Rekonstrukcja lobu płockiego w czasie ostatniego zlodowacenia:
Gespeichert in:
| 1. Verfasser: | |
|---|---|
| Format: | Buch |
| Sprache: | Polish |
| Veröffentlicht: |
Łódź
Łódzkie Towarzystwo Naukowe
2010
|
| Schriftenreihe: | Acta Geographica Lodziensia
96 |
| Schlagworte: | |
| Online-Zugang: | Inhaltsverzeichnis Abstract |
| Beschreibung: | Zsfassung in engl. Sprache u.d.T.: Reconstruction of the Płock lobe during the last glaciation Bibliogr. s. 147-161 |
| Beschreibung: | 171 s. Ill., Kt. 30 cm |
Internformat
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| 245 | 1 | 0 | |a Rekonstrukcja lobu płockiego w czasie ostatniego zlodowacenia |c Małgorzata Roman |
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| 490 | 1 | |a Acta Geographica Lodziensia |v 96 | |
| 500 | |a Zsfassung in engl. Sprache u.d.T.: Reconstruction of the Płock lobe during the last glaciation | ||
| 500 | |a Bibliogr. s. 147-161 | ||
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Datensatz im Suchindex
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| adam_text | TRESC
Zarys
tresei
_________.......................... 7
Wprowadzenie
9
Obszar badań
IO
Dotychczasowe poglądy dotyczące zdarzeń glacjalnych w ¡obie płockim.,
13
Cel i zakres pracy oraz uwagi dotyczące wybranych pojęć 1
6
Metody badań
17
Badania terenowe
.......... ........... 17
Badania laboratoryjne
22
Analiza archiwalnych materiałów geologicznych i kartograficznych
23
Prezentacja wyników badań i uwagi o przyjętej stratygrafii
24
Budowa geologiczna i rzeźba obszaru badań
27
Podłoże kenozoiku
___....... ......_.........................................____.......... .................. 27
Podłoże czwartorzędu
28
Miąższość czwartorzędu
37
Wykształcenie i stratygrafia plejstocenu
_____.......... .....___________........................................38
Podłoże osadów stadiału głównego zlodowacenia wisły
42
Rzeźba i powierzchniowa budowa geologiczna
43
Analiza sedymentologiczna i mezostrukturalna
........................... ................_____.................... 48
Stanowiska w strefach glacimarginalnych zaplecza LGM
48
Stanowiska Paruszewice i Otmianowo
_______..............____...............__________________ 48
Obszar testowy
Izbica
Kujawska
-
Pustynia
63
Stanowisko Piotrów
73
Stanowisko Korzeń Królewski
........... .................._____.............. ........ ............ 79
Budowa geologiczna i formowanie stref glacimarginalnych na zapleczu LCiM
84
Stanowiska w strefie maksymalnego zasięgu lądolodu
................. .......... 86
Stanowisko Przedecz
..................................._........................ .......................... 86
Stanowisko Mijakowo
...................................____................___............................. 90
Obszar testowy Kubłowo
................. .......................................... ................. 92
Maksymalny zasięg ostatniego lądolodu
........................____.........................._____..........98
Stanowiska wysoczyznowe
............................................................................._............_........100
Stanowisko Guźlin
..............................____.................................................. 100
Stanowiska Lisica, Kretki, Zawada Nowa, Gaj, Gole, Kowal i Rokicie
........................ 104
Interpretacja przewodnich cech budowy geologicznej wysoczyzn
.......______.......... ...... 110
Rekonstrukcja nasunięcia lobu płockiego
........_.................................................................................111
Liczba i wiek zdarzeń glacjalnych w lobie płockim..
..................................................... ......... 111
Dynamika nasunięcia lądolodu w lobie płockim
........................................___.....____..........___124
Kierunki ruchu lądolodu
.............................................................................................124
Prędkość napływu mas lodowych oraz warunki hydrologiczno-termiczne
w podłożu lądolodu
.........................____........................_............................................128
Kształt powierzchni i miąższość lądolodu
............... ..............._.......................... ............133
Lokalne uwarunkowania dynamiki lądolodu w lobie płockim
................................. 135
Podsumowanie i dyskusja
...........................................................____........................................ .....137
Wnioski..
.........................................-...............-.........................................................-........
Л45
Literatura
......................................._____.............................................................____147
Spis ilustracji
............................................._..........................___...........................................162
Summary
.................................................____......................................................164
Małgorzata Roman
RECONSTRUCTION
OF THE
PŁOCK
LOBE DURING THE LAST
GLACIATION
ABSTRACT
The study pertains the dynamics of the ice sheet, the age and chronology of glacial events in the
Płock
lobe during the Vistulian
(Weichselian)
Glaciation.
The issue of the presence of the last Scandinavian ice sheet within the
Płock
Basin has a long history and
so far, no agreement has been found as to the number, rank and age of advances as well as to the course of the last
glaciation.
Complex sedimentological research and luminescence age indices of deposits along with mezostructural analysis of glaciotec-
tonic deformations have been carried out in several-odd exposures. Detailed geological charting has been applied for glaciomarginal
zones, the last glacial maximum limit (LGM) and two belts of hillocky
landforms
apparent in the LGM hinterland, the Czamanin-
Otmianowo-Paraszewice (preLGM-1) and
Izbica
Kujawska-Pagórki Chodeckie-Szewo-Korzeń Królewski (preLGM-2).
Spatial
distribution of
subglacial
and ice-marginal
landforms
were analyzed on the basis of the digital elevation model (DTED2) and also
the relief and lithology of the
subglacial
surface has been reconstructed.
There is no evidence that the ice sheet advanced onto the
Płock
Basin vicinity during the Early and Middle Vistulian. It has been
proved that during the last
glaciation a
singular ice transgression had taken place in the area investigated, which had happened be¬
tween
22.9
and
18.7
ka BP. The event has been correlated with the
Poznan
(Brandenburg) Phase of the Main
Stadial
of the Vistulian
Glaciation.
The ice advance exceeded the earlier
Leszno
(Frankfurt) Phase, forming the short-lived
Płock
lobe and delineated the last
glacial maximum (LGM) in central Poland
(Korzecznik-Przedecz-Kubłowo-Walentowo-Kamienna-Antoniewo-Sokołów-Osiny-
Szczawin-Gąbin-Mijakowo-Goślice-Zągoty).
Dynamics of the
Płock
lobe were influenced by local conditions: topography,
subglacial
hydrology and ice base
thermies.
Transgression proceeded with brief standstills along terrain obstacles close to the preLGM-1 and preLGM-2 trains. Such transverse
trains, where so far believed to have been recession moraines; they represent, however, overridden push moraines (preLGM-l) or
a range of glaciomarginal fans among whom included were older,
pre-
Vistulian marginal forms (preLGM-2). It was also found that
such a transverse large-scale glacial lineation appeared as an effect of a rhythmical building of structures and forms at the front of the
fast moving ice sheet.
Ice sheet in the
Płock
lobe featured a warm base system. Only in the marginal part during the LGM the ice base was cold in
patches. Dominant in the mechanism of the ice movement, prior to the
subglacial
channel drainage build-up and stabilising the ice
front at the LGM line, was a basal sliding resulting in an apparent growth of ice speed and a pervasive
subglacial
deformation. It has
been proved that the ice travel geometry in the
Płock
lobe was of a fan character, typical for a distal part of a land-based ice stream.
A low ice thickness in the lobe (ca
100-300
m) and its flattened longitudinal profile is supportive to admit the lobe to have had an
outlet nature. Self-elaborated parameters for the dynamics and geometry of the ice masses inflow and palaeoglaciological ones admit
to accept as valid that the
Płock
lobe evolved at the end of the fast moving ice stream intensively fed from its hinterland. That dis¬
tinctive element of the LGM margin contour has featured the main ice flow artery in the distal part of the Vistula palaeo-ice stream.
Usefulness of kinetostratigraphy in palaeogeographic reconstruction of glacial events has been demonstrated.
INTRODUCTION
The main subject of investigations pertains
on area within the
Płock
lobe extent. The notion
of the
Płock
lobe introduced in geological lite¬
rature bySkompski
(1969)
refers to the terminal
part of the ice sheet that entered upon the decline
along the Vistula and reached up to the vicinity of
Płock
and
Gąbin,
and delineated the maximum of
the last
glaciation
in central Poland (Figs
1, 2).
It
met the
Gopło
lobe, along the
Głuszyńskie
Lake
meridian, embracing the area between Powidz,
Konin
and Sompolno
(Maik
1961;
Molewski
2007).
Both the lobes constituted a characteristic
element in the marginal configuration of the last
Scandinavian ice sheet, said to have been the Vis¬
tula lobe (Fig.
1).
Investigations have been carried
out over an expanse of
2 700
km2 comprising the
morainic plateau lying in substance within
4
me-
zoregions, the
Kujawy
Lakeland, the
Kutno
Plain,
the
Dobrzyń
Lakeland and the
Płońsk
Plateau,
also referred to as the
Płock
Plateau (Fig.
2).
The aim of this work was to determine the
number and chronology of glacial events, to re¬
construct the course of
glaciation,
finding the ice
dynamics in the
Płock
lobe, as well as indicating
local predispositions and, the time of its being. In
face of the stream theory of the nature of ice
sheets, essential was to find whether the
Płock
lobe constituted a stream terminal or whether it
only expressed a further and southbound inflow
of ice masses onto the relief-predisposed Vistula
palaeovalley.
Detailed investigative tasks concerned the:
-
reconstruction of palaeoenvironmental con¬
ditions for the making of glacial
landforms
and
sedimentation of Vistulian deposits;
164
-
spatial
analysis of
landforms
and geological
structure as related to a local palaeomorphology;
-
finding the extent and distribution of glaci-
otectonic phenomena compared to palaeorelief
elements and contemporary relief, as well as to
determine the age of deformations and vectors of
glaciotectonic transport;
-
reconstruction of ice flow directions and dis¬
tinguishing areas of a varied displacement dynam¬
ics;
-
defining age of the ice advance in the
Płock
lobe as based on lithostratigraphy, kinetostratigra-
phy and deposit age indices;
-
precise defining of the maximum extent of
the last advance of the
Płock
lobe.
The method used comprised field and labora¬
tory works, studies of archive cartographic and
geological materials and study works.
Field works were carried out at exposures in¬
cluding
7
key sites
(Guźlin, Korzeń Królewski,
Mijakowo, Otmianowo, Paruszewice, Przedecz,
Piotrów),
7
documentation sites
(Gaj, Gole, Kowal,
Kretki, Lisica, Rokicie, Zawada Nowa),
2
case
study areas
(Izbica
Kujawska-Pustynia, Kubłowo)
(Fig. 3)
and also detailed geological and geomor-
phological charting in select parts of the glaci-
omarginal zones that amounted to around
370
km2.
Lithofacial
deposit features and directional
elements mainly in tills and tiU-substratum sedi¬
ment tangential planes were investigated at expo¬
sures and glaciotectonic deformations were sub¬
mitted to mezostructural analysis.
Lithofacial
analysis served to define the
(sub)environment and conditions for deposit se¬
dimentation. The Miall and Rust code with the
Zieliński
(1995)
and Eyles
et al.
(1983)
mod¬
ifications along with the author s addenda was
used for describing
lithofacies
(Tab.
1).
Vector
element investigations concerned the definition of
glacial transport directions against till clast fabric,
lee end turns in the
subtili
boulder pavement,
orientation of striae on boulder tops and small
kinematic structures and also palaeocurrent direc¬
tions.
Glaciotectonic deformation investigations
concerned the style of deformation, the pressure
(transport) direction, dependencies of disturbance
occurrences versus palaeorelief and glacial land-
forms and also age of structures. The relative se¬
quence and structure generations were being de¬
fined and those were correlated with deformation
stages inducted by consecutive ice advances which
allowed for an isolation of kinetostratigraphic units
(cf. Berthelsen
1978;
Pedersen
1993;
Phil¬
lips
et al.
2001)
(Tab.
4).
Laboratory examinations of sediments in¬
cluded a grain size analysis, calcium carbonate
contents, quartz grain morphoscophy, petrography
of fine gravel fraction
(5—10
mm) in tills, palyno-
logical examinations of lake and bog deposits and
indication of deposit age indices by optically sti¬
mulated luminescence (OSL),
thermoluminescence
(TL)
and radiocarbon.
An analysis of cartographic and geological
materials from archives as well as a digital terrain
model DTED2 allowed for the making of maps for
palaeostractural surfaces and, particularly, for the
map for the relief and lithology of the Vistulian
substratum and also the making of the model of the
relief and geology of the
Izbica
Kujawska morainic
ridge. Moreover, in agreement with
Morawski
(2003,2005)
the spatial orientation of glacial linear
landforms (morpholineaments)
was analysed, aim¬
ing at the reconstruction of the ice flow direction.
A simplified
stratigraphie
division scheme
was identical with that applied for the elaboration
of the Detailed geological map of Poland in the
scale of
1:50 000
(Instrukcja...
2004).
For the
Quaternary, the division proposed by
Ber,
Lind¬
ner and Marks
(Ber et al.
2007;
Lindner,
Marks
2008;
Tabela...).
The Mojski s scheme
(Moj
ski
2005)
was used for the Vistulian
Glac¬
iation
(Fig.
6).
RESULTS AND DISCUSSION
Age of advance. Chronology of glacial
events in the
Płock
lobe has been hitherto
grounded mainly upon morphostratigraphic and
hthostratigraphic criteria pertaining the number of
tills, providing a direct record for the presence of
the ice sheet (Galon
1961, 1967;
Galon,
Roszkówna
1967;
Skompski
1969;
Domosławska-Baraniecka
1965;
Bara-
niecka 1989;Mojski
1984, 2005).
For mineral
deposits of the last
glaciation,
and mainly tills, in
the 80ties and 90ties of the 19th century, a number
of
thermoluminescence
(TL)
age indices have been
made
(Brykczyński
et al.
1987;
Klatkowa
1992;
Baraniecka
1993),
whose results gave
grounds to presume an invasion of the
Świecie
Stadial
ice sheet into the relief-predisposed
Płock
Basin area
(cf.
Marks
1988;
Mojski
1991,
1992;
Klatkowa
1992).
Wysota
(2002)
rules
165
out, against thorough Vistulian stratigraphy and
sedimentation environment investigations in the
southern part of the lower
Powiśle,
any possible
advance in the Early Vistulian
(115-75
ka BP). He
also indicates, the
Świecie
Stadial
advance at the
outset of the Middle Vistulian
(75-65
ka BP) could
have embraced the northern and central lower
Powiśle
at its highest, but not any further to the
South.
Brzeziński
(2007)
however, presupposes
the advance to have reached
Brześć Kujawski
and
thus the North of the
Płock
Basin valley decline.
That is denied by the author s new investigations at
Kublowo (Fig.
32),
where an undisturbed intergla-
cial-glacial sequence was documented comprising
in
a palynologie
record the Eemian
Interglacial,
Early Vistulian and a significant part of the Pleni-
vistulian, with a cold Schalkholtz swing corres¬
ponding to the
Świecie
Stadial, also
the Oerel
In¬
terstadial
and up to the second Plenivistulian
stadi¬
al
(Tab.
2).
Fito-climatic relations determined as
against vegetation development of that profile,
show that at the
Płock
Basin area distant from the
Kubłowo
site, there was no ice sheet either at the
Early (MIS 5a-d) or the Middle Vistulian (MIS
3).
In the light of the above, the subject ice sheet ad¬
vance reconstruction delineating the LGM in cen¬
tral Poland pertain glacial event(s) which inter-
played in MIS
2,
perceived as the Main
Stadial
of
the Vistulian
Glaciation
(Moj
ski
1984, 2005;
Lindner
1992),
the Late Vistulian (Wysota
2002)
or the Upper Plenivistulian
(Kozarski
1991b;
Klatkowa
1996b; Turkowska
2006)
(Fig.
6).
Number and age of glacial events.
In the Vistulian
Glaciation
Main
Stadial
(Late
Vistulian/Upper Plenivistulian) plausible are one or
two glacial episodes at the
Płock
lobe (vide Fig.
45)
which are being ranked to phases and are re¬
ferred to the
Leszno,
possibly
Poznań
advances, or
they are being admitted to be
a Gąbin
and
Płock
Subphases
within the younger
Poznan
Phase. The
problem was bound with views on the number of
Vistulian tills and the importance in the transgres-
sive/recessive character of glaciomarginal zones to
be found in the LGM hinterland of the
Płock
lobe.
In the southeastern
Kujawy
Lakeland the
zones make a transverse glacial megalineation
expressed by ranges of a hilly morainic plateau: the
northern, running henceforth the southern limits of
the
Głuszyńskie
Lake throw Czamanin
-
Boniewo
-
Otmianowo
-
Paruszewice and reaching
Chocen,
found to be preLGM-1, and the southern range
(preLGM-2), embracing the
Izbica
Kujawska
ridge, the Chodecz and Szewo hillocks, the
Piotrów
and
Korzeń Królewski
vicinities and as¬
sembly hills around Boryszewo on the eastern
Vistula bank (Fig.
15).
As shown by the author at several-odd sites
one basal till records the sedimentological Vistu¬
lian
Glaciation
advance at the
Płock
lobe. Its age as
against sand OSL dating beneath and above the till
lies between
22.9
and
18.7
ka BP (Tab.
5,
Fig.
39).
The result obtained corresponds well with the Last
Scandinavian ice sheet maximum in Poland as to
have been within
24-19
ka BP (Marks
2010),
although in the question under discourse of phase
age for the advance, there is no unequivocal an¬
swer. Upon OSL dating of glaciofluvial sands at
Pustynia-
1
and
Korzeń Królewski
sites (Figs
25,
29)
whose age varies within
18.7-18.0
ka BP and
are genetically connected with the underlying till,
and appearing as high in the hypsometric profile,
that by no means can they be correlated with their
younger, recessive Vistulian standstills, it is as-
sumable that both the sands and the till have been
deposited while the
Poznań
Phase advanced and
whose maximum is evaluated to be
18.4
ka BP
(Wysota
et al.
2008,2009).
To infer that a singular advance had taken
place in the
Płock
lobe is furthermore justified in
the kinetostratigraphic investigations carried out by
the author. Documented in a number of sites, gla-
ciotectonic structures were shown to be aggregated
with deformation stages evoked by advances from
defined vectors and correlated with tills having
been left over. Henceforth the two kinetostrati¬
graphic units, the Vistulian, the younger, manifests
itself by a progressive sequence. Such a sequence
combined from pro- and
subglacial
structures as
seen at the Otmianowo, Paruszewice, Jozefowo-1
(Izbica
Kujawska-Pustynia case study area),
Korzeń Królewski, Zawada Nowa
sites (Tab.
4)
proves a singular ice advance. Important for pa-
laeogeography and assessment of the ice dynamics
in the
Płock
lobe is, that the progressive sequence
pertains as well glaciomarginal zones allocated in
the LGM hinterland and hitherto perceived to be
morainic chains undergoing a general recession
(Galon,
Roszkówna
1967;
Roszko
1968;
Niewiarowski 1983a; Pasierbski
1984;
Moj
ski
2005).
Another, supplementary argu¬
ment, speaking for a singular advance of the last
ice sheet onto the area investigated is the system of
glacial morpholineaments, i.e. tunnel valleys and
eskers, making a collective body of orthogonal, i.e.
extensional, and sharp-angled, i.e. compressional,
entities (Fig.
41).
That order inherited after prima¬
ry cracking in the ice is legible and hence can be
associated with the singular advance
(cf.
Mo¬
rawski
2005).
166
The Kaliska
site
(Domosławska-
-Baraniecka
1965; Janczyk-Kopikowa
1965)
is unique for stratigraphy of the younger
part of the Quaternary of central Poland in which
only one till covers palynologically documented
Eemian
Interglacial
deposits. As the site lies in the
marginal part of the
Płock
lobe (Figs
8, 15)
undis¬
closed and discursive, were, however, palaeogeo-
graphic relations in the hinterland, inclusive of the
character and rank of the glaciomarginal zones.
Character of glaciomarginal zones.
Recognition of geological structure along with
sedimentological, mezostructural, lithopetrography
investigations and OSL datings of deposits in a
number of sites within glaciomarginal zones al¬
lowed for a making of models of how zones of the
LGM hinterland were being formed (Figs
22, 27)
and how they departed from hitherto accepted
schemes (Fig.
45).
Proved was, that the transverse
ranges of the hilly plateau in the LGM hinterland
are overridden end moraines. Ranges determined
as preLGM-1 and preLGM-2 were being formed
during short standstills of transgression along
transverse terrain obstacles. Deposited at that time
glaciomarginal sediments underwent distortion
resulting from
proglacial
compression, a conse¬
quent truncation beneath the moving ice, recog¬
nized in the zones examined, belong to two kineto-
stratigraphic units, the preVistulian and the Vistu-
lian. Older structures constitute the king-pin of the
Izbica
Kujawska morainic
ridge (Figs
24, 25),
and
hence it is to be accepted as a relict form trans¬
formed in the younger, Visrulian, morphogenetic
stage. Visrulian glaciotectonic structures constitute
together with their covering till a coherent kineto-
stratigraphic unit consisting in a progressive se¬
quence of deforming structures which in fact, is a
record of a singular
deformative
transgression
cycle
(cf. Berthelsen
1978;
Hart, Boulton
1991;
Van
der Wateren
1995;
Pedersen
1996).
Notable also is the absence of outwash
plains originating from glaciomarginal zones while
they were being formed. The results obtained allow
to negate earlier findings, mainly based on mor-
phostratigraphic criteria, treating of an oscillative-
recessive nature of the LGM hinterland zones ex¬
amined (i.a. Galon,
Roszkówna
1967;
Rosz-
ko
1968;
Niewiarowski 1983a; Pasierbski
1984;
Dylikowa, Olaczek
1984;
Mojski
2005).
The preLGM-1 zone, because its morphologi¬
cal rhythm and inner structure, was ascribed in
category of narrow multi-crested push moraines
regarded as the effect of a consequent ice advance
and propagation of
compressive
structures towards
the foreland (Bennett
2001).
That character of
marginal zones is ascribed to surging glaciers or is
referred to palaeo-ice streams (i.a. Croot
1987;
Evans,
Rea
1999;
Van
der Wateren
1981;
Zandstra
1981;
Kasprzak
1988;
Andrze-
jewski
2002).
The statement is substantial for
the assessment of the transgression dynamics that
has exceeded the push moraine belt (preLGM-1)
and again, curtly, its front halted at the transversely
oriented terrain obstacles in the preLGM-2 zone
(Fig.
27).
Moraine forming in that margin was
dynamic and short-lived which is testified by a low
glaciomarginal deposits thickness, usually thin
with only locally occurring
proglacial
sediments
and an absence of
subglacial
channels clearly
bound with the ridges.
Maximum extent of the last ice sheet in the
Płock
lobe possibly having been reached during
the
Poznań
Phase is sporadically noted as end mo¬
raines or clearly seen sedimentation edges (Figs
8,
9, 10, 11, 15).
Proglacial
glaciotectonic deforma¬
tions were found only in marginal forms far from
the lobe axis (Przedecz site, Fig.
30),
and the
course of the LGM line itself is fixed to local forel¬
and relief elements. In the zone between the
preLGM-2 line and a maximum ice limit extent no
intensive
subglacial
erosion has been found and
beneath the thin till cover preserved are preVistu¬
lian glacial relief forms, as around Rogozin
(Fig. 1
5),
with intact surfaces bearing traces of
periglacial transformation, e.g.
Lisica (Fig.
36).
Character of that marginal zone speaks for
al
low
ice thickness, a short time of formation with
a moderate and varying ice margin dynamics.
Moreover it is hypothetically feasible that the
movement mechanism and ice dynamics in the
margin was highly influenced by thermal condi¬
tions of the footwall which was cold in particular
patches. This resulted from a low thickness and
a shower ice flow which reduced friction heat re¬
sulting in an absence of thawing at the ice foot and
reciprocally retarded the motion. Those processes
effected in the reduction of erosion and
subglacial
deformation (i.a. Kleman
1994;
Marks
1994).
This allowed for a preservation of the surface from
before the advance, which is legible from the
Lisi¬
ca
and
Gaj
profile records (Fig.
37).
However, in
the
Gole
profile, on the till base a deforming bed is
seen and is dominated by ductile shear structures
(Fig.
37),
indicating warm basal conditions. It can
thus be claimed that the ice sheet terminal part
during the LGM was a mosaic of the two thermal
types.
To recapitulate, we can indicate that the last
stage of transgression was less dynamic proceeding
167
as if by inertia, when the ice sheet exceeded the
preLGM-2 line. Changes in dynamics and retard¬
ing of the ice sheet motion was certainly highly
influenced by the opening of the
subglacial
tunnel
drainage that took place just prior to the LGM.
Ice sheet dynamics in the
Płock
lobe. Lobes are a characteristic element of the
morphology of ice sheet terminal parts ending their
run on land. Usually they express a varied
glacia¬
tion
dynamics in response to topography, lithology
changes and hydrology of the base but can also
reflect the distal part much faster as related to the
neighboring ice masses of the stream in motion
(Krüger 1983;
Patterson
1997; Stockes,
Clark
2001;
Jennings
2006).
A number of
arguments of a geological nature was collected for
the
Płock
lobe in reference to dynamics which also
indicate that the lobe forming was related with the
termination of the stream perceived
sensu stricto
as a narrow artery of the accelerated ice in mo¬
tion
(Bentley
1987).
As against the analysis of glaciotectonic struc¬
tures, sedimentological records and geomorpholog-
ical evidence, ice flow vectors were reconstructed
for the
Płock
lobe (Figs
40, 41, 42).
We deter¬
mined that the spatial distribution for ice masses in
the lobe was fan-like, typical for the distal part of
the ice stream terminating on land and intensely
fed from its hinterland
(cf.
Stokes, Clarks
2001).
Geological indices for the fast displacement
of ice masses became, in that context, uniquely
significant and that, also was valid for analyzing the
relief and lithology of the base (Fig.
14)
together
with the assessment of hydrology and the
thermies
of the ice sheet footwall (Chapter
Prędkość...),
whose alterations substantiate the local differentia¬
tion of vectors and ice flow. It was documented
that the main component of the rapid ice motion in
the lobe was, at its outset, a basal sliding on a thin
water film (Fig.38). That, admittedly, was domi¬
nant until the ice body came to standstill at
preLGM-1, but along the axis of the
Płock
Basin
decline, possibly, even until preLGM-2.
The melt-out and decoupling till found at
Guźlin (Fig.
35)
is a further good proof for that. At
a further transgression the fast flow resulted from a
pervasive deformation beneath the ice documented
at a number of sites as boulder pavements with
flattened and striated clasts, ploughing marks and
numerous shear deformations in the footwall and
deforming till.
Theoretical results of surface shape and ice
thickness (Figs
43, 44)
prove that it had a flattened
longitudinal profile which is supportive to admit
the lobe to have had an outlet nature developed in
the distal part of the fast moving palaeo-ice stream
(cf.
Patterson
1997;
Stokes, Clark
2001);
but that, however, facilitated preserving of the older
pre-Vistulian morainic forms and retaining of the
preLGM-1 and preLGM-2 transverse linear forma¬
tions bound with the transgression.
Kasprzak
(2000, 2003)
has claimed that transverse glacial
lineation is an expression of longer standstills of
the ice front. However, in context of the short-lived
glacial event in the lobe, the nature of the overrid¬
den moraine belts and evidence for the fast ice
flow, we can claim the transverse phenomena to be
an effect of curt stoppages of the fast displacing ice
of a slender thickness impeded by local obstacles,
changing in hydrology and possibly basal lithology.
Essential in that respect, is an assumed significant
ice margin
depositive
yield conditioned by a prompt
supply of ice masses from the hinterland but with a
richer
subglacial
relief and also an easier material
intake from the base
(cf.
Alley
et al.
1997).
Role of the
Płock
lobe in the Vis¬
tula palaeo-ice stream dynamics. The
handicap in reconstructing lobes in Pleistocene ice
stream terminations appears from an inability to
provide a similitude to contemporaneous phenom¬
ena. Today s streams enter seas, hence there are no
examples of the marginal zones being formed by
terrestrial ice streams. Essential because of the
mechanism of streams, is the subsidence wastage
of ice masses at their fronts stimulating simultane¬
ously ice inflow from the hinterland, the drainage
zone. With water-terminated streams ice wastage is
primordially effected by calving, whereas in terres¬
trial streams by forming lobes below the Equilib¬
rium Line Altitude
(ELA)
i.e. ablation zone, where
the disappearance of ice proceeds mainly through
surface melting (Jania
1993;
Stokes, Clark
2001).
Palaeo-ice streams in their reconstructions
require considering creative
prédisposais
along
with local conditions and their life time. Presup¬
posed Scandinavian ice streaming along the Vis-
tulian maximum (Punkari
1997;
Boulton
et al.
2001b; Marks
2002,
2005a; Wysota
2002;
Morawski
2009)
is substantiated by a friendly
topographic situation, the existence of an Eemian
Sea bay and a consequent valley decline and sub¬
stratum properties that were unconsolidated and
mainly of a low permeability. A suitable relief
predisposed diversifying the main transport artery
of the southwestern part of the Scandinavian ice
sheet, the so-called Baltic ice stream, and generat¬
ing secondary streams
-
the
Odra (B2),
Vistula
(B3),
Mazury
(B4) and Lithuania (B5) which en¬
tered the area of today s Poland exploiting earlier
declines
(cf.
Marks
2002,
2005a) (Fig.
1).
Timing
168
for overriding the Baltic Basin and the last trans¬
gression onto the Central European Lowland was
estimated to be ca
22 000 BP (Rotnicki 2001)
as against radiocarbon deposit datings from the
bottom of the western Baltic
(22
780±660,
21
480±440 14C BP
-
Kramarska
1998)
and its
southern coastline
(22
30±700 14C BP
-
Rat¬
nički,
Borówka
1995
and
21
600Ü060
14C
BP
-
Krzyszkowski
et al.
1999).
After having
calibrated the data according to Fairbanks
(Fairbanks
et al.
2005)
the age obtained is re¬
spectively
27
351±771,
25
780±599,
26
786±846
and
25
896±1334
cal BP
which leads to the con¬
clusion that the advance of the last ice sheet onto
the area of today s Poland commenced no earlier
than the youngest date. Maximum extent of the ice
sheet in western Poland was reached in the
Leszno
Phase i.e. ca
22.3
ka BP as estimated by
Wysota
et al.
(2008, 2009)
on luminescence
datings of
intra
and
subtili
sediments. East of
Ko¬
nin
the LGM fell on the
Poznań
Phase, ca
18.4
ka
BP (Wysota
et al.
2008, 2009),
Marks
(2002,
2005a,
2010)
stressed the asynchronous maxi¬
mum extent of the last ice sheet in Poland with the
advance age in the
Leszno
Phase assumed as
24
ka
BP and the younger events of the
Poznań
Phase as
19-20
ka BP as he wrote in
2010
against calibrated
sub till deposit radiocarbon data and supported by
cosmogenic 10Be and 36C1 isotopes of erratics (left
over by the last advance). The proper,
sensu
Bentley
(1987)
Vistula palaeo-ice stream devel¬
oped below
ELA
whose height in the Central
European Lowland during
glaciations Brod-
zikowski
(1987)
estimated as
800-1000
m.
Considering the ice cover thickness during LGM
the hypothetic line between accumulation and
ablation for the last ice sheet should have run along
the Szczecin
-
Świecie
parallel. That is concordant
with the
0 °С
isotherm for the summer season indi¬
cated by
Kasprzak
(2003)
for the last ice sheet
maximum. Boulton
et al.
(2009),
on the other
hand, treats Poland s area as an entity allocated in
the ablation zone at the time of the last Vistulian
maximum.
The northern part of the ice artery in the B3
palaeo-ice stream was stable since the outset of the
last transgression and only the part south of the
Noteć
valley and the central part of the lower
Powiśle
underwent dynamic alterations with
a double fast episode of a spatially diversified ex¬
tent, which is to say, south of a hypothetical line up
to where recession came, following an older ad¬
vance in the
Leszno
Phase (Wysota
et al
2008,
2009).
The
Leszno
advance delineated the LGM
west of
Konin,
whereas along the Vistula line,
according to the authors cited, the ice sheet reached
at that time up to the
Nieszawa
vicinity (ca
15
km
north of the area investigated). As results from
investigations carried out by the author, the
Płock
lobe area during the
Leszno
Phase was free from
ice and the lobe itself developed only during the
Poznań
Phase which fits well the time-spatial gla¬
cial events scheme presented by Wysota
et al.
(Wysota, Molewski
2007;
Wysota
et al.
2008, 2009).
They stress that both advances in the
Vistula lobe featured a fast ice motion estimated as
250-300
m/year during the
Leszno
Phase and at
least
400-450
m/year during the
Poznań
Phase,
which, east of
Konin,
overrode the extent of the
older phase and delimitated the LGM. The vast
Vistula lobe made at that time in the periphery of
the Scandinavian ice sheet with a width of over
100
km lay at the end of the ice stream and bifur¬
cated onto two secondary lobes
-
Goplo and
Płock
(Molewski
2007;
Wysota
et al.
2009).
Data obtained by the author pertaining dynam¬
ics and ice sheet parameters in the
Płock
lobe sup¬
port the concept of where the area in the distal part
of the ice stream evolved along the Vistula line
was located. The present reconstruction of the
extent and palaeo-ice stream configuration (Fig.
42)
showed that during the
Poznań
advance the
main ice artery of the distal part of the Vistula lobe
was displaced from an N-S axis, dominant during
the older
Leszno
Phase and had a NW-SE heading
concordant with the Vistula palaeovalley axis
(Płock
lobe). Incidentally the N-S ice flow has
been retained in the
Gopło
lobe.
Reasons for the stream divergence and geo¬
metry changes for the ice flow are to be looked for
mainly in local palaeomorphology and the ice
sheet reaction to different hydrogeological condi¬
tions of the base and, presumably, also in the fast
frontal ice disintegration in the presence of a prog-
lacial lake existent in the
Płock
Basin depression.
The fast ice wastage intensified an inflow of ice
masses from the hinterland that was supportive of
the forming and retaining of the main artery of the
flow
(cf.
Stokes, Clark
2001;
Bennett
2003;
Greenwood, Clark
2009).
In the distal part of
the Vistula lobe a relatively most energetic ice flow
was shown along a route referring to the
Płock
lobe
axis. It is expressed by longitudinal
subglacial
megalinear
forms in the northern part of the
Ku¬
jawy
Plateau
(cf.
Molewski
2007)
which run
NWW-SEE and is further unveiled by a melt-out
and decoupling till at
Guźlin
examined by the au¬
thor in detail. Moreover, from the author s recon¬
struction of the geometry of ice flow directions in
the lobe (Figs
40,41)
based on direct evidence and
169
intermediary reconstructions according to
Mo¬
rawski
(2003, 2005),
it appears that the sug¬
gested distal ice flow made a lobe with a width of
70
km, visualized in a fan-like flow vector distribu¬
tion in the rapid displacement.
Evolution of the
Płock
and Goplo lobes was
synchronous, which is testified by a curt glacial
event of the
Poznań
advance, whereas, locally, in
marginal parts insignificant oscillatory moves of
the front could have taken place. Presumably
Skompski
(1969)
described two tills in the east¬
ern
Płock
lobe as correlated with the
Gąbin
and
Płock
subphases
-
following the afore mentioned
behaviour of the marginal ice sheet parts. The au¬
thor of this work has not encountered any evidence
reported by Skompski
(1969)
and the
Rokicie
site profile (Fig.
36)
located within the area of the
two alleged tills is typical for the formation of the
Late Vistulian plateau around
Siecień
and
Dobrzyń.
There are no new elaborated sites from
that area with OSL datings for
subtili
deposits.
Hence, significant seems to be the
Główina
profile,
a few kilometers east of
Dobrzyń
presented by
Wysota* who distinguished one Vistulian till above
OSL
-
dated sands and claimed them to be 31ka
BP old.
Remarks on the method used. Kine-
tostratigraphy was first used in the reconstruction
in the
Płock
lobe advance. Its application required
a combination of mezostractural analysis with
sedimentological investigations of tills and their
contact with footwall sediments. Finding conformi¬
ty of glacial and glaciotectonic transport vectors
became a foundation for further procedure i.e.
defining pro and
subglacial
domains, distinguish¬
ing recessive and progressive sequences along with
kinetostratigraphic units, corresponding to an ad¬
vance. The elaborated procedure initially con¬
cerned profiles of single sites and determining a
phenomena sequence and further their correlation
to relief and palaeogeography, substantiating the
spatial direction of glaciotectonic alterations. Dat¬
ing sediment underlying disturbed units facilitated
the definition of age for sediments that have un¬
dergone deforming as well as the time of when the
structures have come into being.
The use of kinetostratigraphy is worthy of un¬
derlining in defining particular sequences of glacial
events, and the more, in areas where multistage
sediment deformations have taken place and when
an application of hitherto used standard
stratigraph¬
ie
methods are tedious if not impossible, and in
case of morphostratigraphy, devious at times. Me¬
zostractural analysis that is consistent in investiga¬
tive proceedings for kinetostratigraphy had a sig¬
nificant interpretative valour in the examination of
the birth of glacial marginal forms and the dynam¬
ics of the
Płock
lobe.
Orientation and
vergence
of
compressive
structures allowed for a minute definition of glaci¬
otectonic transport vectors and also for an evalua¬
tion of the dynamic state in the margin in trans¬
gression.
In the reconstruction of the lobe advance par¬
ticularly stressed was the rendition of ice flow
directions (Chapter
Kierunki...)
(Roman 2007c,
2008a) and also delimiting areas of varied ice flow
speeds. The results obtained substantiate an offer
for the following reconstruction proceedings: stage
one
-
finding ice movement vectors
,
stage two
-
defining features of the ice displacement, inclusive
of
1 -
reconstructing of a spatial distribution,
2 -
connecting it with the ice sheet dynamics,
3 -
indi¬
cating vector differentiation reasons and speed,
4 —
providing a chronology for the inflow of ice
masses. The appliance of direct indices for the ice
flow and only supported by indirect methods is
essential for the procedure offered.
CONCLUSIONS
Numerous fresh data have been found from
complex investigations pertaining the advance of
the last Scandinavian ice sheet in the
Płock
lobe.
Those findings allow for a formulation of an
own concept of how the glaciomarginal zones were
formed, the ice sheet dynamics proceeded, con¬
firming other investigators views, as well as
rejecting some outdated ones. Presented below are
most significant conclusions from the
glaciation
synthesis.lt has been proved that within the
Płock
lobe in the Vistulian one only transgression had
taken place. The event was coincident with the
Main
Stadial
of the Vistulian
Glaciation
and de¬
termined the Last Glacial Maximum (LGM)
in central Poland. A clear record of the presence is
a single basal till and connected glaciotectonites,
*
the paper presented
27
November
2007
in Polish Geological Institute in Warsaw Chronology, extent and dynamics of the
Scandinavian ice sheet advances during Vistulian
Glaciation
in Poland , authors: W. Wysota, J. A. Piotrowski, A. S. Mur¬
ray,
M. D.
Batman
170
making together a coherent kinetostratigraphic
unit.
1.
Proved has been that the Vistulian kineto-
straigraphic unit both in the morainic plain and as
well as in glaciomarginal zones apparent in the
LGM hinterland comprises a progressive (trans-
gressive) sequence. That documented sequence is
expressed by a stockpiling of small
subglacial
shear deformations upon
proglacial
compression
structures and testifies a singular transgression.
2.
deposits beneath and above the till we de¬
termined the transgression to appear between
22.9
and
18.7
ka BP. Thus no explicit answer has been
found as to whether the last
glaciation
maximum in
the Vistula lobe fell within the
Leszno
Phase (ca
20.3
ka BP) or perhaps the
Poznań
one (ca
18.4
ka
BP). Considering the age and palaeomorphology of
the outwash sands resting above the till we found
the advance to have taken place within the
Poznań
Phase.
3.
As against
litho-
and kinetostratigraphic
investigations along with OSL datings of deposits,
we have proved that transverse trains of the hilly
morainic plateau in the LGM hinterland within the
Kujawy
Lakeland have
defacto
come into being
while the ice sheet transgressed, and not, as has so
far been believed, that they were strands of reces¬
sion moraines. They represent overridden push
moraines (preLGM-1 margin) or a range of glaci¬
omarginal fans among whom included were frag¬
ments of older,
pre-
Vistulian marginal forms
(preLGM-2). It was also found that such a trans¬
verse large-scale glacial lineation appeared as an
effect of a rhythmical building of structures and
forms at the front of the fast moving ice sheet.
4.
Basing on geomorphological and geologi¬
cal criteria we specifically stated the last glacial
maximum (LGM) limit in the
Płock
lobe (Kor-
zecznik
-
Przedecz
—
Kubłowo
-
Walentowo
-
Kamienna
-
Antoniewo
-
Sokołów
-
Osiny
-
Szczawin
-
Gąbin
-
Mijakowo
-
Goślice
-
Zągoty)
and also determined that the forming of
the LGM marginal zone was curt.
5.
On a large amount of sedimentological
proofs it is to be seen that the inflow of the ice
masses was swift, and probably at a tempo rated by
Wysota
et al.
(2008, 2009)
for the Vistula lobe in
the
Poznań
Phase, i.e. ca
400-500
metres yearly.
Ice sheet in the
Płock
lobe featured a warm base
system. Only in the marginal part during the LGM
the ice sheet base was cold in the patches. Domi¬
nant in the mechanism of the ice movement, prior
to the
subglacial
channel drainage build-up and
stabilising of the forehead at the LGM line, was
a basal sliding on a thin water film resulting in an
apparent growth of ice speed and a pervasive sub-
glacial deformation.
6.
It has been proved that the ice travel geo¬
metry in the
Płock
lobe was of a fan character,
typical for a distal part of a land-based ice stream.
Distribution, local flow directions and the dis¬
placement tempo of the ice masses were influenced
by topography,
subglacial
hydrology along with
the ice base
thermies. A
low ice thickness in the
lobe (ca
100-300
m) was also found.
7.
Self-elaborated parameters for the dynam¬
ics and geometry of the ice masses inflow and
palaeoglaciological ones admit to accept as valid
that the
Płock
lobe evolved at the end of the ice
stream intensively fed from its hinterland.
8.
Geological investigations in the LGM
zone bore fruits in documenting at
Kubłowo
the
longest in central Poland undisturbed Eemian-
Vistulian sequence, whose palynological record
comprises the Eemian
Interglacial,
Early Vistulian
and a significant part of the Plenivistulian, up to
the second Plenivistulian cold interval. Vegetal-
climatic relations determined by the development
of vegetation indicate the lack of an ice sheet in the
Early and Middle Vistulian in the
Płock
Basin.
9.
Usefulness of kinetostratigraphy in pa-
laeogeographic reconstruction of glacial events has
been demonstrated.
Reconstruction results contribute to a wide
current of research on the general model of ex¬
panding and the recession of the last Scandinavian
ice sheet in Europe. The author hopes the exem¬
plary ice lobe advance will forward further studies,
thus providing grounds for testing digital ice sheet
models as lately having been stipulated for Poland
(e.g. Hermanowski, Piotrowski
2009).
Translated by
Jerzy
Münnich
171
|
| any_adam_object | 1 |
| author | Roman, Małgorzata |
| author_facet | Roman, Małgorzata |
| author_role | aut |
| author_sort | Roman, Małgorzata |
| author_variant | m r mr |
| building | Verbundindex |
| bvnumber | BV039702315 |
| ctrlnum | (OCoLC)751154575 (DE-599)BVBBV039702315 |
| format | Book |
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| genre | (DE-588)4143413-4 Aufsatzsammlung gnd-content |
| genre_facet | Aufsatzsammlung |
| geographic | Płock Region (DE-588)4228597-5 gnd |
| geographic_facet | Płock Region |
| id | DE-604.BV039702315 |
| illustrated | Illustrated |
| indexdate | 2024-07-10T00:09:20Z |
| institution | BVB |
| language | Polish |
| oai_aleph_id | oai:aleph.bib-bvb.de:BVB01-024550832 |
| oclc_num | 751154575 |
| open_access_boolean | |
| owner | DE-12 |
| owner_facet | DE-12 |
| physical | 171 s. Ill., Kt. 30 cm |
| publishDate | 2010 |
| publishDateSearch | 2010 |
| publishDateSort | 2010 |
| publisher | Łódzkie Towarzystwo Naukowe |
| record_format | marc |
| series | Acta Geographica Lodziensia |
| series2 | Acta Geographica Lodziensia |
| spelling | Roman, Małgorzata Verfasser aut Rekonstrukcja lobu płockiego w czasie ostatniego zlodowacenia Małgorzata Roman Łódź Łódzkie Towarzystwo Naukowe 2010 171 s. Ill., Kt. 30 cm txt rdacontent n rdamedia nc rdacarrier Acta Geographica Lodziensia 96 Zsfassung in engl. Sprache u.d.T.: Reconstruction of the Płock lobe during the last glaciation Bibliogr. s. 147-161 Eiszeit (DE-588)4014129-9 gnd rswk-swf Płock Region (DE-588)4228597-5 gnd rswk-swf (DE-588)4143413-4 Aufsatzsammlung gnd-content Płock Region (DE-588)4228597-5 g Eiszeit (DE-588)4014129-9 s DE-604 Acta Geographica Lodziensia 96 (DE-604)BV035914667 96 Digitalisierung BSB Muenchen 2 application/pdf http://bvbr.bib-bvb.de:8991/F?func=service&doc_library=BVB01&local_base=BVB01&doc_number=024550832&sequence=000005&line_number=0001&func_code=DB_RECORDS&service_type=MEDIA Inhaltsverzeichnis Digitalisierung BSB Muenchen 2 application/pdf http://bvbr.bib-bvb.de:8991/F?func=service&doc_library=BVB01&local_base=BVB01&doc_number=024550832&sequence=000006&line_number=0002&func_code=DB_RECORDS&service_type=MEDIA Abstract |
| spellingShingle | Roman, Małgorzata Rekonstrukcja lobu płockiego w czasie ostatniego zlodowacenia Acta Geographica Lodziensia Eiszeit (DE-588)4014129-9 gnd |
| subject_GND | (DE-588)4014129-9 (DE-588)4228597-5 (DE-588)4143413-4 |
| title | Rekonstrukcja lobu płockiego w czasie ostatniego zlodowacenia |
| title_auth | Rekonstrukcja lobu płockiego w czasie ostatniego zlodowacenia |
| title_exact_search | Rekonstrukcja lobu płockiego w czasie ostatniego zlodowacenia |
| title_full | Rekonstrukcja lobu płockiego w czasie ostatniego zlodowacenia Małgorzata Roman |
| title_fullStr | Rekonstrukcja lobu płockiego w czasie ostatniego zlodowacenia Małgorzata Roman |
| title_full_unstemmed | Rekonstrukcja lobu płockiego w czasie ostatniego zlodowacenia Małgorzata Roman |
| title_short | Rekonstrukcja lobu płockiego w czasie ostatniego zlodowacenia |
| title_sort | rekonstrukcja lobu plockiego w czasie ostatniego zlodowacenia |
| topic | Eiszeit (DE-588)4014129-9 gnd |
| topic_facet | Eiszeit Płock Region Aufsatzsammlung |
| url | http://bvbr.bib-bvb.de:8991/F?func=service&doc_library=BVB01&local_base=BVB01&doc_number=024550832&sequence=000005&line_number=0001&func_code=DB_RECORDS&service_type=MEDIA http://bvbr.bib-bvb.de:8991/F?func=service&doc_library=BVB01&local_base=BVB01&doc_number=024550832&sequence=000006&line_number=0002&func_code=DB_RECORDS&service_type=MEDIA |
| volume_link | (DE-604)BV035914667 |
| work_keys_str_mv | AT romanmałgorzata rekonstrukcjalobupłockiegowczasieostatniegozlodowacenia |