GEOCHRONOMETRIA 31 (2008), pp 31-37
DOI 10.2478/v10003-008-0014-9
Available online at
versita.metapress.com and www.geochronometria.pl
PLEISTOCENE STRATIGRAPHY OF POLAND AND ITS CORRELATION
WITH STRATOTYPE SECTIONS IN THE VOLHYNIAN UPLAND
(UKRAINE)
LESZEK LINDNER and LESZEK MARKS
Institute of Geology, University of Warsaw
Żwirki i Wigury 93, 02-089 Warsaw
Received 10 January 2008 Accepted 08 February 2008
Abstract: Recent stratigraphic subdivision of the Pleistocene of Poland presents 4 complexes: Pre-
glacial, South-Polish, Middle-Polish and North-Polish ones. Each complex comprises a set of strati-
graphic units, corresponding to the previously distinguished 8 glaciations/coolings and 7 intergla-
cials/warmings. Three younger complexes and corresponding extents of Scandinavian ice sheets in
Poland are described in more detail. Three older interglacials in Poland (Augustovian, Kozi Grzbiet
and Ferdynandovian) are characteristic for their bi-optimal climatic sequences but so far, they have no
equivalents in loess sections of the Volhynian Upland in the Ukraine. Coolings between the optima of
these interglacials are occasionally considered as small glaciations, during which the ice sheet could
occupy only a northern part of Poland. All younger interglacials are mono-optimal in Poland and as
such, they are also reflected by single palaeosols in loess sections of both countries. Till occurrences
in key loess sections of Poland and Ukraine enabled precise delimitation of ice sheet extents, espe-
cially within the Middle-Polish Complex with the glaciations Liwiecian, Krznanian and Odranian as-
cribed to OIS 10, 8 and 6, respectively. During the youngest (Vistulian, Valdai) Glaciation, 3-4 loess
deposits were formed in the Lublin and Volhynian Uplands; they are separated by palaeosols that de-
veloped during interstadial-rank warmings.
Keywords: complexes, interglacials, glaciations, stratotype sections, loess, palaeosols, Pleistocene,
Poland, Ukraine.
1. INTRODUCTION Bogucki et al., 1995; Szełkoplyas et al., 1985;
Szełkoplyas and Christoforowa, 1987). They contain tills
(Bojanice) as well as loess deposits and separating pa-
Pleistocene glaciations and interglacials distinguished
in the territory of Poland are the principal units of the laeosols (Bojanice, Korshiv) that were correlated with the
stratigraphic subdivision of the glacial part of the Quater- Pleistocene main stratigraphic units in western and mid-
nary in Poland (1.4-0.01 Ma). Limits of some of these eastern Europe (among others Lindner et al., 1998; Lind-
glaciations (Sanian 1, Sanian 2, Odranian and Vistulian in ner and Marciniak, 1998).
Recent proposal of an updated stratigraphic time table
Fig. 1) are expressed by glacial landforms and sediments,
whereas the others (Narevian, Nidanian, Liwiecian and of the Pleistocene of Poland (Ber et al., 2007a, b) pre-
Krznanian in Fig. 2) are represented by buried deposits, sents 4 complexes, namely Preglacial, South-Polish,
Middle-Polish and North Polish ones. Each complex
overlain by younger glacial series. All glaciations and
interglacials are correlated with reliable Middle and Late comprises a set of stratigraphic units, including the previ-
Pleistocene stratigraphic horizons in the stratotype sec- ously distinguished glaciations/coolings and intergla-
cials/warmings (Fig. 2).
tions Bojanice and Korshiv in the Volhynian Upland
(Figs 1, 3). These sections have been examined for al- The paper is a short description of three younger com-
most 30 years (among others Boguckij et al., 1980; plexes, with their glaciations and interglacials, correlated
with main units (horizons) of the stratigraphic subdivi-
sion of the Pleistocene in the Volhynian Upland in the
Corresponding author: L. Lindner
Ukraine (Fig. 3). Besides, maximum limits of Scandina-
e-mail: l.lindner@uw.edu.pl
ISSN 1897-1695 (online), 1733-8387 (print) 2008 GADAM Centre,
Institute of Physics, Silesian University of Technology.
All rights reserved.
PLEISTOCENE STRATIGRAPHY OF POLAND AND ITS CORRELATION WITH STRATOTYPE SECTIONS&
During the Augustovian Interglacial (Fig. 2), previ-
ously known as the Podlasie Interglacial, a vast lake was
formed in northern part of the present Biebrza Basin (near
Augustów in north-eastern Poland). Organic sediments of
this lake were examined in several borehole sections
(Ber, 2000) and document a bi-optimal floristic succes-
sion (among others Janczyk-Kopikowa, 1996; Marciniak
and Winter, 2003; Lisicki and Winter, 2004), different
from the younger interglacials in Poland due to the ab-
sence of fir (Abies) and hornbeam (Carpinus) in the lower
optimum. Bi-optimal succession of this interglacial is
13 18
also supported by isotope analysis of C and O by
Jędrysek (Ber, 2000). Deposits at the setting of this inter-
glacial from the section Kijewice (northern Mazovia)
were TL dated at 890-820 ka (Bałuk, 1991). In the Carpa-
thians, the age of the fluvial sediments of this interglacial,
comprising reverse magnetic polarisation (Matuyama
Epoch), was TL dated at 749ą112 ka (Butrym and
Zuchiewicz, 1985).
During Nidanian Glaciation (Fig. 2) the Scandina-
vian ice sheet occupied not only Central Poland but
spreading along the Sudetes, it reached the Moravian
Gate and western foreland of the Carpathians. Its pres-
ence, indicated by a till at Kończyce (Oświęcim Basin)
seems to be supported by palaeomagnetic examination
that determined the setting of the Bruhnes/Matuyama
boundary (778 ka) in the overlying interglacial deposits
Fig. 1. Limits of main Scandinavian glaciations in eastern Poland and
(Wójcik et al., 2004). The front of the ice sheet along the
neighbouring countries and location of the stratotype sites Bojanice
and Korshiv. northern edge of the Małopolska and Lublin uplands
dammed the rivers flowing to the north, what resulted in
development of proglacial lakes. Anaglacial part of his
glaciation is connected with deposition of the oldest sub-
vian ice sheets (cf. Marks, 2004a) in eastern Poland,
western Belarus and Ukraine are presented (Fig. 1). Dur- till loess in Poland, particularly well preserved on slopes
of buried fluvial valleys in the western part of the Holy
ing the last few years the distinguished stratigraphic units
Cross Region (Lindner, 1991).
of the South-Polish Complex, have been supported by
During the Kozi Grzbiet (Domuraty) Interglacial
numerous new key sites and therefore, more detailed
(Fig. 2), an exceptionally rich accumulation of fauna
palaeogeographic and palaeobotanic evidence is available
remains formed in the cave Kozi Grzbiet in the Holy
(Janczyk-Kopikowa, 1996; Winter, 2001; Marciniak and
Cross Region. These remains, comprising abundant bones
Winter, 2003; Pidek, 2003; Lisicki and Winter, 2004;
and teeth of mammals, amphibians, reptiles and also
Wójcik et al., 2004). Such approach enabled to delimit
shells of terrestrial snails, represent a bi-optimal warming
extents both of older and younger glaciations. On the
that corresponds to the Dutch Cromer II. The Brun-
other hand, analysis of till occurrences in stratotype loess
hes/Matuyama palaeomagnetic boundary preserved in
sections of Poland and Ukraine (Lindner et al., 2004)
cave deposits (Głazek et al., 1977), enabled their correla-
founded the basis to delimit Scandinavian glaciations
tion with OIS 19. These cave deposits are presumably of
within the Middle-Polish Complex (Lindner, 2005). In
the same age as lake sediments in the southern part of the
this very case, it concerns particularly Liwiecian and
present Biebrza Basin in north-eastern Poland, among
Krznanian glaciations (corresponding to OIS 10 and 8,
others at Domuraty. They represent (Lisicki and Winter,
respectively), but also the Odranian Glaciation, together
with its recession Warta, Wkra and Mława stades corre- 2004) a bi-optimal floristic succession, younger than the
one of the Augustovian Interglacial and different by its
sponding to OIS 6.
co-occurrence of hornbeam (Carpinus) and fir (Abies)
during the second optimum, as well as presence of ash
2. SOUTH-POLISH COMPLEX
(Fraxinus) during the mid-interglacial cooling. The above
mentioned interglacial lake sediments from the section
The Narevian Glaciation is the oldest unit of this
Kończyce (Wójcik et al., 2004) are presumably of the
complex (Fig. 2). The Scandinavian ice sheet invaded
same age.
northern Poland, slightly more southwards to the west
During the Sanian 1 Glaciation (Fig. 2) the Scandi-
than presented previously (cf. Lindner and Marks, 1995).
navian ice sheet occupied the largest area of Poland. It
In the west it reached the Lower Odra and Middle Noteć
reached both the Sudetes and the Carpathians (Fig. 1),
valleys and in the east, it occupied a northern part of the
invading them with immense lobes that used the river
Radom Plain and Lublin Upland. In mid-western Poland
valleys open to the north, among them the Upper Odra
a distinct proglacial outflow system was developed
valley in the Moravian Gate (Lindner, 2001). In its mar-
whereas vast ice-dam lakes occurred in eastern Poland.
32
L. Lindner and L. Marks
Fig. 2. Stratigraphic subdivision of the Quaternary of Poland and its correlation with eastern Europe, after Ber et al. (2007a, b), supplemented.
ginal part the ice sheet moved around high-elevated area (Pidek, 2003). TL dating suggest the age limits of this
(main ranges of the Holy Cross Mountains, Polish Jura, interglacial from 543ą65 ka to 522ą63 ka (Rzechowski,
Ślęża), favouring development of abundant nunataks. The 1996). In the Volhynian Upland this interglacial corre-
next sub-till loess was also deposited, preserved at pre- sponds presumably to fluvial(?) erosion and accumula-
sent in western and southern parts of the Holy Cross tion, recorded in the section Bojanice (Fig. 3) and repre-
Region (Lindner, 1991) and recently found also in the sented by sands with gravels and sands above the oldest
Lublin Upland near Hrubieszów (Dolecki, 2002). In the loess horizon. It can also correspond to the Lubny (Solot-
neighbouring Dubienka Basin to the north of Hrubi- vin) palaeosol horizon (Boguckyj and Aanczont, 2002).
eszów, there are corresponding (TL age 680-620 ka) lake The Sanian 2 Glaciation (Fig. 2) is the youngest
sediments, containing mostly aeolian material, presuma- stratigraphic unit of the South-Polish Complex. During
bly being an aquatic facies of loess (Dolecki, 2002). This this glaciation the Scandinavian ice sheet, after advance
loess in Poland probably corresponds to the oldest loess around the Holy Cross Mountains and occupation of the
in the Volhynian Upland (Lindner et al., 1998), preserved Lublin Upland, entered the Sandomierz Basin (Fig. 1); it
in the section Bojanice (Fig. 3) and defined as the Don reached also the north-eastern slopes of the Sudetes.
(Sula) horizon. Similarly as during the preceding glaciation, the highest
The Ferdynandovian Interglacial (Fig. 2) is also ranges of the Holy Cross Mts and some intermontane
expressed by a bi-optimal climatic succession (Janczyk- basins formed the nunataks. At the edge of the Carpathi-
Kopikowa, 1991); it is characteristic for presence of ans a latitudinal marginal valley was formed: it collected
hornbeam (Carpinus) but in the second optimum only. proglacial and extraglacial waters and drained them to the
Diatomologic investigations of lake sediments in the Dniester drainage basin. In the Holy Cross Region ice
territory of Poland evaluated water level changes (Mar- sheet advance was preceded by deposition of a sub-till
ciniak and Lindner, 2003). A mid-interglacial cooling is loess (Lindner, 1991). The loess in a similar geologic
considered for a small glaciation, during which the Scan- setting was also noted near Hrubieszów in the Lublin
dinavian ice sheet reached the northern part of Poland Upland (Dolecki, 2002). The corresponding loessy-like
33
PLEISTOCENE STRATIGRAPHY OF POLAND AND ITS CORRELATION WITH STRATOTYPE SECTIONS&
fluvial sediments with Holstein-type fauna at Serniki at
440-400 ka. Bones of a cave bear from the same interval
are known from a karst section at Draby near Działoszyn,
dated by FCl/P and collagen method at 440-320 ka
(Głazek et al., 1976). The Mazovian Interglacial in loess
sections is represented by palaeosols, noted both in bore-
holes and exposures in the Lublin Upland (Dolecki
2002). In the Volhynian Upland it is represented by a
palaeosol of the Sokal (Zavadivka) horizon, noted in the
sections Bojanice and Korshiv (Fig. 3).
The Liwiecian Glaciation (Fig. 2) is represented by a
till that delimits ice sheet extent in north-eastern and mid-
eastern Poland. A vast proglacial lake was formed by
damming the Vistula valley and its tributaries to the south
of Warsaw. In the section Zbójno near Przedbórz, sedi-
ments of this lake were TL dated at 388 ka (Lindner and
Brykczyńska, 1980). In western Poland two latitudinal
valley systems were formed (based on relic network from
the preceding interglacial) that drained proglacial and
extraglacial waters westwards, to the Elbe drainage basin.
Similar system but to east was directed to the Pripyat
drainage basin. During the anaglacial part of the Li-
wiecian Glaciation, deposition of the oldest supra-till
loess deposits in the Lublin Upland occurred (Ma-
ruszczak, 1991; Dolecki, 2002). In the section Nieledew
they are bracketed by TL dates from 367.8 ka to 351 ka.
In the Volhynian Upland these loess deposits correspond
Fig. 3. Stratigraphic setting and thermoluminescence age of Pleisto-
to the loess of the horizon Orel (with a thin chernozem at
cene deposits in sites Bojanice and Korshiv, after Lindner et al. (1998),
the bottom), preserved in the section Bojanice, and possi-
updated.
bly also to a thin layer of sand in the section Korshiv
1 Cretaceous marls; 2 till; 3 sands with gravels; 4 sands;
(Fig. 3).
5 loess; 6 illuvial horizons (B) of interglacial forest soils; 7 cher-
The Zbójnian Interglacial (Fig. 2) is indicated by
nozems; 8 interstadial tundra soils; 9 soliflucted deposits; age TL in
ka after Butrym (Bogucki et al., 1995; Szełkoplyas et al., 1985), in lake-boggy deposits known from several key sections in
brackets after Shelkoplyas (Szełkoplyas et al., 1985; Szełkoplyas and
Poland. In the section Zbójno near Przedbórz a paly-
Christoforowa, 1987).
nologic succesion records palaeoclimatic conditions,
expressed firstly by exceptionally large participation (to
48%) of linden (Tilia), with abundant hornbeam
loams in the Carpathians were TL dated at 476ą71 ka (Carpinus), alder (Alnus) and hazel (Corylus) during
(Butrym and Zuchiewicz, 1985) and at the section climatic optimum (Lindner and Brykczyńska, 1980). TL
Załubińcze they comprised the palaeomagnetic episode age of these deposits is less than 388 ka and older than
Empereur (Nawrocki and Wójcik, 1995). In the section 236 ka (Lindner and Marciniak, 1998). Fluvial sediments
Korshiv and the second (from the bottom) loess in the of the Zbójnian Interglacial were TL dated in the section
section Bojanice they correspond to the oldest loess Wąchock near Starachowice at 352 ka (Lindner and
(Fig. 3). This horizon Tiligul is referred, together with the Prószyński, 1979). This interglacial is also indicated by a
overlying till, to the Oka Glaciation (Lindner et al., palaeosol in the loess sections of the Lublin Upland (Ma-
1998). ruszczak, 1991; Dolecki, 2002). In the section Nieledew
this interglacial is represented by a palaeosol, developed
3. MIDDLE-POLISH COMPLEX on the oldest supra-till loess, TL dated at 367 ka and
overlain by the lowermost older loess, TL dated at
300 ka. In the Volhynian Upland this interglacial is repre-
The Mazovian Interglacial is the oldest unit of this
complex in Poland (Fig. 2) and it is represented by abun- sented by the mid-loessy palaeosol of the horizon Luck
dant sites with lake-boggy deposits that, basing on pa- (Potagaylivka), preserved both at Bojanice and at Korshiv
(Fig. 3).
laeobotanic analyses, determine climatic conditions of
During the Krznanian Glaciation (Fig. 2), previ-
this interval. Palynologic analyses indicate (among others
Krupiński, 2000) that the climatic optimum of this inter- ously treated as the pre-maximum stade of the Odranian
Glaciation (cf. Lindner and Marks, 1999; Lindner, 2005),
glacial is indicated by maximum development of oak
the Scandinavian ice sheet reached not only the foreland
(Quercus), elm (Ulmus), linden (Tilia), hazel (Corylus)
and hornbeam (Carpinus). On the other hand, diato- of the Małopolska and Lublin Uplands but also the Fore-
Sudetic Lowland. TL age of glacial deposits was deter-
mologic analyses (Marciniak, 1998) enable to examine
mined at 273 ka in the section Marianka on the Włodawa
the lake water level fluctuations. In the section Krępiec,
Elevation, whereas at 298 ka and 250 ka in the Sudetes
Lublin Upland, lake sediments of this interglacial were
and their foreland (Szponar, 1986). Traces of a proglacial
TL dated at 400-350 ka (Harasimiuk et al., 1988) and
34
L. Lindner and L. Marks
outflow to the west are best preserved in the westernmost cial were also found near Rewal in western Pomerania
foreland of the Sudetes. Loess of this interval (the so- (Krzyszkowski et al., 1999). Lake-boggy sediments of
called older lower loess) is preserved in several patches in the Eemian Interglacial are known from many sites in
south-eastern Poland (Lindner, 1991; Maruszczak, 1991) Poland. Their palynological analysis indicates that a cli-
and TL dated at 298-260 ka. The Carpathian loess (sec- matic optimum was predominated by deciduous forest
tion Załubińcze) of this glaciation comprises a palaeo- with climax of oak (Quercus), then hazel (Corylus), with
magnetic episode Chegan (Nawrocki and Wójcik, 1995). abundant elm (Ulmus) and linden (Tilia); the latter
In the Volhynian Upland this loess corresponds to the reached its climax later than hazel (among others Mama-
horizon Dnieper 1, preserved both at Bojanice as at Kor- kowa, 1989). Water level fluctuations in the Eemian lakes
shiv (Fig. 3). were recorded by diatomologic investigations, initiated
Palynology of the Lublinian (Lubavian) Interglacial already many years ago (among others Marciniak and
(Fig. 2) is represented by the site Losy near Lubawa, with Kowalski, 1978). In loess sections of southern Poland this
lake sediments containing incomplete floristic succession interglacial is indicated by the lower part of the soil com-
(eroded upper part of the section) and floristic image, plex of the type Nietulisko I (Jersak, 1973), determined
different from the Eemian Interglacial one by earlier by Maruszczak (1991) mainly as a forest brown and
entrance of linden (Tilia) than hazel (Corylus) and also by brown leached soil (GI1). According to him, basing on
presence of Azolla (Krupiński and Marks, 1986). Sedi- TL dating of the underlying and overlying loess deposits,
ments of this interglacial are bracketed by TL ages of this soil developed from 130-125 ka to 115-110 ka. In the
270 ka and 181 ka. In loess sections this interglacial is loess sections of Bojanice and Korshiv (Fig. 3), it corre-
indicated by a palaeosol of Tomaszów type (Jersak, sponds to the lower part of the Horokhiv (Pryluky) soil
1973), defined by Maruszczak (1991) as an interglacial complex. In caves of the Tatra Mts, carbonate speleo-
type soil (GI2), capped with an interstadial soil (Gi/GI2).
thems were formed, Th/U dated at 124+60 ka (Głazek,
-16
TL dating of the older and younger loess determine set-
1984).
ting of the described complex as younger than 255.8 ka
During the Vistulian Glaciation (Fig. 2) the Scandi-
and older than 221.3 ka. In the Volhynian Upland this
navian ice sheet reached its maximum extent during the
soil should correspond to the Korshiv soil complex (Kay-
so-called Main (Leszno-Poznań) Stadial. The ice sheet
daky), preserved both at Bojanice and Korshiv (Fig. 3).
occupied a predominant part of northern and central Po-
The Odranian Glaciation (Fig. 2) is the youngest
land (among others Marks, 1998, 2002), reaching Zielona
stratigraphic unit of the Middle-Polish Complex. During
Góra and Konin, but also an immense lobe came to the
this glaciation the Scandinavian ice sheet reached the
Płock Region (Fig. 1) where a vast ice-dam lake was
Sudetes, entered deeply into the Moravian Gate, ad-
formed, filling the Vistula Valley upstream as far as the
vanced to northern slopes of Małopolska (Polish Jura,
area of Warsaw. Further to the east, the ice sheet limit
Holy Cross Mts) and Lublin Uplands, and came to the
was smaller: it occupied Mazury and Suwałki lakelands
northern part of the Sandomierz Basin (Fig. 1). Similarly
reaching south to Nidzica, Kolno and Sztabin. Basing on
as during earlier glaciations, it resulted in development of
radiocarbon dating of organic deposits under the till of
ice-dam lakes in the valleys of Pilica, Vistula and Wieprz
the Main Stadial and analyses of varved clays, connected
rivers. Deglaciation resulted in development of well ex-
with ice sheet retreat, its standstill during the maximum
pressed rows of end moraines of the Warta Stade (previ-
of the Leszno Phase occurred at about 21 ka BP and dur-
ously Wartanian Glaciation), as well as of Wkra and
ing the Gardno Phase at about 14-13.8 ka BP (Marks,
Mławka stades (Lindner, 2005). In the anaglacial part of
2002). During the older pre-maximum Świecie Stadial of
this glaciation, deposition of the so-called older upper
this glaciation, dated at about 70-60 ka, the ice sheet was
loess occurred (Maruszczak, 1991) and continued later
more limited and occupied mostly north-eastern part of
during ice sheet recession of the Warta Stade (cf. Marks,
Poland (Wysota, 2002). In the southernmost part of the
2004b). TL age of this loess was determined in the sec-
extraglacial area in Poland, 2-3 loess horizons, defined by
tion Nieledew at 221.3 to 159.3 ka. In the Carpathian
Maruszczak (1991) as the younger loess, were deposited
(Załubińcze) and Małopolska (Odonów) sections the
during the anaglacial part of the Vistulian Glaciation. In
loess of this glaciation comprises a palaeomagnetic epi-
numerous sections of the Głubczyce Plateau, Małopolska
sode Jamaica (Nawrocki and Wójcik, 1995; Nawrocki
Upland, Lublin Upland and Carpathian Highlands these
and Siennicka-Chmielewska, 1996). In the Volhynian
loess deposits contain interstadial palaeosols. Basing
Upland the loess of the Dnieper 2 (Tyasmin) horizon was
mostly on TL dating,, these loess deposits were formed
deposited, preserved both at Bojanice and at Korshiv
from about 100 ka to about 15/12 ka (Maruszczak, 1991).
(Fig. 3).
Interstadial soils, preserved in Polish loess sections, de-
veloped during warmings at 80-75 ka, 55-50 ka and
4. NORTH-POLISH COMPLEX
32-28 ka. In the main loess sections of the Volhynian
Upland i.e. at Bojanice and Korshiv (Fig. 3), they corre-
The Eemian Interglacial (Fig. 2) is the oldest unit of
spond to loess and separating palaeosols of the Valdai
the North-Polish Complex. During this interglacial, a sea
loess horizon (Boguckij et al., 1980; Bogucki et al.,
ingression occurred in the present Lower Vistula Valley
1994). The oldest ones constitute presumably the upper
region, indicated by sediments of the so-called Tychnowy
part of the Horokhiv soil complex whereas the overlying
Sea, containing fauna remains, among which foraminifers
Dubno, Rowne and Krasilov soils can be the equivalents
and molluscs are the most important (among others Ma-
of interstadial warmings, recorded in Polish loess and
kowska, 1986). Marine sediments of the Eemian Intergla-
35
PLEISTOCENE STRATIGRAPHY OF POLAND AND ITS CORRELATION WITH STRATOTYPE SECTIONS&
Boguckyj A and Aanczont M, 2002. Loess stratigraphy in the Halyc
separating stadial advances during the Vistulian Glacia-
Prydnistrov ja region. Studia Geologica Polonica 119: 315-327.
tion in Poland.
Butrym J and Zuchiewicz W, 1985. Results of thermoluminescent
datings of Quaternary sediments from the Nowy Sącz Basin (West
5. FINAL REMARKS Carpathians). Przegląd Geologiczny 33(3): 126-136.
Dolecki L, 2002. Main profiles of the Neopleistocene loesses on the
Horodło Plateau-ridge and their lithological-stratigraphical inter-
Presented outline of stratigraphy of the Polish Pleisto-
pretation. Lublin, Wydawnictwo Uniwersytetu Marii Curie-
cene comprises its glacial part with 8 glaciations and
Skłodowskiej: 263pp.
Głazek J, 1984. First isotope datings of speleothems from Tatra caves
7 interglacials (cf. Lindner et al., 1995; Marks, 2000),
and their bearing on Pleistocene stratigraphy of the Tatra Mts.
grouped lately (cf. Ber et al., 2007a, b) into 3 complexes:
Przegląd Geologiczny 32(1): 39-43.
South-Polish, Middle-Polish and North-Polish ones. The
Głazek J, Sulimski A, Szynkiewicz A and Wysoczański-Minkowicz T,
new approach in the presented outline is firstly a com-
1976. Middle Pleistocene karst deposits with Ursus spelaeus at
Draby near Działoszyn, Central Poland. Acta Geologica Polonica
plete description of 2 oldest interglacials: Augustovian
26(3): 451-466.
and Kozi Grzbiet (Domuraty) and secondly, a presenta-
Głazek J, Kowalski K, Lindner L, Młynarski M, Stworzewicz E, Tu-
tion of the opinion on separation of the Krznanian Glacia-
chołka P and Wysoczański-Minkowicz T, 1977. Cave deposits at
tion as the older one than the Odranian Glaciation, the
Kozi Grzbiet (Holy Cross Mts, Central Poland) with vertebrate and
snail faunas of the Mindelian I/Mindelian II Interglacial and their
latter with 3 recessional stades (Warta, Wkra and
stratigraphic correlation. Proceedings 7th International Spe-
Mławka).
leological Congress, Sheffield: 211-214.
Harasimiuk M, Maruszczak H and Wojtanowicz J, 1988. Quaternary
ACKNOWLEDGEMENTS
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This approach was presented by the authors (Lindner
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and Marks, 2007) at the 14th Ukrainian-Polish Sympo-
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