounding areas correspond to 
some of the synthems introduced by Funicello & 
Giordano (2008), namely, from older to younger the 
Flaminia (LMN), Villa Glori (VGL), Torrino (TNO), Quart-
accio (QTA) and Fiume Tevere (SFT) Synthems. 

In the study area, the Flaminia Synthem (LMN; MIS 
16-15) is characterized by a rather flat basal unconform-
ity (Unconformity I), tabular geometry and a fining-
upward infill represented by the fluvial Santa Cecilia 
Formation, made of channel gravel (CIL A) and sand 
(CIL B) and deposited by a braided river with a coarse 
bed load. Along with the underlying marine sediment of 
the Monte Vaticano Formation (MVA), the Flaminia Syn-
them represents the substrate into which younger pale-
ovalleys developed. Basing on its almost tabular geome-
try and stacking of facies, the Santa Cecilia Formation 
(CIL) can be interpreted as a “stacked channel sheet 
with smooth or near-smooth basal unconformity”, follow-
ing the valley architectures classification by Holbrook 
(2001). To the east of the study area, however, the CIL 
thickness increases rapidly and its top deepens, sug-
gesting syn- to post- depositional extensional tectonics 
controlling locally the basin infill (Funicello & Giordano, 
2008). 

The Villa Glori (VGL) and Torrino (TNO) Synthems 
are by far the best-preserved paleovalley infills docu-
mented in the Palatine Hill subsurface. These show a 
NW-SE to N-S trend (Fig. 10), high-relief basal uncon-
formities (Unconformities II and III) and a common facies 
motif with a lower gravelly facies grading upward into a 
suite of channelized sands, channel abandonment fines 
and floodplain muds. This facies architecture that indi-
cates valley incision was followed by the establishment 
of an entrenched gravelly braided fluvial system, evolv-
ing upward into a mixed, sandy-muddy suspended-load 
and bed-load river (i.e. channel-levee sands and silt) 
with laterally continuous and well-developed floodplains 
(i.e. mud-prone facies). 

Notably, tough partly cannibalized by the younger 
TNO, VGL (MIS 14-13) represents a particularly valu-
able example for constraining the likely morphology of 
the studied paleovalleys, in that its fluvial infill (the Valle 
Giulia Fm. VGU) is intercalated by ignimbrites from large 
volume catastrophic pyroclastic flows (the Palatino and 
Prima Porta Units, PTI and PPT) capable of blanking the 
topography and providing a snapshot of relative location 
of coeval depositional elements. In fact, for example, the 
PTI ignimbrite covered both the active channel and 
levee-floodplain belt (logs MS 13 and MS 11, in Fig. 7), 
and was later incised by the re-established active fluvial 
channel, represented by facies VGU A above PTI (Fig. 
7). 

A full record of paleovalley morphology and infill 
development is provided by TNO (MIS 12-11). The ex-
cellent preservation of the dominantly fluvial Fosso del 
Torrino Fm. (FTR) allows confidently tracking: 1) the 
stratigraphic replacement of a lower gravel-prone early 
stage-fill (FTR A) by a sandy multi-storey channel belt fill 
(i.e. the main depositional body of facies FTR B) along 
the paleovalley axis (Fig. 10); 2) the evolving relation-

 
 
188 

 
 

Mancini M. et al. 



   

 

ship between the active channel belt and coeval flood-
plains. 

Regarding the latter aspect, it can be noted how, 
over most of the paleovalley infill thickness, floodplain 
muds are intercalated with hydromorphic paleosols sug-
gesting waterlogged conditions (FTR D), whereas in the 
uppermost FTR they contain oxidized paleosols (FTR 
F). This stratigraphic and pedogenetic change from 
poorly- to well-drained floodplains may be interpreted as 
a progressive lowering of the groundwater table, which 
can be explained by incipient channel re-incision of 
floodplain under a general decrease of rate of floodplain 
accommodation (Wright & Marriot, 1993; Miall, 2014). 

Moreover, in the uppermost FTR the widespread 
presence of out-of-channel epiclastites (FTR G) and 
tephra testifies active syn-volcanic alluvial sedimenta-
tion. The tephra horizons preserved within the upper 
floodplain deposits (Plate III b; Fig. 9) might correlate to 
the tephra reported by Marra et al. (2016) as part of the 
San Paolo Fm. (i.e. Fosso del Torrino Fm.) from the 

subsurface of the nearby Capitoline Hill. A sanidine 
sample (SPQR-51sample) from the Capitoline tephra 
was 40Ar/39Ar dated 416 ± 11 ka (Karner & Renne, 1998; 
Karner et al., 2001) suggesting a correlation with the 
Vico α horizon sourced from the Vico Volcanic District of 
northern Latium (Luberti et al., 2017) and thus providing 
important constrain on timing of development of the FTR 
paleovalley infill. 

The study area provides only a partial view of the 
Quartaccio Synthem (QTA, MIS 10-9; Fig. 10). Nonethe-
less, the geometry and facies character of the pyroclas-
tic Villa Senni Formation-Tufo Lionato (VSN1) and the 
Aurelia Formation (AEL) agree with a river system, and 
the corresponding paleovalley, located to the NW of the 
Capitoline Hill (Alvarez et al., 1996; Corazza et al., 
2004), which delivered fines to a left-bank floodplain (i.e. 
AEL) occupying the Palatine Hill area. If the likely loca-
tion of the paleovalleys documented in the subsurface of 
the Palatine Hill and surrounding areas is compared 
(Fig. 10), a progressive westward shift of the river sys-

 
 

189 

Fig. 10 - Paleogeographic sketch map of the Palatine area showing axes and margins of the main buried paleovalleys (modified and 
adapted after Alvarez et al., 1996, and Mancini et al., 2014). 

 
 
Stratigraphy of the Palatine Hill 



   

 

tem is apparent starting from TNO to QTA which may 
reflect the interplay of the long-term regional tectonic 
uplift of the western periphery of the Central Apennines 
(Milli, 1997; Giordano et al., 2003; Marra et al., 2008; 
Milli et al., 2008; Mancini et al., 2013) and the input of 
volcanic products from the Alban Hills in subtracting 
accommodation space to the Tiber River fluvial system. 

One last observation can be made about the sig-
nificance of the Fiume Tevere Synthem (SFT; MIS 5d-1) 
present in the study area, representing the infills of the 
left-bank Velabro and Murcia tributary paleovalleys of 
the Tiber River. Compared to previously addressed 
examples, which refer to the ancient main trunk pale-
ovalleys (VGL, TNO, QTA), the Velabro and Murcia 
paleovalley infills are initiated by coarse and poorly or-
ganized lags deposited by gravitative processes (facies 
SFTba A), contain a much greater proportion of pedoge-
nized, organic-rich fines (SFTba D-F) and appear to be 
deficient of channel sand (SFTba B). This contrasting 
architecture of tributary vs. trunk paleovalley of the 
Tiber, much richer in channel-belt deposits (see also 
Milli et al., 2016), can be interpreted to reflect the fact 
that the higher rate of aggradation of the Tiber River 
valley with respect to surrounding areas might have 
resulted in “passive” backfilling of lateral valleys. 

 
5.2 Methodological remarks on urban geosciences 

Finally two aspects concerning the best practice on 
urban geosciences can be considered, which derive 
from the present research: 1) the extensive use of pho-
tographic illustration for core facies analysis; 2) the 
documentation of temporary outcrops. 

On the first aspect, the photographic depiction of 
cores is well recommended for describing facies of Qua-
ternary units within fluvial and urban contexts (Amorosi 
2006; Sarti et al., 2012), and can significantly contribute 
to solve potential gaps of knowledge on local stratigra-
phy. However, within the rich scientific literature on the 
Rome Basin stratigraphy (Luberti et al., 2017, with refer-
ences) only few examples do exist of core data reported 
through photographic pictures (Marra & Florindo, 2014; 
Martino et al., 2015; Milli et al., 2016). In our opinion, the 
core data here illustrated (Plates I-III) can be potentially 
used as useful reference and comparison material for 
subsoil reconstructions of nearby areas. 

The occurrence of temporary shortly-exposed out-
crops, related to in-progress city works such as subway 
construction and archeological excavations, is well 
documented in this article (Figs. 6 c-e). Their observa-
tion, description and correlation with other field and sub-
soil data should be emphasized. In fact, the integration 
of temporary outcrops with other data can be useful for 
anchoring unsolved stratigraphic reconstructions in 
densely urbanized contexts, where the widespread 
presence of pervious surfaces usually impedes the ob-
servation of natural outcrops, and where available cores 
may be insufficient, in some cases, to provide a com-
plete picture of the subsoil. This is particularly true in the 
ancient historical center of Rome, where the anthropo-
genic modifications and a thick layer of anthropic backfill 
(Moscatelli et al., 2014 b; Ciotoli et al., 2015) often pre-
vents detailed palaeo-environmental reconstructions 
based only on the terrain morphology observation. 

6. CONCLUSION 
 

The facies analysis of core and outcrop data has 
allowed to reconstruct with great detail the stratigraphic 
architecture of the Palatine Hill. This architecture is rep-
resented by a series of nested paleovalley infills related 
to the Tiber River system and encompassing Middle 
Pleistocene to Holocene intervals (MIS 16-9 and MIS 2-
1 intervals) of fluvial sedimentation and distal pyroclastic 
deposition. The paleogeography of the most relevant 
paleo-valleys, as reconstructed from the present study, 
can be related to external forcing as uplift, pyroclastic 
supply and fluvial response to glacio-eustatic changes, 
as well as to internal reorganization of the fluvial system, 
which deserve to be investigated on a wider area. Nev-
ertheless, thanks to its well detailed stratigraphic recon-
struction the Palatine can be considered a key area for 
better understanding trends, characters and continuity of 
fluvial paleo-valleys within the whole Rome Basin. 

 
ACKNOWLEGEMENTS 

The authors thank the reviewers and editors for 
useful comments and suggestions. 

 
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Ms. received: Marz 28, 2018 
Final text received: October 25, 2018