The calcareous deposits in the upper part of Quaternary-age sediments were found in the
Bełchatów mine. These deposits were accumulated in closed depressions. AIl these depressions
are located in Świętojanka valley and tributary valleys (Fig. 1). The geological structure,
chemical and mineral composition of calcareous deposits have been discussed elsewhere
(Goździk, Konecka-BetIey 1992). In the present paper, the results of pollen analysis
and more detailed field investigations of relationship between the calcareous deposits and
neighbouring sediments are presented.
The closed depressions were developed only the where Plenivistu1ian-age thick series of
fluvial silty-sandy sediments occur. Numerous syngenetic ice wedge casts were found in
these sediments (French, Goździk 1988). Pollen analysis of organic layers included in
the siIty-sandy sediments and fossil beetles from one such layer, indicate a tundra depositional
environment. Similar sediments from such present-day environments are always icerich
and susceptible to thermokarst processes. It is very possible that PlenivistuIian-age
fluvial sediments from Bełchatów were the same. Later, when thermokarst processes had
been developed, the closed depressions were formed in places with a higher ice concentration.
There is other evidence which supports a supposition about the important rOle of
thermokarst processes. The 14C dates of the beginning of the formation of the closed
depressions with standing water and the period of calcareous accumulation in Świętojanka
valley established by pollen analysis, are similar to analogical deposits in typical thermokarst
depressions in the area of the last glaciation in northern Poland.
Calcareous deposits were found always to lie on aeolian cover sands, and were never
invaded by dunes. This shows that calcareous deposition began after cover formation and
perhaps after dune stabilization.
Organic sediments from two ancient lakes I and III (Fig. 1) were analyzed by the
palynological method. Calcareous deposits and two layers of peat situated above and below
them were analysed. Results of this analysis are shown on Fig. 3 for lake I and Fig. 4 for
lake Ill.
Radiocarbon dates of peats from the lower levels of organic material of two lakes are
similar - 12 540± 120 BP, GD-1875 (lake I) and 12 710± 130 BP, GD-5031 (lake Ill). Results
of pollen analysis of both peat layers indicate that during their accumulation the vegetational
landscape had a character of a treeless tundra without traces of lacustrine plants. This
vegetation was developed under subarctic climatic conditions.The pollen analysis shows that after the peat accumulation the development of the lakes
and calcareous material deposition began. This deposition in lake I started during Older Dryas
time. It lasted throughout Alleroo and Younger Dryas time and finished at the beginning of
the Holocene. Pollen diagrams of calcareous sediments from lakes I and III show many
similarities, but there are some differences. These differences may indicate colder conditions
during the accumulation of calcareous material in lake I1I--<:haracteristicfor Boiling period.
An alternative interpretation of these differences is habitat rather than climatic.
In the smaller lake III accumulation finished earlier than in lake I, that is at the and of
Latevistulian.W stropowej części osadów czwartorzędowych odsłoniętych w kopalni "Bełchatów"
występują utwory węglanowe, które były akumulowane w zagłębieniach bezodpływowych
w dolinie Świętojanki, dopływie Widawki. Zagłębienia te powstały wskutek krasu termicznego
związanego z powszechną degradacją wieloletniej zmarzliny. Na podstawie badań palinologicznych
utworów oraz datowania 14C możliwe było uchwycenie zarówno momentu początkowego
zjawisk krasowych, jak i okresu ich intensywnego rozwoju.
Występujące w spągu utworów węglanowych torfy tworzyły się w warunkach podmokłych,
lecz bez stałego zbiornika wodnego, w początkowej fazie krasu termicznego. Oznaczenia
wiekowe metodą HC wykazały dla torfu z zagłębienia I datę 12 540 ± 120 lat BP, a z zagłębienia
III datę 12710±130 lat BP. Badania palinologiczne dowodzą, że panowały tu
wówczas otwarte zbiorowiska tundry bezdrzewnej.
Postępująca degradacja zmarzliny powodowała pogłębianie obniżeń, aż do utworzenia się
w nich stałych zbiorników wodnych. W zbiornikach tych gromadziły się utwory węglanowe.
Spektrum palinologiczne z tych utworów dowodzi, że w zbiorniku I powstały w okresie
a11erOdu,natomiast nie rozstrzyga, czy utwór węglanowy w zbiorniku III tworzył się w bollingu
czy allerodzie.
Torfy leżące w stropie węglanów narastały już w holocenie
