OJS 730 Monegato et al 127-148.pub


   

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

Alpine and Mediterranean Quaternary, 36 (2), 2023, 127-148 

THE EARLY AND MIDDLE PLEISTOCENE GLACIATIONS IN THE ALPS 
 

Giovanni Monegato 1, Franco Gianotti 2, Susan Ivy-Ochs 3, Jürgen M. Reitner 4, 
Giancarlo Scardia 1, 5, Naki Akçar 6 

 
1 Institute of Geosciences and Earth Resources, National Research Council, Padova, Italy. 

2 Dipartimento di Scienze della Terra, Università di Torino, Torino, Italy. 
3 Laboratory of Ion Beam Physics, ETH Zurich, Zurich, Swiss. 

4 GeoSphere Austria, Department Geologische Kartierung / Geological Mapping, Vienna, Austria. 
5 Universidade Estadual Paulista (UNESP), Instituto de Geociências e Ciências Exatas, Rio Claro SP, Brazil. 

6 Institut für Geologie, Universität Bern, Bern, Swiss. 
 

Corresponding author: Giovanni Monegato <giovanni.monegato@igg.cnr.it>  
 
ABSTRACT: The Alps experienced extensive glaciations during many Pleistocene cold stages. New stratigraphic and geochrono-
logical data gathered in the last decade depict the Early Pleistocene glaciations and their record is continuously updated. The 
onset of major glaciations since the late Matuyama Chron (MIS 22-20) is better recognized in many end moraine systems along 
the southern side of the Alps. The updated chronology of the Middle Pleistocene phases indicates an improvement of the 
knowledge about the penultimate glaciation (MIS 6) and the evidence that every sector has had its own most extensive glaciation 
in a different time span. The dissimilar architecture of the end moraine systems suggests a different behavior of the glaciers from 
one cold stage to the others. The development of the largest glacier networks with associated piedmont lobes (i.e., Adige, Adda 
and likely Inn) required abundant snow supply promoted by the southerly circulation, like in the LGM. For the systems with the 
highest accumulation areas (i.e., Valais, Dora Baltea, Rhine-Reuss and Ticino-Toce) a larger number of glacial units was recorded 
likely because these were more sensitive to every circulation regime impacting the Alps, whether northwest or south dominated. 
The Alps remain the most studied mountain range with respect to Quaternary glaciations, thereby providing a unique and valuable 
resource. 
 
 
Keywords: Quaternary glaciations, european Alps, Early-Middle Pleistocene, palaeomagnetism, glacigenic deposits. 
 

1. INTRODUCTION 
 
The European Alps (Fig. 1) have been the key site 

for the development of the idea of multiple Quaternary 
glaciations since the milestone work of Penck & Brück-
ner (1901-1909). The study of the glacial history of the 
Alps began earlier, in the XIX century (e.g., Agassiz, 
1840; Morlot, 1854; Omboni, 1861; de Mortillet, 1861; 
Gastaldi, 1865; Taramelli, 1875; Sacco, 1887; Mühl-
berg, 1896; Wannier, 2023), and since that time this 
mountain range has represented a major field laboratory 
for new theories and methodological advances in glacial 
stratigraphy and geochronology. The Alpine terminal 
moraine systems, also known as morainic amphithea-
ters, occur at the outlet of the major Alpine valleys and 
are primary sites for the study of Quaternary glaciations 
(Penck et al., 1894) and developing one of the major 
knowledge advance in Quaternary studies (Orombelli et 
al., 2023). Their morphostratigraphic architecture was 
studied by Penck & Brückner (1901-1909), who defined 
four climatostratigraphic units and correlated them 
across the Alps. Accordingly, this study gave birth to a 
new paradigm in ice age history of the Earth: four Alpine 
glaciations (from older to younger: Günz, Mindel, Riss, 
and Würm) and the intervening “interglacials”. Their 

definition based on glacial sequences consisting of ter-
minal moraines and proglacial outwash terraces stands 
as a milestone in geoscientific research, not only for the 
Alps but also for elsewhere in Eurasia (e.g., Krūkle & 
Stelle, 1964; Grosswald et al., 1994; Lehmkuhl et al., 
2011) and worldwide (Cotton, 1963). For a long time, 
definition and correlation of the glacial and glaciofluvial 
deposits were mostly made by combining the weather-
ing degree and geomorphological evidence (e.g. the 
altitudinal concordance of the distribution of glaciofluvial 
terraces), where topographic elevation is a key for a 
relative stratigraphic framework (e.g., Bini, 1997). 

Subsequent stratigraphic studies, since the 1970s, 
focused on facies analysis and bounding surfaces, lead-
ing to the identification of important discontinuities 
(including buried soils and interglacial/interstadial peat 
layers), casting new light on the age of old glaciations 
and questioning the reliability of the four glaciations par-
adigm (Bowen, 1978; Billard & Orombelli, 1986; 
Schlüchter, 1981; 1986). Based on marine and ice 
cores, the development of the Marine Isotope Stage 
(MIS) stratigraphy documented up to fifty cold stages 
(Shackleton & Pisias, 1985; Lisieki & Raymo, 2005) 
during the Pleistocene (sensu Gibbard et al., 2010) rais-
ing the question if and how the four-glaciation model 

 

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could have been applicable (e.g., Billard & Derbyshire, 
1985; Šibrava et al., 1986; Billard & Orombelli, 1986; 
Schlüchter, 1988). With this change of perspective, in 
the Alps, a minimum of 15 different glacier advances 
were then recognized in the Swiss Foreland (Preusser 
et al., 2011; Schlüchter et al., 2020), and about 11 in the 
central southern foreland sectors (Bini et al., 2014; 
Gianotti et al., 2015). Among these, 13 and 7 respec-
tively, are ascribable to the Early and Middle Pleisto-
cene (Schlüchter et al., 2020; Ivy-Ochs et al., 2022). 
Considering the lack of chronostratigraphic information 
for many Early-Middle Pleistocene glacial units (Hughes 
et al., 2020) and their geographical distribution we can 
pose several questions, such as: how many glacier ad-
vances could have been recorded in the circum-Alpine 
area? Which were the major ones (i.e. foreland reach-
ing)? Did Alpine glaciers have comparable extents in 
each cold phase?  

The Alps were also the playground for testing new 
geochronological tools during the last three decades, 
leading to several attempts to place the glacier advanc-
es within the framework of marine isotope stages, also 
considering the ongoing uplift of the Alps (Champagnac 
et al., 2007; Scardia et al., 2006; 2012; Sternai et al, 
2019). Moreover, the remarkable regional dissimilarities 
in term of number of glacier advances from one sector 
to another (Ivy-Ochs et al., 2022), reflect the differences 
in the morphological and sedimentary archives, due to 
variations in tectonic regimes (uplift vs. subsidence), 
accommodation space, and preservation potential. Such 
conditions have an impact on the choice of suitable 
stratigraphic approach (litho-, morpho-, allostratigraphy) 
and in most cases also on the terminology of glaciations 
(chronostratigraphy, climatostratigraphy). This demands 
the development of new approaches in order to disen-
tangle the stratigraphic puzzle, and its meaning in terms 
of paleoclimate vs. tectonic evolution of the Alps. Apart 
from the Late Pleistocene advances, encompassing the 
Würm (Chaline & Jerz, 1984; Monegato & Ravazzi, 

2018), the Early and Middle Pleistocene glacial units still 
need further investigation. The present review is aimed 
at describing the architecture of Early to Middle Pleisto-
cene glacial units across the Alps and discussing the 
major questions related to their distribution.  

 
2. BACKGROUND STUDIES 

 
As the cradle of the Quaternary glaciation concept, 

the Alps have a long-lasting history of studies concern-
ing when and how mountain glaciers became a vast ice 
field during the Pleistocene. The moraine amphitheaters 
in the piedmont area at the outlet of the major Alpine 
valleys have been the site for countless studies since 
the early researches and also today represent key areas 
for reconstructing Alpine glaciations. Starting from the 
pioneering works by Venetz (1833), Agassiz (1840) and 
de Charpentier (1841), in which the idea of glaciers 
reaching the lowlands was developed, a large number of 
scholars examined in depth the glacial landforms and 
deposits all around the Alps. At the beginning, a single 
cold phase was assumed for the deposition of the mo-
raines (e.g., Venetz, 1833; Martins & Gastaldi, 1850; 
Bruno, 1877) on the basis of lithostratigraphical descrip-
tion, including the outwash deposits. However, very 
soon evidence for multiple glaciations was reported from 
the Lake Geneva area (Morlot, 1854), the Swiss Alpine 
forelands (Mühlberg, 1896), the Northern foreland (e.g., 
Penck, 1882; Blaas, 1884; Penck et al., 1894) (Fig. 2A), 
and the southern Alpine foreland (Nicolis, 1899; Ca-
peder, 1904). With their milestone work, Penck & Brück-
ner (1901-1909) described different suites of gravel ac-
cumulation that were connected upstream to moraines 
(Fig. 2C), recognizing four glaciations all across the 
circum-Alpine area (Fig. 2B). The four fold glaciation 
paradigm was, after its publication, quickly accepted and 
applied in regional studies and maps. Some authors 
added more “glaciations” to the list according to older 
gravel accumulation suites (Eberl, 1930; Schaefer, 

 
 

128 

Fig. 1 - Reference areas for the Alpine Pre-LGM glaciation in the European Alps. Main glacier catchments numbered as in Tab. 1.  

 
 

Monegato G. et al. 



   

 

In the northern foreland, the gravel units at Stadler-
berg and Irchel (Fig. 3B) in northern Switzerland repre-
sent the early phase of the Deckenschotter accumula-
tion at 2.6 ±0.1 Ma (Claude et al., 2017; 2019; Dieleman 
et al., 2022). This is in agreement with the occurrence of 
Mimomys cf. pliocaenicus (Irchel site, Bolliger et al., 
1996) which belongs to the Gelasian/Tiglian MN17 unit 
of the European Land Mammals Zones. These gravels 
are interpreted as glaciofluvial units, thus as evidence of 
an early extensive glaciation that occurred already by 
2.6 Ma in the northern side the Alps. Actually the Deck-
enschotter sequence at Irchel is made of a number of 
different units, whose ages suggest a cut and fill evolu-
tion of the northern foreland during the Early Pleisto-
cene (Dieleman et al., 2022). In the Swiss foreland an 
overall eight glaciations are suggested for the Early 
Pleistocene by Schlüchter et al. (2020), which should 
include the late Matuyama. The Deckenschotter is inter-
preted as the glaciofluvial sediments related to this time 
span also in the German sector of the Alpine foreland 
(Älteste Deckenschotter in German stratigraphy); there 
Deckenschotter is attributed to be the outwash deposi-
tion of Biber and Donau glaciations (Ellwanger et al., 
2011; Doppler et al., 2011), notwithstanding some disa-
greements (see Fiebig et al., 2011). The first dating 
attempt of Deckenschotter in the German sector provi-
ded the age of 2.35+1.08

-0.88 Ma (Häuselmann et al., 
2007) that could be considered quite comparable to the 
Deckenschotter chronology at Irchel despite the large 
analytic uncertainty.  

In the western sector, evidence of cold stages is 
testified only by loess deposition along the Rhone Val-
ley, south of Lyon (Bourdier, 1963) and biostratigra-
phically ascribed to 2.2 Ma (Guerin, 1980; Billard & 
Orombelli, 1986).  

Around the Plio-Pleistocene boundary, the south-
ern side of the Alps was characterized by transitional 
and marine deposits (“Villafranchian”; Carraro et al., 
1996; ), overlain by conglomerate (Ceppo) in the Lom-
bardy sector (e.g., Nangeroni, 1940; Venzo, 1950; 
Orombelli, 1979; Zuccoli, 2000; Bini et al., 2004a). The 
former belongs to the Gelasian in the Adda sector 
based on palaevegetation (Venzo, 1950; Corselli et al., 
1985; Pini et al., 2002) and in the Verbano sector (Bini 
et al., 1997). The first glacier advance is testified by 
Immacolata and Vivirolo formations in the Verbano sec-
tor and tentatively ascribed by magnetostratigraphy 
(Uggeri et al., 1997) to the Gauss-Matuyama geoma-
gnetic reversal (2.58 Ma; Gradstein et al., 2020). Actual-
ly, the magnetostratigraphy presented by Uggeri et al. 
(1997) can be equally correlated to the Jaramillo - late 
Matuyama (C1r.1n-C1r.1r) reversal (0.99 Ma, see next 
section), and the associated glacigenic deposits could 
be ascribed to a late Matuyama glaciation. Lacking inde-
pendent chronologic constraints, the age of the earliest 
glacigenic deposits in the Verbano sector remains an 
open issue. Conglomerate successions that mark the 
increase of sediment production and delivery are pre-
sent in the Prealpine valleys from the Orobic to the 
Julian Alps and Prealps, some of them were ascribed to 
the Early Pleistocene by means of palaeobotanic con-
tent and stratigraphic relationships (Monegato & Stefani, 
2011; Martinetto et al., 2012; Bini et al., 2015; Monegato 

1956; Schreiner & Ebel, 1981; Glückert, 1974; Doppler 
et al., 2011) or split the four glaciations into subunits 
(e.g., Venzo, 1965, 1977; Carraro et al., 1970). This fact 
created some ambiguities in correlating glacial/
glaciofluvial units from one site to another, even if con-
tiguous. The new field surveys, based on the allostrati-
graphic approach, revealed these differences by the 
difficulty of tracing lateral boundaries (e.g., Bini et al., 
2004a, 2004b, 2015), which led to a splitting of the re-
gional Alpine stratigraphy into local, independent strati-
graphic frameworks over the Swiss and Italian sectors 
(e.g., Preusser et al., 2011; Graf & Burkhalter, 2016; 
Fioraso et al., 2021; Ivy-Ochs et al., 2022, and refer-
ences therein). On the other hand, in the German-
Austrian area, the Penck & Brückner (1901-1909) subdi-
vision has been maintained because of the physical 
correlation of glaciofluvial terraces in the piedmont area 
and along the further catchment of the Danube River 
(Ellwanger et al., 2011; Doppler et al., 2011; Van Husen 
& Reitner, 2011a; Ivy-Ochs et al., 2022; Reitner, 2022).  

Within the general architecture of the moraine 
suites in the circum-Alpine area thick sequences of con-
glomerates were also included, known as Deckenschot-
ter (Cover Gravels in German) on the northern side of 
the Alps (Du Pasquier, 1891; Frei, 1912; Graf, 1993). In 
the southern side, coarse-grained gravel deposits, 
known as Ceppo, were partially ascribed to glaciofluvial 
sedimentation based on petrographic composition (e.g., 
Venzo, 1950; 1957).  

The systematic and multidisciplinary study of sev-
eral cores in the southern Alpine foreland yielded during 
the last two decades a more comprehensive framework 
for the onset of “major” glaciations and the mid-
Pleistocene revolution (Muttoni et al., 2003, 2007; Scar-
dia et al., 2006, 2010, 2012). Concurrently, the chronos-
tratigraphy of the Swiss Deckenschotter in the northern 
Alpine Foreland was progressively improved with em-
ployment of new dating techniques all based on cosmo-
genic nuclides. These include the depth profile, burial 
and isochron-burial dating techniques, with the latter as 
well applying the P-PINI age calculation model (Akçar et 
al., 2014, 2017; Claude et al., 2017, 2019; Knudsen et 
al., 2020; Dieleman et al., 2022). This new Deckenschot-
ter chronology outlines three major accumulation phases 
at ca. 2.5 Ma, ca. 1.5 Ma, and ca. 1 Ma (Fig. 3A-C). 

 
3. GLACIATIONS AT THE PLIO-PLEISTOCENE 
BOUNDARY  

 
The earliest evidence of Quaternary glaciation in 

the Northern Hemisphere is documented at the end of 
the Pliocene (ca. 2.7 Ma) by the first occurrence of ice-
rafted debris in North Atlantic oceanic sediments 
(Thierens et al., 2012; Bailey et al., 2013). Terrestrial 
evidence is related to the earliest major waxing of the 
Laurentide Ice Sheet (LIS) at ca. 2.4 Ma and correlated 
with MIS 100 (Balco & Rovey, 2010). Data about the 
Alpine ice fields for that period are scarce (Batchelor et 
al., 2019), although the Alps had already achieved an 
elevation high enough to host large glaciers (e.g., 
Pignalosa et al., 2011; Kuhlemann & Rahn, 2013; Win-
terberg & Willett, 2019; Krsnik et al., 2021; Dieleman et 
al., 2022). 

 
 

129 

 
 
The Early and Middle Pleistocene glaciations in the Alps  



   

 

& Poli, 2015). A burial age to 1.86 ±0.19 Ma was provid-
ed in the Sava valley on conglomerate complex as-
cribed to glaciofluvial environment (Mihevc et al., 2015). 

In the southern foreland, characterized by the transition 
to marine environments (Scardia et al., 2006; Garzanti 
et al., 2011), indications of cold phases triggering alluvial 

 
 

130 

 

Fig. 2 - A) Map of the Southern Bavaria by Penck (1882) in which the Author depicted multiple glacial advances in the Alps; B) Cross sec-
tions correlating glacial units of the end moraine systems with glaciofluvial terraces in the northern foreland depicted by Penck and Brück-
ner (1901-1909). C) Glacial sequence as defined by Penck & Brückner (1901-1909). 

 
 

Monegato G. et al. 



   

 

Deckenschotter (Upper Older Cover Gravels) at Zusam-
platte (Ausburg) recorded the B/M reversal (Doppler et 
al., 2011); the glaciofluvial deposits were ascribed to the 
Early Pleistocene also for the presence of Tiglian mam-
mal fauna (Königswald & Heinrich, 2007). The same 
attribution, because of reverse polarity, was given to the 

aggradation were detected in many sites 
through sediment core analysis (Ambrosetti 
et al., 1980; Ravazzi et al., 2005, 2009; Scar-
dia et al., 2006; 2010; Bini et al., 2015). The 
Ceppo units were ascribed to glaciofluvial 
deposition during the Early Pleistocene (Bini, 
1997). 

According to the available data, glaciers 
could have developed during this period in 
the highest sectors of the Alps (Keller & 
Krayss, 2010; Preusser et al., 2011; van 
Husen & Reitner, 2011a) without directly 
reaching the foreland, but enhancing the 
development of widespread alluvial and 
braided systems at the outlets of Alpine val-
leys, because of the increased sediment 
supply and water discharges. Such process-
es enabled the formation of loess in the Al-
pine Foreland, as recorded in the loess ar-
chives of Stranzendorf, showing the onset of 
loess at the G/M boundary and Krems-
Schießstätte starting with the Olduvai event 
(Fink et al., 1976; Fink & Kukla, 1977). More-
over, the occurrence of trunk valley glaciers 
is still debated as the carving of major valleys 
occurred later, starting from the late Matuya-
ma (Häuselmann et al., 2007; Valla et al., 
2011).  

 
4. LATE MATUYAMA GLACIATIONS 
(MIS22-20) 

 
According to Muttoni et al. (2003) the 

“major” glaciations in the southern side of the 
Alps started at about 0.9 Ma when extensive 
boreal ice sheets expanded (Batchelor et al., 
2019; Greenwood et al., 2022). For “major” 
we mean a climatic stage which was cold 
and long enough to allow the glaciers to 
spread out from the main Alpine valleys, 
forming piedmont lobes in the foreland at 
both the sides of the mountain range.  

In the northern foreland, the till interbed-
ded with Deckenschotter at the Swiss Feusi 
site (Fig. 3A) was dated to 0.9 ±0.1 Ma with 
the P-PINI cosmogenic nuclide burial-dating 
model for glacial deposits (after Knudsen et 
al., 2020). In addition, two Deckenschotter 
sites attributed to the Steig Gravels (sensu 
Graf, 1993) at Irchel were dated to 0.9 ±0.2 
and 1.3 ±0.1Ma using isochron-burial dating 
technique with cosmogenic 26Al and 10Be 
(Claude et al., 2019; Dieleman et al., 2022). 
In the German-Austrian foreland, the 
Lichtenegg diamicton (Menzies & Ellwanger, 
2010; Ellwanger et al., 2011) and the fine-
grained deposits intercalated with the glacial 
till at Pfullendorf (Bibus et al., 1996; Doppler et al., 2011) 
were ascribed to the Early Pleistocene based on reverse 
polarity. Fluvial deposits related to the Älterer Deck-
enschotter (Older Cover Gravels) (Ellwanger et al., 
1995, 2011) at Altheiligenberg showed reverse polarity 
(Fromm, 1989). The covering loess of the Hohere Älterer 

 
 

131 

 

Fig. 3 - A) Outcrop of Deckenschotter at Feusi (Switzerland) (28 in Fig. 1). 
Weakly cemented, in part cross-bedded, gravels interbedded with a 2-m-thick till 
layer (beige unit in the center left of photograph). Numerous glacially striated 
clasts have been found in this till layer. The deposit is capped by deeply weath-
ered till, likely Middle Pleistocene in age (Haldimann et al., 2017). Calculated 
10Be-26Al isochron-burial age of the till is 1.3-0.9 Ma (Grischott et al., 2020; 
Knudsen et al., 2020); B) Outcrop of Deckenschotter at Irchel (Steig Gravels 
sensu Graf, 1996) (28 in Fig. 1). Steig gravels were dated to 0.9 ±0.1 Ma by 
isochron-burial dating with cosmogenic 10Be and 26Al (Claude et al. 2019; Diele-
man et al., 2022); C) Outcrop of Deckenschotter Siglistorf. Calculated 10Be-26Al 
isochron-burial age of these gravels is1.5 ±0.2 Ma (Akçar et al., 2017) (29 in 
Fig. 1); D) Close-up view of Bünten till in the Bünten Gravel Pit at Möhlin, Can-
ton of Basel (29 in Fig. 1). This till dates back to 0.5 ±0.1 Ma by isochron-burial 
dating with cosmogenic 10Be and 26Al (Dieleman et al., 2022). Hammer on the 
picture is for scale; E) Weathering horizon on top of Weisse Nagelfluh (white 
conglomerate) overlain by Graue Nagelfluh (grey conglomerate; proglacial de-
posits of the Günz glaciation) indicating a stable surface under supposed inter-
glacial conditions (location: Kremsmünster, site 19 in Fig. 1, height of the out-
crop approximately 4 m). 

 
 
The Early and Middle Pleistocene glaciations in the Alps  



   

 

Langenloiser terrace of the Danube (van Husen & Reit-
ner, 2011a). The Eichwaldschotter glaciofluvial unit in 
the Salzach piedmont area was tentatively ascribed to 
MIS 22 (van Husen & Reitner, 2011 a, b), because of 
the similarity in facies and presence of lithologies of the 
typical glaciofluvial sediments of the Middle Pleistocene. 

According to the evidence from the northern and 
southern sides, trunk valleys hosted valley glaciers that 
likely originated from ice domes located in the axial sec-
tor of the Alps. In the northern Swiss foreland, the gla-
cial deposits interbedded into the Deckenschotter point 
to an extension of the glaciers similar to but somewhat 

more extensive than the LGM (cf. Frei, 1912; Graf, 
1993; Doppler et al., 2011; Ellwanger et al., 2011; Knud-
sen et al., 2020).  

In the southern side, the first major glaciation has 
been chronologically constrained by magnetostratigra-
phy in the Po Plain subsurface and occurred in the late 
Matuyama chron, between the end of the Jaramillo 
(0.99 Ma) and the beginning of the Brunhes chron (0.78 
Ma; Muttoni et al., 2003, 2007; Scardia et al., 2006, 
2012). Based on this chronostratigraphic framework, 
reverse magnetizations in glacigenic deposits (Carraro 
et al., 1991; Scardia et al., 2010, 2015; Graf, 2019) have 

Fig. 4 - A) The 500 km2 wide Ivrea Morainic Amphitheatre (IMA) (site 2 in Fig. 1) represented by DTM (courtesy of the Piedmont Region) 
extends to the outlet of the Dora Baltea Valley (DB). The bedrock crops out in the IMA inner sector in the granulite Ivrea Hills (IH) and in 
the outer western sector in the Monti Pelati peridotite reliefs (MP). The Serra d'Ivrea lateral moraines, the inner depression (ID) and the 
outer outwash plain (OP) are pointed out. The Dora Baltea River flows out of the IMA through the Mazzé gorge (MA). At the northeastern 
edge the Bessa roman gold mine (BE) extends into a sector previously occupied by the two oldest glacigenic units. White square indicates 
the location of the geological map showed in B. B) Geological sketch map of the IMA left lateral north-eastern sector, which retains the 
largest number of recognized glacigenic units in the IMA. The pre-LGM glacigenic succession is divided in seven synthems referred to as 
many glaciations ranging from the end of Early Pleistocene to the Late Pleistocene. The Bornasco and Montino units separated by an 
interstadial layer (2) are regarded to as subsynthems. The Ivrea Synthem referred to the LGM is split into Internal Serra (Ise, max LGM 
advance), Piverone (Piv), Palazzo (Pal) and Andrate (And) subsynthems. C) Geological cross-section of the IMA lateral north-eastern 
sector (from Gianotti et al., 2015, modified). Profile trace is shown in B (blue line). Interstadial or interglacial markers are indicated with 
asterisks: 1) Bosa Palaeosol; 2) Sorgente Solfurea peat layer; 3) Comunità palaeosol; 4) Gianetto gyttja layer. The glacigenic sequence is 
tentatively related to the Pleistocene glaciations. Possible hypotheses are proposed for Magnano and External Serra units. The correlation 
is made with the global isotopic curve from Lisiecki & Raymo (2005), which is a synthesis of 57 benthic marine oxygen isotope records. 
Chronological boundaries between marine isotope stages (MIS) are reported. 

 
 

132 

 
 

Monegato G. et al. 



   

 

produced the spread of the glaciers. Considering the 
size of the Laurentide Ice Sheet (LIS) and the European 
Ice Sheet (EIS), a circulation model similar to the one 
that produced the Alpine LGM (Florineth & Schlüchter, 
2000; Luetscher et al., 2015; Monegato et al., 2017) can 
be supposed. However, the narrative of this period (761-
242 ka BP, between MIS 18 and MIS 8 cold stages) 
strongly suffers from lack of chronologic constraints, and 
glacial units are best grouped as pre-LGM deposits with 
normal magnetic polarity.  

In the Swiss sector, in addition to field evidence, 
paleobotanical data and luminescence dating were the 
basis for distinguishing three major glacial units: Möhlin, 
Habsburg and Hagenholz glaciations (Preusser et al., 
2011; Schlüchter et al., 2020). Several detailed studies 
on boreholes led to the conclusion that the Middle Pleis-

been confidently ascribed to a late Matuyama 
glaciation and allowed to infer the spatial 
distribution of the first morainic landforms in 
the Alpine foreland, even if they have been 
subsequently eroded. The size of the glaciers 
and the presence of an Alpine Ice field are 
still debated. In the distal sector, the Po Plain 
was filled by outwash streams (Muttoni et al., 
2003; Scardia et al., 2006; Garzanti et al., 
2011). The Ivrea (San Michele-Borgo and 
Granero units in Carraro et al., 1991; 
Mongrando unit in Gianotti et al., 2015) (Fig. 
4 and Fig. 5C) and Garda (Ciliverghe Hill and 
the Chiese River sequence, Fig. 5D) morain-
ic amphitheaters hosted wide glacier pied-
mont lobes and it is likely that also the Ver-
bano (Morazzone unit, but possibly also the 
Immacolata and Vivirolo formations) and the 
Oglio (Valenzano unit) glacier lobes spread 
out from the valley (Bini, 2004a). With re-
spect to the Adda Glacier, paleomagnetic 
analysis of the Brugora glaciolacustrine se-
quence, formerly attributed to the Bozzente 
unit (Bini et al., 2014), provided reverse mag-
netization (Fig. 6). Actually, the deposits of 
the Bozzente unit, as properly defined in 
terms of weathering profile and geomorpho-
logic position (Zuccoli, 2000; Bini et al., 2014) 
bear Brunhes chron normal magnetization 
(Scardia et al., 2010), thus the Brugora site 
must be ascribed to the late Matuyama glaci-
ations, possibly correlative of the San Salva-
tore till (Zuccoli, 2000). Remnants of Alpine 
intermontane basins, such as Ecoteaux, 
Leffe, and Pianico, also recorded vegetation-
al changes and glacigenic deposits related to 
the late Matuyama glaciation (Pugin et al., 
1993; Muttoni et al., 2007; Scardia & Muttoni, 
2009). 

According to Häuselmann et al. (2007), 
intensive glacial overdeepening of Alpine 
valleys began during the late Matuyama ad-
vance (i.e. Aare Valley). Since the late 
Matuyama, the progressive development of 
even more extensive glaciations has promot-
ed deep valley incision and overdeepening in 
many sectors of the Alps. However, it is likely 
that the late Matuyama ice domes had smaller volumes 
than in the Middle to Late Pleistocene glaciations, con-
sidering even if the extension of the piedmont lobes 
looks quite similar. It is remarkable that both the French 
Western Alps and the Eastern Alps are apparently mis-
sing remnants of Matuyama glacial units (Ivy-Ochs et al., 
2022 and references therein).  

 
5. EARLY-MIDDLE BRUNHES GLACIATIONS (MIS18-
8) 

 
Marine Isotope Stages 16 and 12 are related to the 

greatest extents reached by boreal ice sheets (Batchelor 
et al., 2019) as recorded by the prominent spikes of δ18O 
(Lisiecki & Raymo, 2005, Bell et al., 2014; Farmer et al., 
2019). It is likely that also in the Alps these cold phases 

 
 

133 

 

Fig. 5 - A) Frontal moraine of the Bornasco unit (Middle Pleistocene) in the Ivrea 
end moraine system (site 2 in Fig. 1); B) Weathered lodgment till of the Zubiena 
unit (Middle Pleistocene) in the Ivrea end moraine system (site 2 in Fig. 1); C) 
Lodgment till and glaciolacustrine deposits of the Mongrando unit (Early Pleisto-
cene) in the Ivrea end moraine system (site 2 in Fig. 1); D) Weathered fluvio-
glacial deposits (Middle Pleistocene) of Ciliverghe laying on Early Pleistocene 
fluvial and glacial units in the Garda end moraine system (site 7 in Fig. 1). 

 
 
The Early and Middle Pleistocene glaciations in the Alps  



   

 

tocene was a period of intense incision and valley over-
deepening after deposition of the Deckenschotter units. 
In many foreland valleys of the Swiss sector the bedrock 
floor is hundreds of meters beneath the present surface 
topography (Jordan, 2010; Preusser et al., 2010). Paly-
nological and luminescence data suggest that aggrada-
tion phases and filling of the overdeepened valleys be-
gan no later than 450 ka (MIS 12; Preusser et al., 2010; 
Reitner et al., 2010; Gegg et al., 2023; Schwenk et al., 
2022), possibly related to erosion-driven flexural uplift of 
the Alps (Scardia et al., 2012). Recent studies ascribed 
the overdeepening in the Bern area/Aare Valley to MIS 
12 (Gegg et al., 2020; Schwenk et al., 2022). Recently, 

Dieleman et al. (2022) studied the till layer (Fig. 3D), 
which is exposed in a gravel pit at Möhlin (Canton of 
Basel) and attributed it to the Möhlin glaciation. The 
cosmogenic nuclide analysis in the clasts embedded in 
this till layer indicated a deposition age of 0.5 ±0.1 Ma. 

In the Austrian foreland, paleomagnetic constraints 
in loess successions (Scholger & Terhorst, 2013) and 
geological considerations (van Husen & Reitner, 2011a, 
b) were used to tentatively correlate the Günz and Min-
del glaciations with the severe global climatic deteriora-
tions of MIS 16 and MIS 12. In the Austrian part, the 
preserved morphological and sedimentary record indi-
cates the Mindel glaciation as the largest one. Günz end 

 
 

134 

 

Fig. 6 - The Brugora site from the Brianza lobe of Adda Glacier (site 5 in Fig. 1). A) lodgement till passing upward to B) glaciolacutrine fine-
grained, laminated deposits with drop-stones. C) Orthogonal projection of thermal demagnetization data of representative samples from 
the Brugora site. D) Equal-area projection of the characteristic component vectors determined for the Brugora glaciolacustrine deposits. 
Open circles indicate negative inclinations and plot onto the upper hemisphere. 

 
 

Monegato G. et al. 



   

 

“external moraine complex” and ascribed to cold phases 
of the Middle Pleistocene (Mandier, 1982).  

 
6. THE PENULTIMATE GLACIATION (MIS6) 
 

The penultimate glaciation occurred at the end of 
the Middle Pleistocene and it is considered as the lar-
gest in term of ice sheets volume (Batchelor et al., 
2019). Deposits related to this cold phase in the Alps 
were dated with luminescence methods on glaciofluvial 
and glaciolacustrine exposed successions (Preusser & 
Schlüchter, 2004; Bickel et al., 2015a, b; Salcher et al., 
2015; Schielein et al., 2015; Rades et al., 2018). In the 
Swiss-German sector, detailed sedimentological work 
and luminescence dating have been done also on cores 
taken from the overdeepened valleys (Dehnert et al., 
2012; Lowick et al., 2015; Buechi et al., 2018), obtaining 
ages from MIS 6 or even somewhat earlier (Gegg et al., 
2022). These studies depicted several phases of glacier 
advance and withdrawal, suggesting complex dynamics 
of the Rhine glacier system from the end of MIS 7 to the 
waning stages of MIS 6. In many end-moraine systems 
of the Alps, glacial deposits and landforms related to the 
penultimate glacial cycle are often close to those of the 
LGM, suggesting a comparable extension. They are 
distinguishable because their soils are much more de-
veloped, disallowing their attribution to the later Pleisto-
cene (e.g., Venzo, 1977; Castiglioni, 2004; Zanferrari et 
al., 2008; Buoncristiani & Campy, 2011; Doppler et al., 
2011; Preusser et al., 2011; Ellwanger et al., 2011; van 
Husen & Reitner, 2011a; Gianotti et al., 2015; Fioraso et 
al., 2021). In the French Western Alps it is considered 
the “external moraine complex”, tentatively associated 
to the Riss (Buoncristiani & Campy, 2011). In the east-
ern part of the Austrian Alps an exceptionally large MIS 
6 glaciation with terminal moraines up to 40 km down-
valley of their LGM counterparts, like in the Enns Valley 
(Eastern Alps), did occur (Fig. 7). Such findings in nar-
row and gently sloping valleys can be explained by ice-
dynamical reasons, such as ice congestions resulting in 
a disproportionate increase of accumulation areas of the 
Salzach and Enns (van Husen, 2000), promoted by the 
moderate additional lowering of the ELA of around 100 
m (Penck & Brückner, 1901-1909). In the Julian Alps, 
ice-marginal and glacial deposits were dated to MIS 6 
glaciation in the Soča Valley (Bavec et al., 2004; 
Jamšek Rupnik et al., 2022). In the southern side of the 
Alps, MIS 6 moraines are normally very close or partially 
buried by LGM terminal moraines. This situation can be 
detected in many morainic amphitheaters (Cremaschi, 
1987; Rossato et al., 2013; Gianotti et al., 2015; Fioraso 
et al., 2021; Kamleitner et al., 2022). In the Verbano and 
Lario amphitheatres, the Besnate Allogroup, formerly 
ascribed to the Middle-Late Pleistocene (Bini, 1997), 
has been dated to the LGM (Kamleitner et al., 2022), 
suggesting that Golasecca and Binago units (Tab.1) can 
be tentatively ascribed to MIS 6. In the Tagliamento 
sector the MIS 6 moraines and glaciofluvial units were 
traced from the end moraine system to the coastline 
(Zanferrari et al., 2008; Pini et al., 2009; Fontana et al., 
2010). 

 
 

moraines are only preserved where the Mindel glaciers 
had a slightly different advance direction. An outstanding 
Middle Pleistocene succession at Kremsmünster in the 
Krems Valley (19 in Fig. 1) is ascribed to glaciofluvial 
aggradation (Kohl, 2000); it is stratigraphically confined 
between Günz and Mindel tills and glaciofluvial deposits, 
suggesting a cold phase of minor landscape modification 
between MIS 16 and MIS 12. This stratigraphic architec-
ture still needs chronological constraints for a better 
assessment. 

In many morainic amphitheaters of the southern 
Alpine sector the early-middle Brunhes glaciations are 
distinguished in the stratigraphic architecture by the 
means of bounding surfaces marked by buried soils 
(paleosols), pedostratigraphy based on surface soils 
(Bini et al., 2004a; Gianotti et al., 2015; Fioraso et al., 
2021), occurrence of loess (Venzo, 1965) or interbedded 
organic layers containing warm flora (Pini et al., 2009; 
Gianotti et al., 2008; 2015). In detail, in the eastern sec-
tor of the Ivrea Morainic Amphitheatre, seven units 
(Bornasco, Montino, Zubiena, Parogno, Torrazzo, Ma-
gnano and External Serra) are tentatively ascribed to the 
Middle Pleistocene glaciations (Fig. 4), apart from the 
possibility of a Late Pleistocene, pre-LGM age for the 
External Serra unit (Gianotti et al., 2008; 2015). The 
Mongrando (MIS 22-20, with reversed polarity) and Bor-
nasco (MIS 18) units are separated by the Bosa paleo-
sol (MIS 19 interglacial). The Bornasco (MIS 18e) (Fig. 
5A) and Montino (MIS 18a) sub-units are separated by 
the Sorgente Sulfurea peaty layer with cool-climate pol-
lens (MIS18b-d interstadial) and so they can be correla-
ted to the two peaks of the MIS 18 glaciation, Montino 
sub-unit (MIS 18) and Zubiena unit (MIS 16) (Fig. 5B) by 
the Cascina Comunità palaeosol (MIS 17 interglacial), 
the Parogno (MIS 12) and Torrazzo units (MIS 10) by 
the Cascina Gianetto palustrine gyttja with warm-climate 
pollens (MIS 11.3 interglacial, Gianotti et al., 2015).  
Other stratigraphic boundaries (Zubiena-Parogno and 
Torrazzo-Magnano) were identified by pedostratigraphy; 
pedogroup A (Mongrando to Zubiena units) shows hue 
2.5YR, pedogroup B (Parogno and Torrazzo units) hue 
5YR, and pedogroup C (Magnano, External Serra and 
Ivrea synthems) hue 7.5YR. Within the less ancient pe-
dogroup, the Magnano unit (MIS 8 or, more likely, MIS 
6) is distinguishable from the External Serra unit (MIS 6, 
MIS 4 or MIS 3, based on pre-LGM exposure ages of 
erratic boulders) by soils with a thicker B horizon (> 2 m) 
and a higher degree of weathering of the clasts.  

In others morainic amphitheaters of the Lombardy 
piedmont plain several Middle Pleistocene landform 
remnants (moraines and kame terraces) were distin-
guished through the occurrence of paleosols, loess cov-
er and peat layers (Bini et al., 2004a, 2014). Each mo-
raine system has its own stratigraphic subdivision (Tab. 
1), even if geochronological constraints are poor. In the 
Verbano area thick aeolian deposition ascribed to Middle 
Pleistocene cold phases have been distinguished by 
means of paleosols (Terhorst & Ottner, 2003; Terhorst et 
al., 2012; Terhorst, 2013). At east of the Garda system, 
glacial deposits related to early-middle Brunhes are lack-
ing or debated (Zanferrari et al., 2013). The same lack of 
information occurs in the French side of the Western 
Alps, where glaciofluvial units were detected outside the 

 
 

135 

 
 
The Early and Middle Pleistocene glaciations in the Alps  



   

 

 

 
 

136 

 

Fig. 7 - Glacier extent during the Würmian (MIS 2) and Rissian (MIS 6) in the Enns valley and environs and in the Steyr and Ybbs valleys 
(mod. after van Husen, 2011a). 

Fig. 8 - Correlation sketch of the glacial/glaciofluvial units recognized for each sector of the Alps; numbers indicate the sites of Fig. 1 and 
Tab. 1. Black triangles indicate glacial unit and black dots glaciofluvial unit. Green color points to available chronology; yellow color points 
to available reverse polarity. δ18O curve from Lisiecki & Raymo (2005).  

 
 

Monegato G. et al. 



   

 

tary analyses with paleoclimatic proxies (i.e. pollen data) 
that indicate which part of the succession can be related 
to cold stages. For Early Pleistocene glaciations this 
means multidisciplinary investigation on deep cores of 
the depocenter areas (i.e., Po Plain, Rhine graben, and 
Vienna Basin) coupled with investigation in major val-
leys (Anselmetti et al., 2022). 

 
7.2. Extent of glaciations? 

As depicted by the distribution of the preserved 
record, we can argue how glacier expansions developed 
during each cold stage. The reconstruction of the paleo-
climate during the LGM showed how the Alps are sensi-
tive to small shifts in atmospheric that conditioned the 
ELA lowering circulation (Luetscher et al., 2015; 
Monegato et al., 2017; Gribenski et al., 2021). Moreo-
ver, the asymmetry of the Alpine range in terms of distri-
bution of high elevation areas would contribute to dif-
ferentiate the major accumulation sectors according to 
their location with respect to the storm tracks feeding 
the glaciers. As remarked, for example, by the large 
extent of the MIS 6 glaciation in the Austrian sector 
(Ybbs and Enns in Tab. 1 and Fig. 7), we suppose that 
slightly lower ELA can cause the development of a 
much larger glacier system. In this perspective, the con-
cept of a most extensive glaciation can be applied only 
in specific sectors of the range and must not encompass 
the whole Alps. The fact that MIS 12, MIS 6 or LGM 
frontal moraines occupy the outermost position in east-
ern and southeastern Alps more frequently than in the 
southwestern or the northern Alps points to different 
distribution of precipitation during each cold phase, de-
termining the size of the glaciers and piedmont lobes.  

 
7.3. Which were the major glaciations? 

Dissimilar distribution of the glacial units in the 
circumalpine area points to a reduced number of “major” 
glaciations and the most extensive glaciation concept 

7. DISCUSSION  
 
7.1. How many glaciations? 

Located at mid latitude between the Mediterranean 
Sea and continental Europe, the Alps are the highest 
mountain range of this continent and are very sensitive 
to climate changes. In this way, they can have hosted 
mountain glaciers since the onset of the Pleistocene 
glaciations. The available data of glacigenic deposits 
older than the Late Pleistocene are numerous, also 
thanks to more than 150 years of research, and can 
provide insights on how the Pleistocene cold stages 
affected the Alps and how many times.  

According to the available data from the area with 
the more detailed stratigraphic successions (Fig. 8), a 
minimum of 13 different glacier advances of Early to 
Middle Pleistocene age are recognized in the Swiss 
Foreland (Preusser et al., 2011; Schlüchter et al., 2020), 
about nine to ten in the Ivrea and Verbano sectors (Bini, 
1997; Gianotti et al., 2015; Zuccoli, 2000), but apparent-
ly only four in the Lake Garda area (Cremaschi, 1987) 
and two in the Tagliamento system (Zanferrari et al., 
2013). These events should represent locally just the 
major glacier expansions onto the foreland (Fig. 9) and 
other cold stages (e.g. MIS 14 and MIS 8 stages, ac-
cording to their weaker isotopic signal in the MIS curve) 
should have seen glaciers expanded but remaining 
within the Alpine valleys. Moreover, the occurrence of 
multiple phases of glacier advance and withdrawal within 
the same cold stage (i.e., Dehnert et al., 2012; Lowick et 
al., 2015) has to be carefully considered for a correct 
counting of glaciation in a single sector. 

Glaciofluvial input in the foreland is also an im-
portant tracer of sediment production and delivery during 
cold stages (Scardia et al., 2006, 2012; Garzanti et al., 
2011; Preusser et al., 2021; Marcolla et al., 2021). How-
ever, to distinguish them in the Lower-Middle Pleisto-
cene successions implies the coupling of the sedimen-

 
 

137 

Fig. 9 - Map of the Alps with the sectors of Tab. 1 colored for number of recorded glaciation: blue (1-2), purple (3-4), orange (5-6), red (>6).  

 
 
The Early and Middle Pleistocene glaciations in the Alps  



   

 

 

 
 

138 

 
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its

) 
M

id
d

le
 P

le
is

to
ce

ne
 

  
pa

le
os

ol
 (1

0-
2.

5Y
R

 h
ue

 c
ol

or
 in

de
x)

, s
tra

tig
ra

ph
ic

 c
or

re
la

tio
n 

C
re

m
as

ch
i e

t a
l.,

 1
98

5;
 Z

uc
co

li,
 2

00
0 

S
a

n
 S

a
lv

a
to

re
 

M
IS

2
0-

2
2

 
  

re
ve

rs
e 

po
la

rit
y 

Sc
ar

di
a 

et
 a

l.,
 2

01
0 

C
a

sa
n

o
va

 L
a

n
za

 G
ro

up
 

E
a

rly
 P

le
is

to
ce

n
e?

 
  

st
ra

tig
ra

ph
ic

 c
or

re
la

tio
n 

Bi
ni

 e
t a

l.,
 2

01
4 

6 
C

am
o

n
ic

a 
V

al
le

y 
(S

eb
in

o
) 

M
o

n
te

ro
to

nd
o 

M
id

d
le

 P
le

is
to

ce
ne

 
  

pa
le

os
ol

 (1
0-

7.
5Y

R
 h

ue
 c

ol
or

 in
de

x)
, s

tra
tig

ra
ph

ic
 c

or
re

la
tio

n 

C
as

si
ni

s 
et

 a
l.,

 2
01

1 

M
o

n
te

 P
ia

ne
 

M
id

d
le

 P
le

is
to

ce
ne

 
  

pa
le

os
ol

 (5
-7

.5
YR

 h
ue

 c
ol

or
 in

de
x)

, s
tra

tig
ra

ph
ic

 c
or

re
la

tio
n 

F
a

n
te

co
lo

 
M

id
d

le
 P

le
is

to
ce

ne
 

  
pa

le
os

ol
 (5

-7
.5

YR
 h

ue
 c

ol
or

 in
de

x)
, s

tra
tig

ra
ph

ic
 c

or
re

la
tio

n 

C
a

m
ig

n
o

ne
 

M
id

d
le

 P
le

is
to

ce
ne

 
  

pa
le

os
ol

 (1
0-

5Y
R

 h
ue

 c
ol

or
 in

de
x)

, s
tra

tig
ra

ph
ic

 c
or

re
la

tio
n 

P
a

d
e

rn
o

 d
i F

ra
n

ci
a

co
rt

a
 

M
id

d
le

 P
le

is
to

ce
ne

 
  

pa
le

os
ol

 (1
0-

5Y
R

 h
ue

 c
ol

or
 in

de
x)

, s
tra

tig
ra

ph
ic

 c
or

re
la

tio
n 

V
a

le
n

za
n

o 
E

a
rly

 P
le

is
to

ce
n

e?
 

  
pa

le
os

ol
 (1

0-
2.

5Y
R

 h
ue

 c
ol

or
 in

de
x)

, s
ca

tte
re

d 
bo

ul
de

rs
 

7 
A

d
ig

e
/S

a
rc

a
 

va
ll

e
ys

 (
G

a
rd

a
) 

S
e

d
en

a
/A

lb
a

re
 

M
id

d
le

 P
le

is
to

ce
ne

 
  

th
ic

k 
pa

la
eo

so
l o

n 
to

p 
an

d 
st

ra
tig

ra
ph

ic
 c

or
re

la
tio

n 
C

re
m

as
ch

i, 
19

87
,  

Ac
co

rs
i e

t a
l.,

 1
99

0 
C

a
rp

e
n

ed
o

lo
 

M
id

d
le

 P
le

is
to

ce
ne

 
  

C
a

rp
e

n
ed

o
lo

-M
o

n
tic

h
ia

ri 
M

id
d

le
 P

le
is

to
ce

ne
 

  

C
ili

ve
rg

h
e

 
M

IS
2

0-
2

2
 

  
re

ve
rs

e 
po

la
rit

y 
C

re
m

as
ch

i, 
19

87
; B

ar
on

i &
 C

re
m

as
ch

i, 
19

87
; 

Sc
ar

di
a 

et
 a

l.,
 2

01
5 

7a
 

A
d

ig
e

 V
a

ll
e

y 
(R

iv
o

li
 V

er
o

n
es

e)
 

M
o

n
te

 C
riv

e
lli

n
o

 
M

id
d

le
 P

le
is

to
ce

ne
 

  
  

Ac
co

rs
i e

t a
l.,

 1
99

0 
C

a
p

rin
o 

M
id

d
le

 P
le

is
to

ce
ne

 
  

  

P
e

si
n

a 
E

a
rly

 P
le

is
to

ce
n

e?
 

  
  

8 
A

s
ti

c
o

 V
a

ll
e

y 
(C

o
g

o
llo

) 
S

e
gh

e
tta

 
M

IS
 6

 
  

po
lle

n 
da

ta
 

R
os

sa
to

 e
t a

l.,
 2

01
3 

P
rà

 d
e 

O
ch

i 
M

id
d

le
 P

le
is

to
ce

ne
 

  
  

C
uc

at
o,

 2
00

1 

9 
P

ia
ve

 V
a

ll
e

y 
R

is
s 

gl
a

ci
a

l 
M

id
d

le
 P

le
is

to
ce

ne
 

  
th

ic
k 

pa
la

eo
so

l o
n 

to
p 

an
d 

st
ra

tig
ra

ph
ic

 c
or

re
la

tio
n 

Ve
nz

o,
 1

97
7 

10
 

T
ag

lia
m

e
n

to
 

P
la

in
o 

M
IS

 6
 

  
Po

lle
n 

da
ta

 a
nd

 s
tra

tig
ra

ph
ic

 c
or

re
la

tio
n 

Za
nf

er
ra

ri 
et

 a
l.,

 2
00

8;
 L

ow
ic

k 
et

 a
l.,

 2
01

0 

L
e

d
ra

n
ia

 
M

id
d

le
 P

le
is

to
ce

ne
 

  
w

ea
th

er
ed

 g
la

ci
al

 re
m

na
nt

s 
on

ly
 in

 th
e 

lo
w

er
 v

al
le

y 
M

on
eg

at
o 

an
d 

St
ef

an
i, 

20
11

;  
Za

nf
er

ra
ri 

et
 a

l.,
 2

01
3 

11
 

S
o
č

a/
Is

o
n

zo
 

R
a

vn
i L

a
z/

 M
o

d
re

jc
e 

M
IS

 6
 

IR
S

L
 d

a
te

s 
in

 B
o

ve
c:

 1
5

4
.7

 ±
2

2.
8

 k
a

 a
n

d
  

U
/T

h 
d

at
e

s:
 1

52
.7

 k
a

. O
S

L
 d

a
te

s 
in

 M
o

-
d

re
jc

e
: 

16
5

 ±
6

5 
ka

 a
n

d 
1

6
9 

±2
1 

ka
 

  
Ba

ve
c 

et
 a

l.,
 2

00
4;

 B
av

ec
 &

 V
er

bi
c,

 2
01

1 
Ja

m
še

k 
R

up
ni

k 
et

 a
l.,

 2
02

2 

12
 

S
a

va
 

B
le

d-
R

ad
ov

lji
ca

 
M

IS
 6

 
IR

S
L 

da
te

s:
 1

5
6 

±1
8 

ka
 

  
Ba

ve
c 

& 
Ve

rb
ic

, 2
01

1 

U
d

in
 B

o
rš

t 
E

a
rly

 P
le

st
o

ce
ne

 
C

o
sm

o
ge

n
ic

 a
ge

: 
1.

9
 ±

0
.2

 M
a 

  
M

ih
ev

c 
et

 a
l.,

 2
01

5 

13
 

D
ra

u
 

R
is

s 
gl

a
ci

a
l 

M
IS

 6
 

  
  

Bo
be

k,
 1

95
9;

 v
an

 H
us

en
, 1

98
9 

 
 

Monegato G. et al. 

T
ab

. 1
A

 



   

 

 

 
 

139 

 
G

la
ci

a
te

d
 

b
as

in
 

U
n

it
 

A
g

e
 

K
e

y 
re

fe
re

n
ce

s
 

A
tt

ri
b

u
ti

o
n

 
D

at
es

 
O

th
er

 c
o

n
st

ra
in

ts
 

14
 

M
u

r 
R

is
s 

gl
a

ci
a

l 
M

IS
 6

 
  

  
Sp

re
itz

er
, 1

96
1 

15
 

E
rl

au
f 

R
is

s 
gl

a
ci

a
l 

M
IS

 6
 

  
  

M
os

er
 &

 S
ch

na
be

l, 
20

19
 

16
 

L
am

in
g

 
R

is
s 

gl
a

ci
a

l 
M

IS
 6

 
  

  
Br

yd
a 

et
 a

l. 
20

13
 

17
 

Y
b

b
s

 
R

is
s 

gl
a

ci
a

l 
M

IS
 6

 
L

u
m

in
e

sc
en

ce
 d

a
te

s:
 1

5
0

±1
4

 k
a

 (
p

IR
IR

22
5

) 
to

 
1

2
9

±1
4

 k
a

 (
O

S
L

) 
  

N
ag

l, 
19

70
; B

ic
ke

l e
t a

l. 
20

15
a 

18
 

E
n

n
s 

R
is

s 
gl

a
ci

a
l 

M
IS

 6
 

  
  

Eg
ge

r &
 v

an
 H

us
en

, 2
01

1 

19
 

S
te

yr
-K

re
m

s
 

R
is

s 
gl

a
ci

a
l 

M
IS

 6
 

  
  

va
n 

H
us

en
, 1

97
5,

 2
00

0;
 K

oh
l, 

19
99

 

M
in

d
e

l g
la

ci
a

l 
M

IS
 1

2 
  

  
Ko

hl
, 2

00
0 

va
n 

H
us

en
, 2

00
0;

 
G

ü
n

z 
gl

a
ci

a
l 

M
IS

 1
6 

  
  

20
 

A
lm

 
R

is
s 

gl
a

ci
a

l 
M

IS
 6

 
  

  
Eg

ge
r, 

20
07

a 

21
 

T
ra

u
n

 

R
is

s 
gl

a
ci

a
l 

M
IS

 6
 

  
po

lle
n 

da
ta

 
Eg

ge
r, 

20
07

a,
 b

;  
va

n 
H

us
en

 &
 E

gg
er

, 2
01

4 
M

in
d

e
l g

la
ci

a
l 

M
IS

 1
2 

  
  

G
ü

n
z 

gl
a

ci
a

l 
M

IS
 1

6 
  

  
Ko

hl
 2

00
0;

 E
gg

er
, 2

00
7a

 

22
 

S
a

lz
ac

h
 

R
is

s 
gl

a
ci

a
l 

M
IS

 6
 

O
S

L
 d

a
te

s:
 1

9
3

±3
0

 k
a

 1
8

8
±2

7
 k

a 
  

W
ei

nb
er

ge
r, 

19
55

; R
up

p 
et

 a
l.,

 2
01

1 
Sa

lc
he

r e
t a

l.,
 2

01
5 

M
in

d
e

l g
la

ci
a

l 
M

IS
 1

2 
  

  
W

ei
nb

er
ge

r, 
19

55
; v

an
 H

us
en

, 2
00

0;
 D

op
pl

er
 e

t 
al

., 
20

11
 

G
ü

n
z 

gl
a

ci
a

l 
M

IS
 1

6 
  

  

23
 

In
n

-C
h

ie
m

se
e 

R
is

s 
gl

a
ci

a
l 

M
IS

 6
 

  
  

D
op

pl
er

 e
t a

l.,
 2

01
1 

M
in

d
e

l g
la

ci
a

l 
M

IS
 1

2 
  

  

24
 

Is
a

r-
L

o
is

a
c

h
 

R
is

s 
gl

a
ci

a
l 

M
IS

 6
 

  
  

D
op

pl
er

 e
t a

l.,
 2

01
1 

P
a

rs
b

e
rg

 S
W

 P
u

ch
h

e
im

 
M

id
d

le
 P

le
is

to
ce

ne
 

  
  

25
 

L
e

c
h

-W
e

rt
ac

h
 

L
e

n
ge

nf
e

ld
-L

u
d

w
ig

sb
e

rg
 

M
IS

 6
 

  
  

D
op

pl
er

 e
t a

l.,
 2

01
1 

26
 

Il
le

r 
R

is
s 

gl
a

ci
a

l 
M

IS
 6

 
  

  
D

op
pl

er
 e

t a
l.,

 2
01

1 
H

o
lz

h
e

u
e

r 
H

ö
h

e 
B

ra
nd

h
o

lz
-

M
a

n
n

eb
e

rg
 

M
id

d
le

 P
le

is
to

ce
ne

 
  

  

27
 

R
h

e
in

 

D
o

p
p

e
lw

a
ll 

R
is

s 
M

IS
 6

 
IR

S
L

 d
a

te
s:

 1
4

9
 ±

1
5

 to
 1

7
9 

±1
7 

ka
 

  
R

ad
es

 e
t a

l.,
 2

01
8 

L
a

up
e

rt
sh

a
u

se
n 

M
id

d
le

 P
le

is
to

ce
ne

 
  

  
Sc

hr
ei

ne
r, 

19
97

; D
op

pl
er

 e
t a

l.,
 2

01
1 

H
ei

lig
en

be
rg

 
E

ar
ly

?
-M

id
dl

e
 P

le
is

to
ce

n
e 

  
  

S
ch

ie
ne

rb
e

rg
 D

e
ck

e
n

sc
h

o
tte

r 
E

a
rly

 P
le

is
to

ce
n

e 
  

  
G

ra
f, 

20
09

a 

C
h

ro
o

b
a

ch
 D

e
ck

e
n

sc
ho

tt
e

r 
E

a
rly

 P
le

is
to

ce
n

e 
C

o
sm

o
ge

n
ic

 a
ge

: 
1.

8
 ±

0
.1

 M
a 

  
G

ra
f, 

20
09

a;
 D

ie
le

m
an

 e
t a

l.,
 2

02
2 

28
 

  

R
eu

ss
/L

in
th

- 
R

h
e

in
/R

h
e

in
 

B
e

rin
ge

n
 g

la
ci

a
tio

n 
M

IS
 6

 
IR

S
L

 d
a

te
s 

(~
1

8
5

 k
a

) 
a

t 
K

le
tt

ga
u 

O
S

L 
da

te
s 

fr
om

 1
5

9±
8 

ka
 t

o 
20

5±
12

 a
t 

R
in

ik
er

fe
ld

 
  

G
ra

f, 
20

09
b;

 K
el

le
r &

 K
ra

ys
s,

 2
01

1,
 P

re
us

se
r e

t 
al

., 
20

11
; D

eh
ne

rt 
et

 a
l.,

 2
01

0,
 2

01
2;

 L
ow

ic
k 

et
 

al
., 

20
15

; B
ue

ch
i e

t a
l.,

 2
01

7;
 S

ch
lü

ch
te

r e
t a

l.,
 

20
20

; D
ie

le
m

an
 e

t a
l.,

 2
02

2;
 G

eg
g 

et
 a

l.,
 2

02
2 

H
a

ge
n

h
o

lz
 g

la
ci

a
tio

n 
M

id
d

le
 P

le
is

to
ce

ne
 

  
  

H
a

b
sb

u
rg

 g
la

ci
a

tio
n 

M
id

d
le

 P
le

is
to

ce
ne

 
  

  

M
ö

h
lin

 g
la

ci
a

tio
n 

M
id

d
le

 P
le

is
to

ce
ne

 
C

o
sm

o
ge

n
ic

 a
ge

: 
0.

5
 ±

0
.1

 M
a 

  

R
h

e
in

/ 
L

in
th

-R
h

ei
n

 
Ir

ch
e

l D
e

ck
en

sc
h

ot
te

r 
E

a
rly

 P
le

is
to

ce
n

e 
C

o
sm

o
ge

n
ic

 a
ge

s:
 2

.6
 -

 0
.9

 M
a 

  
C

la
ud

e 
et

 a
l.,

 2
01

9;
 K

nu
ds

en
 e

t a
l.,

 2
02

0;
 

D
ie

le
m

an
 e

t a
l.,

 2
02

2a
 

m
am

m
a

l f
o

ss
ils

: 2
.6

 -
 1

.8
 M

a 
(M

N
 1

7
) 

  
Bo

llig
er

 e
t a

l.,
 1

99
6 

R
e

u
s

s
/ 

L
in

th
-R

h
ei

n
 

Ib
e

rig
 D

e
ck

e
n

sc
ho

tte
r 

E
a

rly
 P

le
is

to
ce

n
e 

C
o

sm
o

ge
n

ic
 a

ge
: 

1.
3

 -
 0

.7
 M

a 
  

G
ris

ch
ot

t e
t a

l.,
 2

02
0;

  
Kn

ud
se

n 
et

 a
l.,

 2
02

0 
T

ro
m

sb
e

rg
 D

e
ck

en
sc

ho
tt

e
r 

E
a

rly
 P

le
is

to
ce

n
e 

 
C

o
sm

o
ge

n
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The Early and Middle Pleistocene glaciations in the Alps  

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should be applied with local significance, not being suit-
able for the whole Alpine range. As the LGM can be 
considered a major one, the paleoclimatic setting that 
produced such an ice extent can be assumed also for 
the other large glacier extents in the Alps. Nevertheless, 
favorable microclimate conditions can promote local 
glacier advances in periods not necessarily in tune with 
the cold stages (Gribenski et al., 2021). Considering the 
Ivrea-Verbano area, available data show that six glacier 
advances took place in the Middle Pleistocene (Bini, 
2012; Gianotti et al., 2015, Tab. 1) as related to the 
stratigraphy of the foreland (Scardia et al., 2012; Gar-
zanti et al., 2011), almost every cold stage could have 
here a preserved sedimentary signature. This can be 
related to the high elevation accumulation area (and in 
addition, located very close to the piedmont area in the 
case of the Ivrea Amphitheatre), which is able to host a 
large valley glacier and a powerful piedmont lobe when 
climate became cold enough to force a lowering of the 
ELA. On the northern side, the other major ice domes 
(Rhine and Engadine; Florineth & Schlüchter, 2000; 
Kelly et al., 2004) promoted four major glacier advances 
in the Swiss foreland during the Middle Pleistocene 
(Preusser et al., 2011); in this framework, the Beringen 
glaciation was dated to MIS 6 (Lowick et al., 2015; 
Buechi et al., 2017) and the Möhlin glaciation to MIS 12 
(Gaar & Preusser, 2017; Preusser et al., 2021; Diele-
man et al., 2022). These sectors have high accumula-
tion areas fed both by westerly and southerly circulation 
and can develop large glaciers in both configurations.  

On the other side, in the northeastern Alps the 
larger extent is related to the Riss with overflow of Enns 
glacier into weakly glaciated catchments (van Husen, 
2000); this phase is ascribed to MIS 6 (van Husen, 
2000; van Husen & Reitner, 2011a). Same processes 
are likely for the Mindel (MIS 12) glaciation, where pre-
served moraines and related glacigenic deposits in Aus-
tria and southeastern Bavaria are even more distal from 
the Alpine front. In the southeastern side (Piave, Taglia-
mento and Soča catchments), all the morainic amphi-
theaters show MIS 6 deposits slightly outside the LGM 
(Venzo, 1977; Monegato et al., 2010; Rossato et al., 
2013). No more external glacial deposits have been 
observed, thus indicating that MIS 6 bore the largest 
configuration in the sector.  

The longitudinal extremes (French side and east-
ern Austrian sector) show only one Middle Pleistocene 
glacial unit (Tab. 1 and Fig. 9) larger than LGM. Consi-
dering that in the Western Alps glacier growth is favored 
by westerly circulation, while the Eastern Alps are domi-
nantly fed by southerly storm tracks, these units can 
testify to different cold stages of the Middle Pleistocene. 

The Garda and Adda systems, which are fed by 
the largest mountain catchments of the southern side of 
the Alps, show three major units in the Middle Pleisto-
cene, besides the LGM and the late Matuyama 
(Cremaschi, 1987; Bini, 2012). Considering their size, 
these systems need mostly southerly circulation for the 
expansion of the glacier network and formation of a 
piedmont lobe. In this perspective, apparently only three 
times in the Middle Pleistocene was the circulation com-
parable to the LGM, possibly in phase with the large 

extents of the boreal ice sheets (Batchelor et al., 2019) 
and especially to the Laurentide Ice Sheet, whose to-
pography forced the polar front to the mid latitudes and 
the storm track into the Mediterranean (Beghin et al., 
2015; Del Gobbo et al., 2022).  

 
8. CONCLUSIONS 

 
The nearly 200 years of research on Alpine glacia-

tions has shown that the Alps hosted extensive glacia-
tions in correspondence of several Pleistocene cold 
stages and likely smaller valley glaciers during the minor 
climate deteriorations. Thanks to the stratigraphic and 
geochronological data accumulated in the last decades, 
new insights have been provided for depicting the Early 
Pleistocene glaciations, whose extent was previously 
hypothetical, but now, especially in the northern fore-
land, their record is continuously updated.  

The onset of glaciations since the late Matuyama 
(MIS 22-20) is better recognized in many end moraine 
systems in the southern side of the Alps and correlating 
with foreland core stratigraphy. The updated chronology 
of the Middle Pleistocene phases indicates it is likely 
that every sector has had its own most extensive glacia-
tion in a different time span. The dissimilar architecture 
of the glacigenic units at the outlet of the major Alpine 
catchments points to a different behavior of the glaciers 
depending on global paleoclimate configuration, which 
was likely dissimilar from one stage to the other. Moreo-
ver, in the large accumulation areas of the Central Alps 
(Adige, Adda and Inn) the development of an extensive 
interconnected glacier network with associated piedmont 
lobes required abundant snow supply also from the 
southerly circulation, which was promoted by the large 
extent of the Laurentide Ice Sheet. In the higher accu-
mulation areas (Valais, Dora Baltea, Rhine-Reuss and 
Ticino-Toce) a larger number of glacial units was record-
ed probably because a small ELA lowering in these 
catchments could lead to glacier advance.  

Finally, the Alps remain the most studied mountain 
range for reconstructing extents of Quaternary glaciers 
and testing new methods and models. The long lasting 
studies are a treasure to preserve and a motivation for 
even better depicting the climatic and geomorphological 
evolution of the highest mountain environment of central 
Europe. 

 
ACKNOWLEDGEMENTS 

We want to thank the reviewers G. Orombelli and 
L. Gegg, whose suggestions greatly improved our man-
uscript. We also thank A. Fontana (A.E.) for his com-
ments. 

 
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Ms. received: February 28, 2023 Revised: May 4, 2023 
Accepted: May 8, 2023  Available online: May 22, 2023