South-Polish glaciations (Nidanian, Sanian) in southern Central Poland

POlIKA AKADEMIA NAUK • KOMITET NAutC HOlOGICZNYCJI

'AI!ISTWOWE livYDAWNICTWO NAUKOWE. WARSZAWA

Vol. 32, No~

3.4

LESZEK LINDNER

acta geologlca polonica

. WarszaWQ 1982

South-Polish glaciations (Nidanian, Sanian) in southern Central Poland

ABSTRACT: In southern Central Poland there occur sediments and landforms indicative of a subdivision of. the South-Polish ⁽⁼ Cracovian, Mindel) GlaCiation into two separate glaciations: Nidanian (= earlier part of the Oka Glaciation, Hetme-KaZtzeit) and Sanian (= later part of the Oka· Glaciation, EZster-Kattzeit s. s.), divided by the· Malopolanian ⁽⁼ Voigsted-Warmzeit) Interglacial. The latter has been dated by FCIIP and paleoma.gnetic methods and documented by faunistic . remains of the KoziGrzbiet site, Iloly Cross Mts. Within the Sanian GlaCiation the two stadials arerecogwzed:older (maximum) and younger (post-maximum) ones, separated by an interstadial period. During the bipartite older .stadia! of this glaciation the Scandiilavian icesheet reached the Carpathianil whereas during

the younger stadial it occupied only the northern part ot the studied area.

INTRODUCTION

'I1he SOIUthernCeDJt.raJ. Pola;nd suppUestJhe most OOmplete daIta for·

a subdivision of the South-Polish (= Cracovian, Mindel) Glaciation into two gla.c:i.artD.QIrlS: Nddaln-ialIl (Mindel I). and SaniaIIl ~Mir!del Il), sepa.rated by the Malopolanian IIlIteIig1laciail (cf. '.Dex~:fd.gs 1 and 4). Thls conclusion results from the alIl'alysilS of the interglac:i!al fauna pr1e,sented in the karst fi1Jin.gs at·Kozi Grzbiet d:n rtlhe Holy C:ross Mts (Glarek & at 1976, 1977).

It i!S noteworthy thart; a oonsidoem1blepa!I'lt .0£ t..~earea lies outside the 00e of extents of the yOlUlriger glacia'tiOlIls (cf.· LiJIidner & GrzybowSlkd 1982) and 1lhus the ,glacial sed.iments crftJhe ·Sou.th-Polish glaciadions (NidaInian alIld Samdan) can beamaJyzed ·not only in .the iboI>eiholes bUit also in numerous e~:res. Ln thoiJs paper the South-Polish glaci:a.tiorts

164 L. LINDNER

of the Central Poland a're discussed, the precedm:g interglacial, named by R6Zycki (1978, 1980) the Podlas:ian IllIteflglareiaJ including.

PODLASIAN INTERGLACIAL (= CROMERIAN)

This interglacial is represented in the marginal parts of the area by alluvia (20-30 m thick) in buried vall~ys that are incised in slope sediments of the Narewian' (Giinz) Glaciation, in still earlier gravels of the Polaniec Series and in . .pre~Quatemary sediments (Lindner 1978, 19'19, 1980,1982).

o

,

¹⁰⁰

, ^km

o ¹

. Fig. 1. Location of the investigated area . 1 locality- of organogenic deposits of the Poiilasian Interglacial at Ceten near Opoczno; 2 maximum icesheet extent during the Nidanian Glaciation; 3 faunistic locality of the Malopolanian Interglacial at KoZi Grzbiet in the Holy Cross Mts;

4 locality of organogenic sediments of' the Malopolanian Interglacial at Jasionka near Rzesz6w; 5 maximum icesheet extent during the Sanian Glaciation; 6 main ranges of the Holy Cross Mts; 7 limits of the investigated area . . .

SOUTH-POLISH" GLACIATIONS

165 AtCeteit near Opoczno (cf. Text-figs i & 4) there- are ·at least four alluvial sedimentary cycles with ;l gyttja insert (Makowska 1976, 1977). This complex is overlain by a pavement, formed in result of washing of glacial sediments deposited duri~g' the South-P~J,ish" glaciations. A pollen analysis of the gyttja rePresents a fin:al ' 'part of the " Cromerian interglacial with three vegetation phases: toe e~rlie~t one ' is of a bh'-ch-pine' typ~, the middle is birch-pine with spruce, and the latest one is of a pine-birch _typ~ (Borowko-D1uzakowa 1977).

In central and "southern parts of the area these alluvia ate Synchronous with the so-called "gravel series devoid of ·the Scandinavian material", found within ma,ny valleys (Czarnocki 1931; 1950; Lyczewska 1971; Lindner 1977, 1980, 1982) and usually Qverlyingthe sediments of the Narewian Glaciation and formed due to their. wasMing.

After a chranostrati~aphic iSubdivilSioJ;l of the Quatema:ry, proposed by Zuba-l~ov (1978), the Podlasiain In1lerglaJClial shortild oorillpcise an m~

t-erva,l from 790000 .to 680000 years B.P. Wihel'ealS acoording to Rozycki (1978) it lasted from 870 000 to 690 000 )'Iea'l"s B.P. Ln German Democratic Republic (cf. Oepek 1967) this :int~ should be reJ.arted _to'the Artern-Warmzeit. In deep-'seasedimen:ts it is :tlhe equivaJlent of tihe 2!-5t i,SOhorizon, datlled for 782000':"""729 000 years. RP. (Shackleton &

Opd)'lk-e 1973). WYJSOCzanski-M~nkoWlicz (1980) named thiisperiod the' Ceteil? I'IlIterglacial and dated it fur 871 000-810 000 years B.P.

NIDANIAN" • GLACIATION

In thesouthe:rn Centml PIOlaLnd ,the ea~liiest sedli:men.ts of the Nidanian GlaciattiOlIl inclrude(Lindner 1980) slope d~ts, iCE~dam deposits as well as loess 'series, owrl-am !by a ,till hor.i:zon; locally they. ccmta:in flo.ristic and maJac~logic~ rem8li,llIS' (Cmnnooki 1927, 1931,-1950, 1975;

Polmsk-i 1927; Lycrewska 1971, 197.^{. . '} 2; Fdlonowic;l 1972; Watlczowski 1972). - . . ' .

Anoccurrenoe of these sediments wit1ihm Itibe valleys, tbeir lJi1lhologli.c features as wen as t:heir extent arnd Itibe sedir.menstlalry cOver, maiinly by the oldest till (to .the norlh of the Holy C'l'OStS Mts) and the satndy-gralVel"

series with Scan(ltinavian IIlaIberia:1 (Ibo theSOUlth of the Holy Cross Mm), prove "their d€'pOlS1ti:(J/Il linvallley-dammed reservoirs. The latter were form·ed due to damming in tihe lower valley fragmenJtsby the entering icesheet. tongues of .the Nidanian GlaciartJiOn, delSClI'libed previousily as the SICl'-<:aHed S~wczyn Stadial w:iltIhin . the earlier part of tihe SowtIh.- -Polish .G1aciatian.(LiIIldner 1977). A can5i.derable participation of loess

am

a ,looss,..type m81larofauna (Poliilski 1927) indicaJtes that the first

ioesh~t . advance was preceded ·by ,the loess accuroUJlatian (Text-fig. 4).

The materiail. of fbhe latter was ilfuen i'noorporai1led, !in ,reSUlJt of washing, into ,.the sed:iments that" occur. under ,thetilil' horizon. An linter:fingering of rIlhe ea~1ri.est sandy-6l:1ty seri'eS with oollruvial flows andWlith glac!ial or fluvdoglaciail sedimem.ts document'a deposition close to tlhe ic·eshret (Lindner 1977).

166 ^{L., LINQNER}

A do.se occurrence ofrbhe' Wesheet' :is 'alse> suggested. by a· presence ofWr"Ved c1ay

mserts and'

^:f.1Ilie pieces of ' SaanJCi1m8lvianl'!ocks; 'niO,1ied Within' theeairliest sllOpe~custrme

series, as '

well

as

on the basisru US~ClUTl'!eri;o~·~ /to 240~26Q ttD. a,s.J. "(cZarr-~ '1927, 1931, 1950, 1975;

I.yczewSka 1971; Fdlonowicz 1972;

wa:lczows1ti

^{1972; .LiJndner i977).}

Such a high water drumming :in the vaUey and depositi-OOl of tihick ice~

~da.m series could be d<me· :by the !iIoeSheet thaJtentered the ^{aIrea '} llJOlt onJyf-rlOlm the nor.th but ailoo . from the west rund eaJSrt.

An . .extent of' 1Jhe ti 11 that covers' fihe . eaa-l!iest sl~laCusbi'iirre' series and petflographl:c oompCl'S:ition Of i'hegraV'el .. boulder till. fTaotton maJrk the ioesheet advaJI1Ce of tlhe NidalIlJian GilaoiaIti-OOl. as fa.r as the 1l).<>T.thern sllO!Pe. 0If ,:the Holy Cl"oss'Mts (T,eXit-fig. 1). A hypsomemcal· positilOO'l of the eal"liest :rl7iH in this area suggests it!hat . .i!f Clhe"ia!rer siglnif:icant -!lie(),;

teic1iOlll'ic movements aJI'le excluded thEm' the licesheet ioot "OiOOllned' during the Nidalniatn GlaciartliJOn ,up to' 240-270 m ' a.sl. 'TIhrough.owtthe' passes

of the marlin ranges of, 'the HolyCTIMS Mtls I(ef. ,TeXit-fig. 1) the glacw tongwes mOiVtedS€'VIera!l !killometres' iur.ther :to the south.' These tongues are 'J.'Iecog;n±Zlihlte, now by ,thin till 1h0000000ems unde:rl1a.d!n by tlhe ea;rliest ice.-dam rund f;lIuV'ioglacia'l sedim€l.IlllB :iJn 1lhe western' part of the 'Holy Crt>ss Mbs (Lindner 1977), 'and a'Lso by itlhte iSO'-'caJ1ed''1ocal till", in clelIlJ1lr-al and eastern pa:rts of ,the Holy Gr.oss Mtts (OZlall:nockIi. 1927, 1950; t.y- czewska 1971, 1972).

To the east of t1!nearea,' in the Lulbl!iin Upland, 'the NidaaldaIn Glacia- tion tits proIbably ~ented by sedime'Ilits of tine lJOweJ." glacial phase of the Senn:iikii Stadiall; SOUith-PoldJSh Giaciaihtool (cf.Mojskii 1969) whereas to tbe' ~t (run the't.Odz Up1aJnd) by

the

10Wlermoot giaclgeme'ihOrii.ttID Within: " th~' Bekthrut6wGcibeiIl., . referred to ltihe LOwer Stadiailaf tihe South-Polish Glaciation (efBarahieeka & Sarnacka 1971)~

: ' ' 'lit

tiheEUrO~ WIle'IO! theSovret Union ttllJi.s paIl't of ~he NidahJm Gl~tfliantis represented bytheearliest'1liilil of the Oka 'GlaciJaltiO!Il (cf.

Zllba;kov & 'Kocheg\,lT~' 197.3)'dartJed bya t1lhermoluminescehee metth-odfot 600000±60 000 year-s RP., rund by ,tJhe loesse.s dJatedfor607000±65 000 yOOirs B.P. Wihereasdn" German DeinOOratic RapUlblik by the -irnIterval Helme-Kaltzei-t= Grundmoranen El (cf;Cepek. ,1967). Acooroingto"Zu.., bako'V (1978) tihiisglacia1Don -, compriSes ^8; time' wervta:l from 720 000 '00 680000 years B.P. Wysocz:ailski-MilIikoWlicz:(1980)defitlleS <it as the pa-e- -Nida Glaclaitiml and daites fur 8HlOOO-74'8 500' y,eall'S RP. Witth'i!n th~

deep-seasedimen.ts-:tJhe 2tltih18()' horlizon, da.tied £01'729 0'00--,-70600'0' Y'ealfs B.P.·' (ef. Sihaddeton & Opdyk,e :1973), ~eemstio be: of, thesahte'

~.

MALQPOLANIAN,INTERGLACIAL

Sandy-gravel sediments, gmVlels and mora:i.n!i.c' pavements art the top of the albov€ described deposits represemt d!n sCJUitnern Qe:ntral Poland

SOUTH-POLISH' 'GLACIATIONS 1'"67

aIlintexglaciaa fhiVlia,1 acc~Iati!on.' In most

Oases

the interglacial fluvial sed~ts ctllil.~~·· Scrui~~an' :~ks. '. '

In the Holy Cross Mts, these sediments fill the valleys (W--20 m deep), formed in result of erosion initiated at the end 'of the previous glaciatiQn. Outside the valleys, particularly a~ a loessy substrate, the weathering-soH processes have . developed during this interglacial an.d are marked· now by paleosoils (Czarnocki

1975, Lindner 1977).

The faunistic site at· Kozi Grzbiet in the southcwestern· Holy Cross Mts (Cf. Text-figs 1~) supplied with neW data for this .teme interval (Kowalski 1975, 1976;,. Glazek, Lindner &

Wysoczaiiski-Minkowli!z' 1976; Glazek,KowaISki, 'L1ndner, Mlynarski, Stworzewicz, TUcholka

& Wysoczal'iski-Minkowicz im; Sz~dlar 1981) ... The cave depoSits contain there (Text~fig. 2A)

but faunistic remains, also the·.InlJterlal (feldspars,heavy minerals) coming undoubtedly from washed fluvioglacial sediments of We. Nidaruan Glaciation. A rich taunistlc assemblage: con- tains numerous snails, amphibians,reptiles' :and' mammals. Among the snails the most im- portant are: HeUctgona banatlca,. SooBia" diodonta, IsognoTlWstoma' peTBonatum, Zenobtella vtctna, Cochtodtna laminata, c. OrthOBtOn.a, LactntaTta cana, Ruth'entca' tttogTama, Ctausttia CTuctata, Iphtgena tatestTtata, 1. tumtda·'apd· Acanthlflutir.· acuetata,' representative for a re- latively warm and wet forest. Among the amphibians· and' . reptiles (cf. Szyndlar 1981) the most common are' Natrtr natrix and TriturU8 cf;'· crtstatuB, the both species typical of deciduous and wet forests. At the same time there 'are some thermopirlIou8 genera (ptto- batrachus and E!aphe) as well as very rare st~ppe .. onl;ls (petobates). The p).'esen!:e of boreal mammals (LemmUB temmuB and Dicrostonyx st'mpttctor) proves a quite cool, .. steppe climate, whereas castor tiber, Cte-thrtonomys cf. gtareotUB, sua cf. 'scrota, Atces·sp. and Pttomys !enkt

suggest a forest and wet environment. . . .

The age of the Kozi Grzbiet locality carl. bedetined on the ground of the overlying fluvioglacial sands of the Sanian Glaciatlon.(W6dkowski 1971, Lindner &

Kowalski 1974, Lindner 1977, Radlowska & Mycielska~Dowgiano 1972) as well as the presence ... Qi Pliomys lenki, Mimomys savini,Dicrostonyx simplicioT, Ursus deningeri, HeZicigona banatic(l"PUobatrachus langhae .. an.d probably, Bornbina cf.

bombina for the Late Cromerian (Glazek, Kowaiski, Lindner,Mlynarski,. Stwo~

rzewicz(Tucnolka & Wysoczailski-Minkowicz1977}. A similar conclusion is di-awn from absolutedatings of· bones by FClIP .methodas 559 .. ~ .. 700 000 years B. P.

(Glazek, Lindner & Wysoczailski-Minkowicz 1976), pointing out the so-called Cromer 11 of 'the Dutch worke~sas' well as from paleomagnetic studiefj (Te~t-fig. 2.13) of P. Tucholka (cf. Glazek, Kciwalski, Lindne;t·, Mlynarski,Stworzewicz;'Tucholka &

Wysoc,zanski-Min~owicz 1977)' that show a positive magnetic polarization of cave sediments and so,exclude thei.r accumulation during the optimum phase of the Cromerian Interglacial (cf. van Montfrans 1971). All the data prove the integlacial to be warmer than the present times.

Fluvial sediments of the MaloPolanianlnt~rglacial, noted in southern Central P<!land (Lindne:r: 1982), correspond probably .. in .the Lublin Upland to a thick series of alluvia, deposited during the iri.terphase 6f the so-called Serniki Stadial (cf. Mojski 1969) and .to the intermor;linic deposits that separate the tills of lower

and 'up~~r' sta:dials of the South-Polish Glaciation in the Belchat6w Graben

(cf. Baraniecka &. Sarnacka 1971). Theup~r . part .of the interglacial .is also represented by organogenic sedimentsat Jasionka pear Rzesz6w (DllbrowskL 1967,

.Laskowska-Wysoczanska 1967). ..

In German Democratic Republic this interglacial corresponds (cf. Cepek ,1967, Erd 1978) to the Voigstedt- Warmzeit, and in the Soviet Union -- with the warming that separates a deposition of lower and upper tills of the Oka Glaciation (Zubakov & Kochegura 1973). After Zubakov (1978) this interglacial las.ted from 680 QOO to 610 000 years. B. P., and according toWysoczanski-Min- kowicz (1980) from 748 500 to 687 000. years . B. P. In . deep-sea sediments this

168 L .. LINDNga

interglacial can be referred to the warming marked· by the 19th ¹⁸0 horizon, dated for 706000-688000 years B.· P. as the earliest distinct warming within the Brunhes paleomagnetic epoch (cf. Shackleton & Opdyke 1973, Bonifay 1980).

o

1

2

3

sands

CQve loams

~\,4,1 brecciated

claY5

~~) red sandy clays

k..~fJ f~ne clayey sands

mIIIIl ^{residual clay"}

"., flow.stone

dabrl~

o limutone blocks

G> ~nQil ~heUs

. . . bones

Fig. 2A. Sequence ot cave sediments with fauna of the Malopolanian Interglacial at Kozi Grzbiet qear Ch~ciny in the Holy Cross Mts (after Glazek &al. 1977)

SOUTH-POLISH GLACIATIONS

SANIAN GLACIATION.

OLDER (MAXIMUM)STADIAL

In southern Central Poland two till horizons were deposited by the icesheet of the maximum stadial of the. Sanian Glaciation. (Text-fig. 4).

these tills are accompanied in many places by loessy, ice"dam, slope and fluvioglacial sediments (CzarnOcki ·1927, 1931, 1950, 1975; Lyczew- ska 1971; FilonoWicz 1972; Hakenberg & Lindner 1971; Lindner 1971a;

Lindner & Kowalski 1974;. Lindner 1977). Usually, especially outside the

Inclination

•

• normal

o

^reverse

Declination

Fig. 2B. Results of paleomagnetic analyses of the profile obtained at Kozi Grzbiet . . (as indicated in Text-fig. 2A) .

170' ^{L. LiNDNER}

valleys, the top surface of the iower till is washed; this indicates a distinct break between deposition time of the lower and. the upper till horizon. These tills seem to correspond (Hakenberg & Lindner 1971;

Lindner 1971b; Lindner & Kowalski 1974; Lindner 1977,' 1978) with the successive phases separated by the Kielce Interphase. This bipartity is considered wrongly by Wysoczaiiski-Minkowicz (1980) the equivalent of "Nida and Sail Glaciations", lasting since 687 000 to 626000 years B. P. Within the deep-sea sediments this tripartite intertVal is represented by the "18th, 17th a:nd i6th 18() horizons, dated for 688000 to 592000 yea!s, B. ~,,:, (~f. Sh~fklet9p::~ <?;pdyke 1973).

L~~: ieez.datn,-slf>.pe--er .. fluVioglaCial sediments 'overlilin by the lower'lill.ot·the.olcier-stadial,

prOVe

a loessy and an ice-dam accumulation, locally intetfingeringwiih slope and fluvioglacial deposits' before the icesheet advance during the older phase of this stadia!.

s Mt. Miedzianka

I ^{- r T r} --

ICESHEET

'm a.s.I.

400 D

200

400~ r-r("1-:-C~ C

200o/~~/~ .

400 . Kozi Grzbiet Hi" Wit . h cave , t~ ^{; , , "' . "}

200~~//~ _---- ^B

400 A

200

Fig. 3. Scheme of evolution of glacial and fluvioglacial deposits in the western part of the Holy,' Cross Mts during the South-Polish glaciations (after Glazek

& al. 1977)

A - Nidanian Glaciation, B - Malopolanian Intergla€ial, C ~ older phase of the maximum stadial of the Sanian Glaciation, D - younger phase of the maximum

stadial of the Sanian Glaciation

SOUTH-POLISH GLACIATIONS

A,n extent of the lower till' (2~15 m thick) proves that the icesheet or the older phase has not covered entirely the Holy Cross Mts. During its maximum expansion,not only the nunatak-like hills. over 300.0.:.:..350 ma.sJ. high' were iCe-free' (Text-fig~ 3), but also several' lower areas that 'were the'intraglacial oases (Lindner 1977). KnoWing a petrographic composition of the gravel-boulder fraction of the lower till and especially, the: presence of the Tertiary and Paleozoic rocks outside their occurrence belt but within the till, supports the 'prelViousopinions '(Siemiradzki 1888~' Czatnocki 1931; Lyczewska 1971; R6zycki 1967, 1972) on a possible EmcircIirtg the Holy Cross Mts· by the' icesheet of the South-Polish glaciations,' from the east and south'::east.

'During the Kielce Interphase a deglaciation' caused almost' the whole' ttrea:

to be ice~free. Only in some valleys but not entirely, -the dead ices had remained, then ()overlain by the icesheet of the younger phase, what resulted, in a single acumulative horizon of the discussed older stadial(Lindner 1977, 1979).

'The petrographic composition and occurrence of till of the you,nger phase of the older stadial' (Text-fig. 3),' enabled to reconstruct the , . .maximum icesheet extent in the western part of the Holy Cross, Mts

(Li~ci:ner 1977)., The received data (Glazek, Kutek & Lindner.1976; Lind-

ner:1977, 1978) supported theprovious suggestions (Siemiradzki 1888;

Cz~rnockiI927, 1931;, Lyczewska 1971; R6zycki 1967, 1972) on, the

en~rance of a glacial lobe into this area; the icesheet. transported the Tertiary rocks from the south-eastern margin of the Holy Cross Mts _{, , ,} and from their Paleozoic core.

An analysis of the icesheet movements and deglaciation, of the lIoly Cross, Mts(cf. Klatka 1965; Lindner 1971b; Lindner & Braun 1974;

Lindper 1977; Racilowska &Mycielska-Dowgial~o 1972, 1974) as welLas

t~~, data onpetrqgraphic composition of gl~cial graiVels (Dr.Z. Lampar- ski, personal information), the occurrence of the Scandinav,ian material up to 450-500 m a.s.l. (Miklaszewski 1911, Czarnocki 1931, Walczowski 1972, Lyczewska 1971) point out that during the maximum extent of the icesheet, it finally overpassed the main ranges of the Holy Cross Mts, 'in spite 'of its previous attacks from the east and west. , This\

conclusion does not exclude, however, the possible occurrence of rnina- taks (cf. Klatka 1965), 'being the icesheet oases (Text"';fig. 3) with a kame accumulation (Lindner 1971b, 1977; Lindner & Kowalski 1974; Radlow- ska& ,Mycielska-DowgiaUo 1972, 1974).

'In the north-western part of the investigated area, the older (maxi- mum) stadialof the Sanian Glaciation is also represented by two till horiz-ons, the lower one of which corresponds, together with the underlying sands and silts, to the older phase whereas the upper till to the 'younger (maximum)' phase of this· stadial (Lindner 1979).

In the northern part of the area the younger erosive-denudation

172 L. LINDNER

processes (MazovianInterglacial) resulted in a considerable denudation of the sediments of _ the South-Polish glaciations (Ruszczyilska 1961;

Lindner 1971;. Grzybowski 1972; Makowska 1976, 1977; Lewandowski 1977). In a lVast area, these glaciations are marked by a residual pavement and in some sections only a single or two till horizons could be noted.

In the eastern part of the area a residual occurrence of glacigenic sediments, deposited during the South-Polish glaciations, makes it dif- ficult to note a bipartity of the maximum stadia!. In most cases there exists only a -single, intensively destroyed till (Samsonowicz 1934; Po- zaryska 1948; Radlowska 1963; Kosmowska-Suffczyilska 1966, 1972; Bie- lecka 1969; Kowalczyk & Pu9Howska 1977).

A similar situation existed in the southern part of the area where there is usually a single till horizon of the maximum stadial of the Sanian Glaciaton (cf. Radlowska 1966; Lyczewska 1968, 1969, 1971; Wal- czowski 1972; Szajn 1978; Kwapisz 1978). Only in the zone with higher elevations there is a distin~t bipartity of these tills, accentuated by inserts of sands and silty-clayey series (Hakenberg & Lindner 1971, Lindner 1977, Lindner & Ziembiilska-Tworzydlo 1974).

The works on the younger phase of this stadialin the- Central Poland, have been mainly concentrated in the Holy Cross Mts (Radlowska &

Mycielska-DowgiaUo 1972, 1974; Lindner 1977; .Lindner & Braun 1974;

Lindner & Kowalski 1974) and documented an areal type of the degla- ciation in this area as well as its run during at least two phases.

The sediments of the maximum stadial of the Sanian Glaciation in·

southern Central Poland correspond probably to deposits of the upper phase of the so-called Serniki Stadial in the Lublin Upland (cf. Mojski 1969) and the lower till horizons noted within the Belchat6w Graben, connected also with the maximum stadial of this glaciation (cf. Ba- raniecka & Sarnacka 1971).

INTERSTADIAL

In the north-western and northern parts of the area there are fluvial sandy-gravel sediments and silts in many borehole sections, underlain by the till of the maximum stadial and representative for the post-maximum interstadial (Text-fig. 4). A stratigraphic position of these sediments is best documented by the boreholes in the Wysmie- rzyce region (Jurkiewiczowa & al. 1973; Lindner 1979, 1982). The 8edi- ments of the Luszawa Interstadial from the Lublin Upland (cf. Mojski

1969) are synchronous with the deposits of the interstadial of the Sanian Glaciation. Within the deep-sea sediments this warming is recorded by the 15th ¹⁸0 horizon, dated for 592 000-542 000 years B. P. (cf. Shackleton

& Opdyke 1973).

ACTA GIlOLOGICA POLONICA, ·VOL. 33 L. LINI)NBR, Fro . •

Main stratigraphic units of the earlier Middle Pleistocene

GDR SOUTHERN PART OF CENTRAL ^USSR

_after ¹⁸

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POLAND

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stage

. V.V. Kochegura (1973),

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S:2 z

^{OLDER .}

_~Hlm B Illmmlll~ Hmi.llmmmu . . Hf9!am~·!.I.~~~m' ^..

^Oka

L

younger till

0 _~

¹⁶¹⁷

-I ~ ^STADIAl

~ .rC~:~:·~:d:·~·'~:~1 ~'~'::w:.;;;';';;':';~'.~. 18

1--- ~

~

MALOPOLANIAN

_~

^~~

^.. I

^Josionko

* ¹

^-I -19

VOIG TSTED-WARMZEIT

:- . . . ®

v!l r

Kozi Grzbiet (!)

0

INTERGLACIAL

a...

I

I

(Kozi Grzbiet FCVP=SSO-700 000 BP!

I. «

~-~--- ~

J:

..

I- _• 1

0

::>

NIDANIAN

DHDHILYBlmlg~~gu[~~:z~ ~.===~: .

²⁰

HELME-KALTZEIT

g

GLACIATION Oka

L

^older tilt

- ---- -

« ..

• IKozi Grzbietl

i~ ~t

C.ten

I . . ..

ARTERN-WARMZEIT PODLASIAN

~ I

BIAtOWIEiA

~

..

21

INTERGLACIAL

INTERGLACIAL

« I

~ •

,.

~2 0]5

1 tills, Z ~oesses, I localities of organogenic sedimtmts, , faunistic locality, 5 chronostratigraphic extent of the Kozi Grzbiet sequ~ce, .• sam~

pIes with absolute datings (FClIP, TL and paleomagnetism after Glazek &. at 1978, 1977; 180 horizons after Shackleton & Opdyke 1973)

SOUTH-POLISH GLACIATIONS 173 Y()UNGER (POST-MAXIMUM) STADIAL

An overlying of these sedimenis by a successive till horizon of the Sanian Glaciation and the presence of synchronous loess deposits to the, south (Lindner 1979, 1982) allows eo distinguish the younger stadial

of the Sanian Glaciation (Text-fig. 4). .

To the north of .the Lower Pilica valley, this stadialis represented by a till horizon of the Cracovian Glaciation (Ruszczynska,...Szenajch 1966). In the Lublin Upland it corresponds to the Kock Stadial(Mojski 1969) whereas in the I:..odz Upland it is represented by the youngest till of the South-Polish glaciatioils (ej. Baraniecka & Sarnacka 1971). Within the deep-sea sediments this stadia! corresponds probably to the 14th 18()

horizon, dated for 542000-500000 years B. P. (cf. Shacldeton & Opdyke 1973).

In connection with thestratigraphic subdivision of the Quaternary in western Europe (Cepek 1967, van Montfrans 1971), the bipartite Sanian Glaciation corresponds to the so-called Glaciation B (= Elster-Kaltzeit s.s., Grundmoriinen Ell). In the European part of the Soviet Union this period is represented by the tills band e of the Oka Glaciation, dated by the thermoluminescerice method for 560 000 ± 60 000 and 483 000 ± 54 000 years B. P. (Zubakov & Kochegura 1973).

Institute of Geology

of the Warsaw University, Al. Zwirki i Wigury 93, . 02-089 Warsaw, Poland

REFERENCES

BARANIECKA M. D. & SARNACKAZ. 1971. The stratigraphy of the. Quaternary and the palaeogeography of the drainage. basin of the Widawka. Biul. Inst.

Geol., 254:, 157-270. Warszawa.

BONIFAY M. F. 1980. Relations entre les donnees isotopiques oceaniques et l'histoire des grandes faunes europeennes pliopleistocenes. Quat. Res., 14, 251-262. New York.

BOROWKO-DLUZAKOWA Z. 1977. Ceten - Pollen diagram of Ceten sequence on the Drzewiczka River. Przew. Symp. Teren. CzwaTtorz~d zachodniej cz~sci regionu swi~tokrzystkiego; pp. 126-127. Wyd. Geol.; Warszawa.

CEPEK A. G. 1967. Stand und Probleme der Quartarstratigraphie im Norteil der DDR. BeT. Deutsch. Ges. Geol. Wiss, A, Geol. PaUiont., 12 (3--4), 375-404.

Berlin.

CZARNOCKI J. 1927. Sur les glaciations de la partie centra le du Massif de St. Croix. Posie.dz.!Vauk. P.I.G., 17, 18-21. Warszawa.

1931. Diluvium der Swi~ty Krzyz Gebirge. Rocznik P.T.G. (Ann. Soc. Geol.

pologne),7,85-105:Krak6w. .

1950. GeoJogy of the Lysa G6ra Region. Prace P.I.G., 1~104. Warszawa.

- 1975. Pleistocene. Prace I. G., 76, 1-155.Warszawa.

174 L~·LINDNER

D.t\BROWSKl M. J. 1967. Pollen analysis of an interstadial· profile from Jasionka near Rzesz6w. Acta Geol. Polon., 17 (3), 509-520. Warszawa.

ERD K. 1978. PoIlenstratigraphie im Gebiet der skandinavischen Vereisungen.

Schriftenr. Geol. Wiss., 9, 99~1l9. Berlin.

F~LONOWlC~ P. 1972. Pleistoc.ene. deposits in. the SW part of the Holy Cross Mts. Rocznik P.T.G. (Ann. Soc. Geot Pologne),. 42 (1), 105-116. Krak6w.

GAlGALAS A. & KONDRATlENE O. 1976. Quaternary depositii stratigraphy. In:

The buried paled-incisions of sub-Quaternary rocks surface of the south':'east Baltic' Region (Ed.: A. Gaigalas), 117-131. Mokslas P'UbUshers; Vilnius.

GLAZEK J., KOW ALSKl K., LlNDNER. L., ML YNARSKl M.,. STWORZEWlCZ. E., TuCHOLKA p, & WYSOCZANSKl-MlNKOWSKl T .. 1977. Cave dElP9sitsat Kozi Grzbiet (Holy Cross Mts, Central Poland) with vertebrate and. snaq faunas of the iVIirideliim . i/Mindellan II lnter!!Hacial and their stratigraphic correlations. Prac.· 7th Intern. Speleolog. Congr;; pp. 211-2i4. Sheffield.

GLAZEK J., KUTEK J. & LINDNER L .. 1976. Boulders of Tortonian limestones in till deposits of the Sitki hill near .Ch{lciny, Holy Cross Mts. Przegl. Gem., 8 (280), 459-463. Warszawa.

GLAZEK J.~ LlNDNER L. & WYSOCZANSKI-MINKOWICZ T. 1976. Interglacial 'Miridel 1JMindel II in fossil-bearing karst at . Kozi Grzbiet in the Holy Cross Mts. Acta Geol. Polon., 26. (3),337-393. Warszawa.

GRZYBOWSKI K... 1972. Remarks on the Pleistocene in the Pilica valley of south Sulej6w .. Rocznik P.T.G. (Ann. Soc. Geol. Pologne), 42 (1), 143-150.

Krak6w.

HAKENBERG M. & LINDNER L. 1971, Quaternary deposits of the middle Nida valley. Acta Geol. PoZon.~ 21 (2), '241-264; Warszawa. . JURKIEWICZOWA l., MAMAKOWA K. & RUHLE E. 1973. Middle Pleistocene

deposits south of Wysmierzyce near Nowe Miasto ·on the Pilica River.

Folia Quaternaria, 43, 1-26. Krak6w. .

KLATKA T. 1965. Geomorphology of the Holy Cross Mts. Roczni"ki Gleboznawc~e, 15, 12~-162. Warszawa.

KOWALCZYK A. & PUCILOWSKA E. 1977. Stratigraphic position of the fossil lake series in the exposure of Lojowice. near Sandomierz. Prace Na'Uk. Uniw.

Slqsk., 192 (Geologia 2), 123~129. Katowice.

KOWALSKl K. 1975. Earliest appearance of lemmings in. the Quaternary .of Po- land. In:' ALBERDI A. T. & AGUlRRE E. (Eds), Acta I coloquio Internacio- nal . Sorbe Biostratigrafia Continen:tal del. Neogen9 Superior y Cuaternario Inferior, Montpellier-Madrid 19'74, pp. 99--1104. Madrid. . . 1976. Fauna krc::gowc6w plejstocenskich regionu swi{ltokrzyskiego, Materialy

II Na'Uk. Konf. Paleontolog6w, Kielce.

KWAPISZ B. 1978. Quaternary of the Upper Mierzawa drainage oasm. Kwart.

Geol.;22 (1), 197~11. Warszawa.

LASKOWSKA-WYSOCZANSKA W. 1967. The interstadial .

of

the Cracovian Gla- ciation from Jasionka near Rzesz6w. Acta Geel. Polon.; 17 (3), 4195-507. War- szawa.

I.EWANDOWSKI J. 1977. Sediment and transgression character of the anaglacial part of Middle-Polish Glaciation in the OilOczno region. Prace Na'Uk. Uniw.

Slqsk., 192 (Geologia 2), 130-138. Katowice.

LINDNER L. 1971a. Pleistocene stratigraphy and palaeogeomorphology of the north-western mar.gin of t.he Holy Cross Mts, Poland. St'UdiaGeol. Polon., 35, 1---.113. Warszawa.

·1971b. Loess deposits at Obl{lgoreknear 'Kielcei Holy Cross Mts. Acta Geoi.

Polon., 21 (2), 265-278; Warszawa.

SOUTH-POLISH GLACIATIONS 175

1977. Pleistocene glaciations in the western· part of the Holy . Cross ,Mts, Cen- tral Poland. Studia Geol. Polon., 53, 1~HI3. Warszawa.

1978. Palaeogeomorphologic evolution of .the western part of. the' Holy Cross region in Pleistocene. Rocznik P. T.G. (Ann. Soc" GeoZ. Pologne), 48 (3-4), 479--508. Krak6w.

11979. Stratigraphic position .and extent. of tills in tqe central part of the Malbpolska ,Upland. Btuz. GeoZ. Uniw. Warsz., 23, 59--77. Warszawa .. 1980. An outline of chronostratigraphy of Quaternary in the Holy . Cross Mts. Kwart. Geol., 24 (3), 689-710. Warszawa.

1982 .. Plejstocen i holocen w G6rach Swi~tokrzyskioh. In: Budowa Geolo- giczna Polski, t. I -:-. Stratygraiia, cz. 3 Kenozoik - Czwartorz~d (Ed.: J. E.

Mojski). Inst. Geol., Warszawa.

& BRAUN J. J. 1974. Stratigrap'hie du Quaternaire et developpement mor-

phologique de la val1ee de. la Bobrzyczka aux environs. de la ,grotte de Raj.

Bad. i udost. jaskini Raj, pp. 131-14'2. Wyd. Geol.j Warszawa.

& GRZYBOWSKI K. 1982. Middle-Polish glaciations '(Odranian, Wartanian)

in southern Central Poland. 'Acta Geol. Polon., 32 (3-4), 191-206. Watszawa.

& KOW ALSKI W. R. i974. QUaternary cover around Mt. Miedzianka in the

Holy Cross Mts. Acta GeoZ. PoZon.~24 (2); 415-424. Warszawa.

& ZIEMBINSKA-TWORZYDW .M. 19114 •. The Eemian Interglacial deposits

at

zakrucze near Malo:goszcz, western, part of the Holy Cross Mts .. K~aTt.

'GeoZ., 18 .,3), 636~. Warszawa.

LYCZEWSKA J. 1968. Vaccumulation fluvio-perigl;lciaire dans la partie. centrale duBassin de la Nida,. Pologne Centrale. Biul. Perygl., fT, 125---147. L6di..

1969. Sedimentset processus Quaterna,ire du versant cretaoe de . la, . Basse Nida (partie' meridionale

de

la Pologne Centrale). Biul. PerygZ.,

18,

19~08.

l..6dz.

. 1971. The ~uatern.ary of the Holy Cross r~gion .. Prace Inst. Geql., .64, 5--108.

Warszil.wa.

197~. Problems of Quaternary investigations in the HolY· Cross Mts. Rocznik

P. 'T. G. ,(Anllo .• Soc,. Geol. Pologne), ~ (1), 81...-92. Krak6w.

MAKOWSKA A., 1197:6. Old-Pleistocene or,ganogenous deposits at Ceteit and thei:r connection with the preglacialseries of southern Mi;lzovia. Kwart.GeoZ., 20 (3), 597-624. Warszawa.

1977. Ceteit - OI1ganogenic deposits of Early. Pleistoc.ene ~t Ceteit on the

. Drzewiczka River.' przew. Symp. Teren., Cwartorz~d zachodniej cz~§ciTe­

gion'iL 8wi~tokrzyskiego;

PP.'

1lS-::-126. Wyd. Geol.; Warszawa.

MIKLASZEWSKI S.1911. Les tr,aces du glacier sur .1a ,montagn.e de .S,-te Croix.

Spraw. Totv.Ntiuk~Warsz.,4, 388-390. Warszawa.

MOJSKI

i

E. 1969. Stratigraphy.' of lVIeso-Pleistocene glacial dep.osits. Kwart.

Geol., 13 (2), 385-:-407.' Warszawa.

van MONTFRANS H. M. 19'71. Palaeomagnetic dating in the North Sea Basin, 1-H3, PrincoN. V.; Rotterdam.

POLINSKI W. 11927. Gasteropodes diluviaux de Kielce. Posiedz.Nauk. P. I. G., 17, 21-22. Warszawa.

POZARYSI<A K. 1948~Stratigraphy of Pleistocene of the Lower Kamienna valley.

Biut P. 1. G., 52, 1-4H;' Warszawa.

RADLOWSKA C. 1966. Zgeomorfologii okolic Pmczowa. In: Studia geograficzne w powiecie piitczowskim. Prace 'Geograf. Inst. Geograf~ PAN, 41, 13-38.

Warszawa.

176

L.'LINDNER

& MYCIELSKA-DOWGIALLO E. 1972. Comments"ort deglaciation in W part

of Swi~ty Krzyi; Mountains - near ^Ch~ciny. Przeol.Geooraf., 44 (4),' 649- -6'72. Warszawa.

& 1974. Deglaciation in the SwiI:tokrzyskie Mts; Geograph. Polon., 28,

19-48. Warszawa.

ROZYCKI S. Z. 1967. The Pleistocene of Middle Poland, 1-251; Panstw. Wyd.

Nauk.; Warszawa.

1972. Plejstocen Polski' Srodkowej; Wyd. 2, 1-315. Panstw. Wyd. Nauk.;

Warszawa.

1979. From Mochty to a synthesis of the Polish Pleistocene. Rocznik' P. ^T. G.

(Ann. Soc. Geol. Pologne), 48 (3~), 445-4,78. Krak6w.

1980. Principles of stratigraphic subdivisions of Quaternary of Poland. ^Quat.

Stud. Pol., 2, 99-o106.Warszawa-Poznail..

RUSZCZYNSKA H. 1961. The Quaternary in the neighbourhood of Tomasz6w Ma- zowiecki and Sulej6w on the Pilica River. Praceo Plejst. Polski Srodko- wej, H}.l-I06. Warszawa.

19f56. Pleistocene stratigraphy and palaeogeomorphology in the Lower Pilica Region, Central Poland. Studia Geol. Polon., 22, 1-100. Warszawa.

SAMSONOWICZ J. 1934. Objasnlenia arkusza Opat6w og6lnej mapy geologicznej Polski. Panstw. inst. Geol.; Warszawa.

SHACKLETON N. J. & OPDYKE N. D. 1973. Oxygen isotope and palaeomagnetic strati~aphy ^of ~uatorial Pacific core V28J238: Oxygen isotope temperatu- res and ice volumes on a 10' year scale. Quaternary Res.~ 3 (1), 39--55. New York.

SIEMIRADZKI ^J., 1888. Compte rendu de recherches geologique executees en

ete

1887 aux environs de Kie1ce et de Chc:ciny. ^Pami~tn.

Fiz;ograj., 8, 3-18.

Warszawa .

. SZAJN J. 19'18. Stratigraphy of Pleistocene deposits and development of rive!

network in eastern part of the Wloszczowa basin. Kwart. Geol., 22 (1), 18-1- -t95. Wa.,rszawa.

8ZYNDLAl{ Z. 1981. Early Pleistocene reptile fauna from Kozi Grzbiet in the Holy Cross Mts. ^Acta Geol. ^Polon., 31 (1-2), 81-101. Warszawa.

WALCZOWSKI A.19'l2. Stratigraphy of Quaternary deposits of the SE part oJ.

the Holy Cross Mts region. ^Rocznik P. ^T. G. (Ann, Soc. GioZ. ^PoZogne), 42 (1), 125-134. Krak6w.

WODKOWSKI A .. 1971. Fragment d'une caverne

a

ossement de la faune pleisto- cene aux eJ.virons du mont Miedzianka - Montagnes de St. Croix. ^Speleolo- gia, 6 (1-2), ';1-47. Watszawa.

WYSOCZANSKI-MlNKOWICZ T. I960. Dating of bone remnants as a fundamen~ tal criterion for . determination of stratigraphy and chronology of tbe Pleistocene in Poland Guide-book of field seminar "Stratlgrapby and ^Chro~

nOlogy of the loesses and .glacial deposits of the lower and middle Pleisto- cene in SE Poland", pp. 23--29. Lublin.

ZUBAKOV V. A. 1978. Pozdnikainozoiskaya lednikovaya epokha: khronologiya y peryodizatsiya. Chtenya pamyati ·L. S. Berga. ^Nauka; Leningrad. '

& KOCHEGURA V. V. 1973. Khronologiya noveyshego etapa geologicheskoy

istoryi SSSR (ot 3000 000 do 60 000 let). In: Khronologiya pleystocena i klimaticheskaya stratigrafya, pp. 39-73. Geogr. Obskch. SSSR; Leningrad.

SOUTH-POLISH GLACIATIONS 171

L. LINDNER

ZLODOWACENIA POI..UDNIOWOPOLSKIE W POI..UDNIOWE,J CZ~SCI POLSKI SRODKOWE,J

(Streszczenie)

Przedmiotem pracy SIl zachowane w poludniowej CZE:SCi Polski Srodkowej (patrz fig. 1) osady i formy upowazniajllce do podzialu zlodowacenia poludniowo- polskiego (= krakowskiego, Mindel) na dwa odrE:bne zlodowacenia: Nidy (= starsza

cz~sc zlodowacenia Oki, HeZme-KaUzeit, Minde1 I) i Sanu (= mlodsza CZE:SC .zlodowacenia Oki, EZster-KaUzeit s.s., Mindel 11), kt6re oddzielone sll (patrz fig.

2-4) interglacjalem malopolskim (= Voigstedt-Warmzeit). Interglacjal ten dato- wany jest metodll FClIP i paleomagnetycZDIl oraz dokumentowany S2.CZlltkami faunistycznymi w stanowisku krasowym Kozi Grzbiet kolo Ch~cin. W obr~bie

zlodowacenia Sanu wyr6:iniono dwa stadialy: maksymalny i pomaksymalny, oddzialone okresem interstadialnym. Podczas dwudzielnego stadialu maksymalnego tego zlodowacenia Illdo16d skandynawski pokryl caly opisywany obszar i si~gal

aZ po Karpaty, natomiast w czasie stadialu pomaksymalnego objlll swym zasi~giem

jedynie p61nocnll cz~sc obszaru.