The Ferdynand6w Interglacial in Poland

Kwartalnik Geologiczny, t. 35, nr 1,1991 r. str. 71-80

Zofia JANCZYK-KOPIKOWA

The Ferdynand6w Interglacial in Poland

During the removing of the overburden in the western face of the Bclchat6wmine,Ihe Quaternary lacustrine and boggy sediments named "Buczyna pod brukicm" have been exposed. The pollen analysis of these sediments has shown, that they have represented the same pollen succession which has been illustrated by the pollen diagram from Ferdynand6w. Owing to the characteristic pollen spectra from the interglacial ciimatic optimum it may be stated, that the noms of Ferdynand6w and "Buczyna pod brukiem" are of the same age. The sediments of Ferdynand6w Interglacial al Biatobnegi on Pilica river, Sosnowica and Podlod6w have also been taken into account.

INTRODucrION

The paper "Flora of the Mazovian Interglacial at Ferdynand6w' (Z.Janczyk-Kopi- kowa, 1975) requires presently some comments. In the sixties, owing ^to the detailed analyses of the material (J.Rzechowski et aI., 1966; J.Rzechowski, 1967; J.E.Mojski, 1969), the geological situation of the interglacial sediments at Ferdynand6w ap- peared to be fully precised. The interglacial sediments have been situated between the South-Polish Glaciation and Middle-Polish Glaciation. In the earlier strati- graphic schemes (S.Z.R6iycki, 1964, 1967; E.Rlihle, 1965; A.Srodon, 1960 et al.) the stratigraphic unit between two glaciations ensuing one after the other, that is be- tween South-Polish Glaciation and Middle-Polish Glaciation, was called Mazovian Interglacial. The sediments documented palaeobotanically (with strictly determined pollen succession), as well as sediments lacking in fioral remains, for instance very thick fluvial series of sandy sediments, were included in the Mazovian Interglacial.

The author, writing about the fiora from Ferdynand6w, had in mind mainly its stratigraphic position (between the South-Polish Glaciation and Middle-Polish Gla-

72 Zofia Janczyk·Kopikowa

ciation), nevertheless stressing strongly the differences between the pollen succcs- sions at Ferdynand6w, and at Nowiny Zukowskie (J.Dyakowska, 1952), Cicchanki Krzesimowskie (M.Brem, 1953) and other floras of the same agcs, which are gencr- ally callcd floras of the Mazovian Interglacial. The difference between the. ages of those floras and the age of flora from Ferdynand6w was doubtless, but their mutual relationship remained an open question (Z.Janczyk-Kopikowa, 1975). The essential floral differences between them were the basis for the distinguishing of two different interglacials by ASrodon (1969) - that is the Mazovian and Lublin interglacials.

The stratigraphic position of the floras spoken about caused a broad discussion.

Controversial opinions were formulated by many authors (K.Erd, 1978; L.Lindner, 1981; J.Lyczewska, 1977; S.Z.R6iycki, 1978; E.Rlihle, 1976; H.Ruszczynska-Sze- najch, 1978; M.Sobolewska, 1969; ASrodon, 1969; L.N. Voznyachuk, 1978 et al.).

The palaeobotanical and geological proofs and detailed analysis of full material allowed to formulate an opinion, that the flora from Ferdynand6w represents a new interglacial in Polish stratigraphic schemc of the Quaternary (Z. Janczyk-Kopikowa et aI., 1981). It is presently called Ferdynand6w Interglacial (/.c.). According to the rule of priority, the term Mazovian Interglacial was saved for the interglacial, for which the pollen successions at Nowiny Zukowskie, Ciechanki Krzesimowskie and others of the same age are characteristic. As it is accepted, both interglacials occupy the stratigraphic position between South-Polish (San) and Middle-Polish (Odra) glaciations with the reservation, that the Ferdynand6w Interglacial is situated below Mazovian Interglacial (/.c.; J.E.Mojski, 1985) and is set apart by a distinction ofWilga Glaciation.

The floral characteristics of both interglacials are different. For Mazovian inter- glacial, it was discussed many times (W.Szafer, 1953; J.Dyakowska, 1952; ASrodOlI, 1972 et al.). The pollen succession of Ferdynand6w is most fully illustrated by the pollen diagram from Ferdynand6w. Similar type of floral development was confirmed also in other sites mentioned below.

THE SITES OF FERDYNAND6W INTERGLACIAL iN POLAND

M.Sobolcwska (1969) published a pollen diagram from Luk6w, stating that the developments of floras at Luk6w and Ferdynand6w (Z.Janczyk-Kopikowa, 1963) were similar. This statement found strong confirmation after the detailed working- -out of the sediments from Ferdynand6w; the diagrams from Ferdynand6w and Luk6w were acknowledged as beeing of the same age (Z.Janczyk-Kopikowa, 1975).

The flora from Podg6rze (l.Jurkiewiczowa et aI., 1973) was also accepted as beeing of the same age as Ferdynand6w (Z.Janczyk-Kopikowa et aI., 1981).

J.E.Mojski (1985) correlated the corresponding pollen spectra from Podg6rze with the lower and upper climatic optimum at Ferdynand6w.

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The Ferdynand6w Interglacial in Poland 73

In the seventies, the fossil Oora at Bialobrzegi on Pilica river was worked-out (Z.Janczyk-Kopikowa, 1981). The samples were taken from the boreholes made by

"Geoprojekt" of Warsaw, situated at the right bank of Pilica beyond its valley. The boreholes penetrated the upper strata of soil and sands and then the upper, not very thick horizon of till, under which the lacustrine and boggy sediments (with thickness reaching about 19 m) lay. These formations in turn lay on the lower horizon of till.

Full data about the Pleistocene sediments below the interglacial series are lacking, because none of the boreholes cut through the Quaternary. ,

It is evident from the Geological Map ot Poland 1:200 000, sheet Skierniewice (A.Makowska, 1970) that Tertiary sediments were overlaid by the till of the South- -Polish Glaciation, the Ouvioglacial sands and gravels, and the upper till (Middle-Pol- ish Glaciation - two horizons). More precise definition of the ages of these two horizons of glacial till is controversial.

It results from the detailed geological data for the Quaternary sediments (E.Ciuk, E.Riihle, 1952) for the area lying about 2 km west of the localization site of the

"Geoprojekt" boreholes, that the till on the Warta Glaciation occurs to the north of Pilica valley only.

The age of tills of the Middle-Polish Glaciation in the vicinity of Bialobrzegi was not strictly defined in the Geological Map ot Poland 1:200 000 (A.Makowska, 1970);

they remained there undivided. The presence at this area of till of the Wana Stage was accepted by M.D.Baraniecka (1971) and Z.Sarnacka (1988).

Taking into account all statesments given above, it is difficult to accept an unequi- vocal age for the till covering the interglacial sediments at Bialobrzegi; the sequence of deposits underlaying the interglacial series is also unkown.

The age of the interglacial series was determined using the palaeobotanical crite- ria. The pollen succession at Bialobrzegi can be unequivocally referred to that of Ferdynand6w.

The pollen analysis at Bialobrzegi was done in three boreholes (Bialobrzegi 71 - Fig. 1; Bia/obrzegi 82 - Fig. 2 ; Bialobrzegi 98 - Fig. 3). The fullest image of the pollen succession was achieved in the profile 98. The pollen diagram shows here thc development of Oora, beginning with the boreal coniferous forests with preponde- rance of pine (Pinus). Later the preponderance of birch (Betula) with traces of light-demanding shrubs Ephedra and Helianthemum was noted with a minimal in- crease of herbaceous plants (NAP). The diminishing of the amount of birch (Betula) and pine (Pinus), and the appearance of the thermophilous deciduous trees (Quercus, Ulmus, Tilia) began the phase of prevailing mixcd forests. After their decay, the deciduous forests developped. Oak (Quercus) and elm (Ulmus) acicvcd the amounts of 21.1 and 19.9%; linden (Tilia) of 5.0% and hazel (Cory/us) 44.0%. The share of alder (Alnus) approached 20%; hornbeam (Carpinus) was not found. This phase may be connected with the third phase of development of Oora at Ferdynand6w - the phase of the climatic optimum.

74 Zofia Janczyk-Kopikowa

In the profile 98 at Bialobrzegi the next phase of Ferdynand6w -the fourth phase with Abies - is lacking. This phase is shown at the diagram (Fig. 1 and 2), where the share of fir is distinctly marked.

After the fourth phase all diagrams from Bialobrzegi show the cooling of the climate expressed by the dominant birch-pine forests and the increase of the amount

of the herbaceous plants (with maximum up to 37.0% in the profile Bialobrzegi 84).

The diagrams depict the renewed warming and the come-back of the deciduous forests (phase seven at Ferdynand6w): Quercus, Ulmus, TWa, Corylus and Alnus. The showing-up of Carpinus for the first time in the diagrams (reaching the maximum value of 31.0%) is especially worth mentioning in the profile Bialobrzegi 71 (Fig. 1).

After this warming, in Bialobrzegi the come-back of boreal pine-birch forests was noted, connected with the increase of the share of .the herbaceous plants 10 29.2%

(Bialobrzegi 84 - Fig. 2). This reigning of pine-birch forests ends the interglacial development of flora at Bialobrzegi.

The interglacial lacustrine-boggy series at Bialobrzegi are especially worth notic- ing because of their full development and geological situation. Unfortunately the technique of boring used by "Geoprojekt" in the year 1974 gave no possibility for taking of sufficient amounts of samples for the pollen analysis. The distances between samples generally equaled 0.5-1.0 m, what allowed for obtaining of only approximate data. However, the interglacial pollen succession at Bialobrzegi can be unequivocally referred 10 the pollen succession at Ferdynand6w. Nevertheless, it would be suitable to make a thorough, universal work-out of the interglacial sediments at Bialobrzegi.

The type of the pollen succession, similar 10 given above, is noted in the histogram from Sosnowica in the district of Lublin (Fig. 4). The lacustrine-boggy sediments lie here at the depth of 13.50-18.35 m between two horizons of tills (L.Dolecki et aI., in print). The development of flora begins with the domination of tundra. The share of the herbaceous plants amounts to 64.0%, among which Gramineae are reaching 11.0%, Cyperaceae and Artemisia 10 16.0% each. Chenopodiaceae and Ranunculaceae are rather plentiful. The boreal pine-birch forests, reigning after the tundra, give place 10 the deciduous forests with Quercus up to 21.6%, Ulmus up 10 20.0%, TWa up to 5.6% and Cory/us up to 26.7%. The phase of dominant deciduous forests at Sosnowica corresponds to the third phase at Ferdynand6w. It is the climatic opti- mum.

The fourth phase, in which significant is the share of Abies reaching 30%, is conspicuous in the diagram at Sosnowica.

The cooling after the climatic optimum is also distinctly marked and represented through the reigning of pine-birch forests. At the top of the prOfile the decrease of the amo.unts of Pinus and Betula, and the increase of amount of the thermophilous deciduous forests (Quercus, Ulmus, Tilia, Cory/us) can be noticed. Carpinus appears for the first time in the profile. It seems, that pollen spectra of three highest samples can be connected with the seventh phase, that is with the renewed warming in the profile of Ferdynand6w.

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Fig, 3. Pollen diagram of the Ferdynand6w Interglacial in Bialobrzegi, profile 98 . Explanations as in Fig. 2

Diagram pyJkowy interglacjalu ferdynandowskiego w Biatobrzegacb, profil 98

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The Ferdynand6w Interglacial in Poland 75

The pollen succession at Sosnowica ends with the image of the thermophilous deciduous forest with hornbeam (Carpinus). It seems, that lack of the boreal forests in the end of the interglacial is the result of destroying (by erosion) of the highest part of the interglacial sediments.

At Podlod6w in the district of Lublin the pollen spectra from the climatic opti- mum seem to belong to the Ferdynand6w Interglacial. This profile is still beeing worked-out.

'BUCZYNA POD BRUKlEM'

The sediments in the profile 'Buczyna pod brukiem" were described by M.D.Ba- raniecka and A.Haluszczak (1982). They lie in the central pan of the western exploi- tation face in Belchat6w. The samples were taken for the pollen analysis from the mineral and mineral-organic series found there at the height of 160.25 up to 162.20 m above sea level. Their depth amounts to 2.20 m. 29 samples were taken for the pollen analysis, mainly with the distance between the samples of 5 em, more seldom of 10 cm, and in one case the distance was 25 cm.

The profile "Buczyna pod brukiem' is lithologically diversified. The sandy sedi- ments are overlaid by lacustrine silts containing peat at the top, then by silty peat, in parts containing sand; they are in turn overlaid by silts. These silts were incised by the pavement at the place of sampling (M.D.Baranieeka, A.Haluszczak, 1982).

The sediments from the site 'Buczyna pod brukiem" belong to the lower structural horizon of Quaternary and lie (at the place of profiling) in its upper part on the sandy beds, below which the horizon of till occur·,.

The pollen diagram of the site "Buc')na pod brukiem' (Fig. 5) depicts the domi- nant tundra or forest-tundra. The herbaceous plants (41.6%) consisted mainly of Artemisia - 18.0%, Gramineae, Cyperaceae, Rosaceae, Compositeae and others, for instance Saxifrnga, Gentiana, Caryophyllaceae, Chenopodiaceae . Among shrubs, Salix, JunipenJS and Helianthemum, Hippophae, Ericaceae. This type of flora can witness the presence of subarctic climate, typical for the glaciation. The diminishing of the share of herbaceous plants to about 10% and high amount of birch (Betula) in the pollen spectrum of sample 27 allows to suppose the warming of climate, allowing for the development of thickets, or birch forest. The warming disappears higher for some time (what can be seen from the pollen spectrum of sample 26), giving place for the second time to the development of herbaceous plants of the open plains.

It can be accepted, that the lower part of the diagram from 'Buczyna pod brukiem' shows the climatic changes during the end of the glaciation preceding the Interglacial at Buczyna.

Beginning from the site of taking of the sample 25, the full reigning of arborescent plants is observed - the pine-birch trees with spruce (Picea) and larch (Larix). The amount of herbaceous plants is diminishing, the climate becomes boreal.

76 Zofia Janczyk-Kopikowa

The showing-up of Quercus and Ulmus announces the time of deciduous forests, that is the climatic optimum of the interglacial. Characteristic for this optimum are high values for elm (Ulmus) - 14,5%, oak (Quercus) - 20.0%, and hazel (Corylus) - 39.3%. Linden (Tilia) achieves the value of 7.7% and alder (Alnus) about 30.0%.

Fir (Abies) also shOWS-Up, achieving in the highest sample 3 the value of 5.9%. The presence of Carya and Celtis pollen deserves special notice. These trees do not belong to the present-day flora of Poland and were not found on the Eemian Interglacial.

The presence of such thermophilous trees, as: Buxus, Taxus , Ligustrum and Hedera is also worth stressing. Characteristic is the complete lack of Carpinus. The climate of the optimum was moderate with tendencies to beeing moderately warm, what allowed for the presence of trees: Celtis and Carya, unknown in the flora of present- time Poland.

At the site 'Buczyna pod brukiem', the floral succession after the climatic opti- mum cannot be observed, because the upper part of sediments was destroyed (M.D.Baraniecka, AHaluszczak, 1982). Nevertheless, the pollen succession of the remaining part of the existing interglacial sediments allows in this case for unequivo- cal correlation of 'Buczyna pod brukiem' Interglacial with Ferdynand6w Interglacial.

CONCLUSIONS

The data collected till now for the Ferdynand6w Interglacial allow to state its floral peculiarity. The characteristic pollen succession, repeating in several profiles spoken about, allows for the precising of its features, from which most important are:

1. Small role of spruce (Picea) in the whole interglacial.

2. The climatic optimum, expressed by the reigning of thermophilous deciduous forest, mainly of oak (Quercus) and elm (Ulmus) in more or less equal amounts (about 20%). The culmination of hazel (Cory/us) amounting to several tens per cent after the maxima for oak and elm. Small amount of linden (Tilia). SporadiC or lacking hornbeam (Carpinus).

3. The early spreading-out of alder (A/nus).

4. Short-lasting, but Significant role of fir (Abies) together with insignificant share of yew (Taxus).

5. The warming of climate for the second time in the upper part of the profile, expressed through the reigning of deciduous forest with the significant amount of hornbeam (Carpinus).

It is accepted, that the correlation of the sites of Ferdynand6w Interglacial is unequivocal, if we take the palacobotanic criteria as a base. The stratigraphic posi- tion of this interglacial is still not quite clear because the uniform opinion, rcsult"ing from the interpretation of geological materials about the sequence of Mazovian and Fcrdynand6w interglacials is still lacking. The comparison of geological data and TL dating for the profile of Ferdynand6w (Z.Janczyk-Kopikowa et aI., 1981; J.E.Mojski.

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The Ferdynand6w Interglacial in Poland 77

1985) for the sites of "Buczyna pod brukiem" and Podg6rze (L.Lindner, 1988) induce to the opinion that Ferdynand6w Interglacial is older than Mazovian Interglacial.

However, as it was pointed out, it can be said from the interpretation of the geological profile in Luk6w, that the interglacial sediments of Luk6w lie higher than Mazovian Interglacial.

Interglacial pollen succession of Luk6w and Ferdynand6w are identical and there is no possibility whatever (without complete overlooking of the palaeobotanical criteria) of accepting different ages for these floras.

On the other hand, the character of the pollen and macroscopic flora (existing taxons, their succession and share in per cent) of the Ferdynand6w and Mazovian interglacials do not give, according to the author, sufficient basis to determine which of these floras is older.

The palaeobotanical correlation of Ferdynand6w Interglacial with the intergla- cials of the Russian Plain (for which the stratotype lies in the Nizhniynskiy Rov in Byelorussia), although simple and certain, does not at present solve the problem, because the stratigraphic position of this interglacial in the stratigraphic schemes of USSR is equivocal. G.J.Goriecki et al. (1987) supposes that this interglacial is younger than Likhvin Interglacial, but O.P.Kondratiene and AF.Sanko (1985), L.N.Voznyachuk (1978) and others situate the sediments of Shklov (Nizhniynskiy Rov) below Likhvin Interglacial. So, the mutual relation of Mazovian and Ferdynan- d6w interglacials remains an open question.

Transla/cd by R. poroliski

Zaklad Stratygrafii, Tckloniki i Paleogeografii

Pa~slwowego InstYlutu Geologicznego Warszawa, uJ. Rakowiccka 4

Received: 25.10.1990

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