Upper Maastrichtian and Paleocene deposits at Szaflary, Pieniny Klippen Belt, Carpathians, Poland

R O C Z N I K P O L S K I E G O T O W A R Z Y S T W A G E O L O G I C Z N E G O A N N A L E S D E L A S O C I É T É G É O L O G I Q U E D E P O L O G N E

V ol. XLVIII — 1: 27—37 K raków 1978

Stefan W. A l e x a n d r o w i c z 1, Krzysztof B ir k e n m a j e r 2

UPPER MAASTRICHTIAN AND PALEOCENE DEPOSITS AT SZAFLARY, PIENINY KLIPPEN BELT,

CARPATHIANS, POLAND

<4 Pig., 1 Tab.)

U tw ory górnego mastrychtu i paleocenu w Szaflarach, pieniński pas skałkow y

■ (4 fig., 1 tab.)

A b s t r a c t : At the contact of the Pieniny Klippen Belt with th e Podhale Flyseh (Palaeogene) at Szaflary (Polish Carpathians), occur late Maastrichtian and Paleocene deposits of small thickness, characterized by aibundant, pre­

dominantly planktonie foraminiferal assemblages, developed in a facies unknown from the Klippen successions in Poland. These deposits correspond to a zone known in Slovakia as the „peri-KBppen” zone, resp. Myjava Furrow, which was situated to (the south of the Klippen Belt basin and its southern exotic massif, and to the north of the folded Central Carpathian (Su'b-Taitric and High-Tatric) units.

INTRODUCTION

A t the contact of th e Pieniny K lippen Belt and th e Podhale Palaeo­

gene flyseh a t S zaflary (Polish C arpathians), occur late M aastrichtian and Paleocene deposits developed in a facies unknow n from the K lip­

pen successions of Poland. These rock’s a re younger than th e young­

est ilithostratigrap'hic u n its of 'the K lippen successions, w hich are re p ­ resented by preorogenic flyseh of the Sromowce Form ation (Coniacian to Low er Cam panian — see B i r k e n m a j e r , 1977) in the southern tectonic units, and by pelagic Globotruncana marlis of the P ustelnia M arl M ember (Turonian to Lower M aastrichtian — see A l e x a n d r o ­ w i c z , 1975; B i r k e n m a j e r , J e d n o r o w s k a , 1976; B i r k e n ­ m a j e r , 1977) in the northernm ost p a rt of the geanticlinal Czorsztyn Succession.

1 Instytut Geologii i Surowców Mineralnych AGH, al. MLokiewicza 30, 30-059 Kraków.

8 Zakład Nank Geologicznych PAN, ul. Senacka 3, 31-002 Kraków.

— 28

The Paleöcene rooks a t S zaflary have been recognized in 1964 by D u r a n d - - D e l g a (1965) on m icrofaunal investigation by J. M a g- n é. Sm all outliers of the C am panian-M aastrichtian, Paleocene (?) and Eocene-Oligocene rocks of small thickness, have been traced w est of Szaflary, along the boundary of the Pieniny K lippen B elt w ith the Podhale Palaeogene, by M o r g i e l and S i k o r a (1972, 1973). The sequence discussed differs both in age and in facies from those recog­

nized in th e K lippen successions ( B i r k e n m a j e r , 1965, and la ter papers), and represents an independent succession w hich w as a ttrib u ­ ted to th e so-called „Złatne succession” by M o r g i e l and S i k o r a (op. cit.), b u t correlated w ith the M yjava succession of W est Slovakia by B i r k e n m a j e r (1977, p. 140). T h e M aastrichtian u n it of the succession is p artly coeval w ith the M aastrichtian flysch and molasse of the J a rm u ta Form ation, w hich is rep resen ted by coarsely to fine- -d etrital clastics w ith abundant rock m aterial from the K lippen succes­

sions as secondary deposit, and w hich was deposited unconform ably upon folded K lippen successions and, besides, in th e M agura basin (G raj­

carek U nit — see B i r k e n m a j e r , 1965, 1970, 1977) — to the n o rth of the Czorsztyn geanticline.

Fig. 1. Location of Szaflary w ithin the Pieniny Klippen Belt. 1 — Magura Nappe;

2 — Podhale Flysch; 3 — Pieniny Klippen Belt; 4 — Northern and southern tec­

tonic boundaries of the Pieniny Klippen Belt

Fig. 1. Położenie Szaflar w pienińskim pasie skałkowym. 1 — płaszczowina magur­

ska; 2 — flisz podhalański; 3 —• pieniński pas Skałkowy; 4 — północna i połud­

niowa granica tektoniczna pienińskiego pasa skałkowego

The p resen t paper gives the resu lts of lithologie and m icrofaunal investigations of a section exposed along the rig h t bank of the D una­

jec River a t Szaflary (Fig. 1), at the southern contact of the P ieniny K lippen Belt. The field w ork fwas done in 1969.

LITHOLOGY, MICROFAUNA AND AGE OF THE DEPOSITS

The section along the rig h t bank of the Biały D unajec River expo­

ses several! U pper Cretaceous lilt bostratigraphic u n its of th e P ieniny Succession (Fig. 2: 6— S) on the north, and a 25 m thick com plex of

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M aastrichtian and Paleocene rocks on the south, at the contact w ith the Podhale Flyseh (Zakopane Form ation, U pper Eocene). The rocks are vertical or dip at v ery steep angles to the south or to the north, and are often recum bent. The M aastrichtian-Paleocene complex is re p re-

AGE

M ID D L E

PALEOCENE

Fig. 3. Lith-ostratigraphie coluimn of the Upper Maastrichtian and Middle Paleocene sediments at Szaflary, f — Tectonic contacts

Fig. 3. Kolumna lit o stratygraficzna osadów górnego mastrychtu i środkowego paleo­

cenu w Szaflarach, f - kontakty tektoniczne

sen ted by tw o lithostratigraphic u n its of form ation rank: the older m arly com plex (with sa n d sto n e-sed im en ta T y b reccia intercalation in th e middle) w hich yielded U pper M aastrichtian foram inifers, and the youn­

ger, shaly com plex w hich yielded Paleocene foram inifers (Fig. 3).

U p p e r M a a s t r i c h t i a n Unit 1 (8 m)

The oldest p art of the M aastrichtian complex tectonically contacts w ith the Podhale Flyseh (Zakopane Form ation, U pper Eocene) w hich is o verturned in a narrow zone adjoining the contact, then (further south) it dips norm ally tow ards the south. The M aastrichtian u n it 1 is re p re ­ sented by pale-grey, pale-green, w hitish w eathered, strongly cleaved m arls and m a rly lim estones (Fig. 2: 1).

Ten sam ples for m icrofauna w ere taken. The microfossils w ere dif­

ficu lt to separate from hard m arls and m arly limestones, w here they w ere often deformed, and only so fter m arls yielded determ inable forms. The dom inant elem ent of the m icrofaunal spectrum (Tab. 1: as­

semblage 1) is represented by planktonie forms, of w hich G lobotrun- cana stuartiform is Dalbiez is the m ost common, and is associated w ith stratigraphically im portant G. stuarti (Lapparent), G. conica W hite, Abathom phalus mayaroensis (Bolli) and P seudotextularia spp. Of th e

Microfaunal spectra of the Upper Maastrichtian (units 1, 3) and Middle Paleocene (unit 4) pelagic sediments from Szaflary

s _ sin gle; r — rare; f — few ; c — com m on; a — abundant

T a b l e 1

Species Ldfchostratigraphic unit: 1

Assemblage:

Reophax sp.

Hormosina ovulum ((Grzybowski) Nodellum velascoense (Cushman)

Glomospira charoides (Jones et Parker) Glomospira gordialis (Jones et Parker) A m m odiscus siliceus (Tenquem)

Trochamminoides irregularis White Textularia. plum merae Lalicker

Spiroplectam m ina semicomplanata (Carsey) Gaudryina of. pyram idata Cushman

Tritaxia tricarinata Reuss Areno bvlim ina sp.

Dorothia bulleta Carsey Dorothia trochoides (Marsson) Leniicidina maorodisca (Reuss)

Lenticulina milcoxensis (Cushman et Ponton) Astacolus compressas (d’Orfoigny)

Vaginulina trilobata (d’Orbigny)

Neoflabellina cf. numdsmalis Wedekind Pseudoglandulina parallela (Marsson) G yroidinoides nitidus (Reuss)

Stensioeina caucasica (Subbotina.) Stensioeina pommerana Brotoen Eponides cf. franhei Brotzen Anomalina cf. w elleri (Plummer) G avelinella pertusa (Marsson)

Pseudovalvulineria cf. praeacuta Vassilenko Cibicidoides cf. actulagayensis Vassilenko

Globigerina triloculinoides Pllumimer Globorotalia aegua Cushman et Renz Globorotalia angvlata (White)

Globotruncana area (Cushman) Globotruncana contusa -(Cushman) Globotruncana conica White Globotrunca-na of. gagnebini Tilev Globotruncana ganss&ri B elli Globotruncana stuarti (Dapparemt) Globotruncana stuartiform is Dadbiez Abathom phalus m ayaroensis (BoLli) Rugoglobigerina rugosa (Pllummer) Reussella szajnochae (Grzybowski) Pleurostomella sp.

Aragonia ouezzanensis (Rey) Bolivina incrassata Reuss

Bolivinoides giganteus Hiiltermann et Koch Pseudotextularia acervulinoides (Egger) Pseudotextularia elegans (Rzehak) Pseudotextularia varians (Rzehak)^

1

r s r s s r s s s s s s r

f f

f

s r r c r f s s

s r f

s r s s s s r s s s s s s

s r s s r

s r c s s s s s s s

s s r s

r s s s s s s s

a r c

— 32 —

benthie form s, th e m ost characteristic are: Gavelinella pertusa (M ars- son), Stensioeina pom m erana Brotzen, S. caucasica (Su'bbotina) and Reussella szajnochae (Grzybowski). T he variation w ith in th e foram ini- ferai 'spectrum betw een the sam ples is negligible, and depends on the percentage of benthos (10—20%). The assemblage indicates th e U p p er

• M aastrichtian, possibly the latest U pper M aastrichtian, age of the marls.

U nit 2 (4 m)

The u n it sta rts w ith a sedim entary breccia (0.1 m) composed of w hitish or greenish m arl fragm ents (0.5—2 cm in diam eter) of the same type as th a t of the underlying u n it 1, fine fragm ents of Inoceramus shells and of quartz grains. The colour of the rock is grey-green. There follow several thin layers (2— 10 cm thick) of grey, grey-blue, fine to m edium -grained calcareous sandstone, passing at th e top to arenaceous m arl. - Sm all fragm ente of w hite to green m arl of th e same tyipe ais th a t of the first unit, are freq u en tly m et w ith in the basal, graded p a rt of th e sandstone layers. The highest p a rt of the u n it is form ed by two layers of grey-bluish or grey-green, fine to m edium -grained calcareous sandstone, w ith w ell developed norm al graded bedding m arked by coar­

ser quartz grains at th e sole (facing south) of the higher layer.

No m icrofauna has been obtained from the sandy-brecciose com­

plex. The rocks resem ble very m uch th e M aastrichtian Orbitoid-foearing breccias and sandstones of W est Slovakia.

Unit 3 (10 m)

The youngest p art of the M aastrichtian com plex is represented (from the bottom to the top) by: a) cleaved m arls and shaly lim estones, grey-green, w eathered pale-grey (6 m); b) shaly m arls, pinkish-grey, greenish and variegated (2 m); c) soft shaly m arls, grey-green (2 m).

The m icrofaunal assemblages investigated from 6 samples w ere ge­

nerally very sim ilar to those from the lower m arls (unit 1). P articu larly freq u en t is Globotruncana contusa (Cushman), besides Rugoglobigerina rugosa (Phiimmer), less fre q u en t are foram inifens of th e genus Pseudo- textularia. The benthos is represented i.a. by N odellum velascoense (Cu­

shman), Eponides cf. fra n kei Brotzen, Aragonia ouezzanensis (Rey) and Bolivina incrassata Reuss (Tab. 1: assemblage 2). The ratio of plankto­

nie to benthie form s is sim ilar to th a t of the low er m arls (unit 1). The assem blage indicates th e U pper M aastrichtian age of the unit.

P a l e o c e n e Unit 4 (10 m)

T he u n it consists of soft m arly shale and shaly m arl, cherry-red, som etim es variegated. The planktonie foram inifers investigated from 9 samples, decidedly predom inate (90% of the assemblage) over benthie

ones. The plankton is represented by th ree species, p articu larly im por­

ta n t fo r determ ination of the age of u n it 4: Globigerina triloculinoides P lum m er (Fig. 4: 2a-c), Globorotalia angulata (White) (Fig. 4: la-c) and G. aequa Cushm an et Renz (Fig. 4: 3a-c). The firs t species occurs in all investigated sam ples w here it form s 60—70% of th e whole assem ­ blage, th e second species is less common in th e same sam ples, th e th ird one occurs only in the stratigraphically highest samples. The bemlthic form s are subordinate, the m ost common are arenaceous form s G lomos- p ira a n d Am m odiscus; calcareous 'benthos is ra re (Taib. 1: assem ­ blage 3).

— 33 —

Fig. 4. Planktonie foraminifers from the Middle Paleocene at Szaflary, la—c — Globorotalia angulata (White); 2a—c — Globigerina triloculinoides Plummer; 3a—c —

Globorotalia aeąua Cushman et Renz

Fig. 4. Planktoniozne otw om ice z środkowego paleoeenu Szaflar, la —c — Globoro- talia angulata (Wbite); 2a—c — Globigerina triloculinoides Plu/mimer; 3a—c — Glo­

borotalia aequa Cushman et Renz

The presence of Globigerina triloculinoides (Lower-M iddle Paleoce­

ne) and Globorotalia angulata (zonal index for the Middle Paleocene) in the low er samples, a n d together With G. aequa (M'iddle-Upper Paleocene and Low er Eocene) in the upper samples, clearly indicate a Middle P a­

leocene (Landenian) age of u n it 4: Globorotalia angulata Zone, resp.

G. pusilla pusilla Zone (early Landenian), and lower p art of G. aequa

3 — R ocznik PT G XLVIII/1

— 34

Zone (M e Landenian to early Ilierdian), recognized over wiide areas of the T ethys ( P o s t u m a , 1971), including the W est C arpathians of Slo­

vakia ( S a m u e l , S a l a j , 1968) and P oland (J e d n o r o w s k a , 1975).

It should be noted th a t J. M a g n é (in D u r a n d - D e l g a , 1965) recognized th e following foram inifers in a sam ple taken from u n it 4:

Truncorotalia (= Globorotalia) aequa C ushm an et Renz, T. angulata W hite, T. gr. velascoensis Cushman, T. aff. re x M artin, Globigerina cf. lina- perta Finlay, G. triangularis W hite, G. velascoensis Cushman, and o th ­ ers (not listed). Magné w as of th e opinion th a t th is mîcroÆaïuna is „cer­

tainem ent éocène e t très probablem ent d u Paléocène su p érieu r”.

CONCLUSIONS

1. The U pper M aastrichtian and Paleocene (Landenian) units a t Sza­

fla ry are w ell defined by th eir m icrofaunal assemblages and lithology, and may be tre a ted as two separate lithostratigraphic units of fo rm a­

tion rank. The u n its are left unnam ed u n til fu rth e r investigation.

2. The tectonic contacts a t the bottom of the M aastrichtian m arls and a t the top of the Paleocene shales, separate th e succession from both th e Podhale Flysch (Zakopane Form ation: U pper Eocene) and th e U pper Cretaceous lithostratigraphic units of the Pieniny Succession. The M aas- trichtian-Paleocene rocks and th e ir m icrofauna show close analogies w ith the so-called „peri-K lippen” Senonian-Palaeogene succession of East and W est Slovakia (see S a m u e l , 1972; A n d r u s o v , S a m u e l , 1973) w hich occur a t the southern m argin of the P ieniny K lippen Belt, at the contact w ith C entral C arpathian tectonic u n its of U pper C reta­

ceous age, and Inner-C arpatbian Palaeogene.

3; The appearance of rew orked M aastrichtian mauls as fragm ents in fine-grained sedim entary breccia and fine-imediiuin grained, graded sandstone, is explained as the effect of bottom erosion iby tu rb id ity c u r­

ren ts w hich tem porarily in te rru p ted pelagic maul sedim entation in th e M aastrichtian, to form fine-clastic tutfbidites.

4. Based on lithology, th ere seems to be a passage from the U pper M aastrichtian m arls, w hich become pinkish-grey and variegated in the upper p art, to the Paleocene ch erry -red shales at Szaflary. H owever, the lack of Low er Paleocene (Danian and M ontian) m icrofaunal indices in the ch erry -red shales, would ra th e r suggest a tectonic hiatus or non- -deposition a t the contact of units 3 and 4.

5. Com pared w ith coarsely-detrital developm ent of the M aastrichtian Ja rm u ta Form ation (molasse and flysch — see B irkenm ajer, 1977) of the Pieniny K lippen Belt of Poland in the nearest vicinity at Szaflary (about 1 km tow ard the north), the pelagic sedim entation of marls, m a r­

ly lim estones and m arly shales at the boundary of Cretaceous and P a-

— 35 —

laeogene, represented by- th e succession here 'described from Szaf'lary, indicates that these plankton-rich, open-sea sedim ents w ere laid down in a géosynclinal fu rro w not affected by folding at the Cretaceous-Ter­

tia ry boundary. The palaeotectonic position of this zone would be to the south of the already folded Klippen B elt arc and its southern Exotic Massif (which was the m ain source of clastics supplied to the Pieniny K lippen B eit (basin during 'the A ptian th rough M aastrichtian), Ibu't to the n o rth of the folded C entral C arpathian zone {Sub-Tatric and High- -T atric nappes of the Slovakian Block), w ithin the M yjava Furrow sensu S c h e i ' b n e r (1968, Fig. 2).

6. The M aastrichtian m arls 7.6 m thick described by M o r g i e l and S i k o r a (1972, p. 1054) from the left bank of th e B iały D unajec Ri vor at Szaflary ( M o r g i e l and S i k o r a , 1972, p. 1053, erroneously w rite

„right b ank”, but from the te x t of their paper „w est of Biały D unajec”

it is clear th a t th e y re fe r to the left bank), are a close equivalent of the m arls from the rig h t b an k here described.

7. The flysch-flyschoid and shaly developm ent of the Cam panian- -M aastrichtian, ?Paleocene and Eocene-Oligocene age, described from the area of the S krzypny stream near M aruszyna (west of Szaflary) by M o r g i e l and S i k o r a (1972, p. 1054; 1973, p. 641), should also belong to the „peri-K lippen” ve.l M yjava F urrow zone. T aking into ac­

count strong tectonic reductions, it cannot be solved a t p resen t, w hether the succession from the S krzypny stream belongs to the same succession as th a t from Szaflary, or the differences observed are caused by the presence of d ifferent lithostratigraphic units in these two sections.

8. The M aastrichtian-Paleocene sequence at Szaflary, and the Cam- panian-M aastrichtian, ?Paleocene and Eocene-Oligocene sequence of the S krzypny stream , w ere included by M o r g i e l and S i k o r a <1972, 1973) to the „Z łatne succession” sensu S i k o r a (1969, 1971) which, in his opinion, represents a continuous sequence of Jurassic through Oli- gocene sedim ents typical fo r the southernm ost p art of the Pieniny K lippen Belt of Poland. However, as already m entioned by B i r k e n ­ m a j e r (1977, p. 11), S i k o r a ’ s „Złatne succession” is a heterogeneous unit. It includes both th e earlier defined K lippen successions (Jurassic through Upper Cretaceous), the Palaeogene m antle of the K lippen suc- cessons, and th e ,,peri-K lippen” (vél M yjava Furrow ) Senonian-Pallaeo- gene successions. The continuous passage from the Cretaceous to the T ertiary, though n o t (proven so far, m ay be assum ed in P oland only for the zone of th e „peTi-Klippen” (Myjava) tectonic scales, b u t not for the rest of the Pieniny K lippen Belt, w here th ere is an im portant hia­

tus betw een the folded Jurassic to Cam panian Klippen successions and the M aastrichtian Ja rm u ta Form ation (molasse and flyseh), resp. th e transgressive Low er Eocene conglom erate-flysch sequence of the K lip­

pen M antle (see B i r k e n m a j e r , 1970, 1977).

9. The p resen t fragm ental occurrence of the M aastrichtian to P a ­ laeogene pelagic rocks of sm all thickness along th e so uthern boundary of the P ieniny K lippen B elt in the C arpathians, is the resu lt of the early Neogene (Savian) folding.

ACKNOWLEDGEMENTS

The authors are indebted to Prof. D r Michel D urand-D elga (Labo­

rato ire de Géologie m éditerranéenne, Toulouse, France) who most kin -

*dly supplied detailed inform ation as to ithe localization of bis sam ple w ith Paleocene m icrofauna at Szaflary.

M anuscript received March 1977, accepted A pril 1977

— 36 —

REFERENCES — WYKAZ LITERATURY

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A n d r u s o v D., ( S a m u e l O. (1973), Cretaceous-Palaeogene of the West Car­

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B i r k e n m a j e r K. (1965), Zarys budowy geologicznej pienińskiego pasa skałko­

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ków.

B i r k e n m a j e r K. >(1970), Przedeoceńskie struktury fałdowe w pienińskim pasie skałkowym Polski (iPre-Eooene fold structures in the Pieniny Klippen Belt, Car­

pathians, of Poland). Stud. geol. pol., 31: 1—77. Warszawa.

B i r k e n m a j e r K. (1977), Jurassic and Cretaceous lithostratigraphic units of the Pieniny Klippen Belt, Carpathians, Poland. Stud. geol. pol., 45: 1—^159. War­

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STRESZCZENIE

Na kontakcie pienińskiego pasa skałkowego z fliszem podhalańskim w Szaflarach w ystępują osady górnego m astrychtu (białawe m argle i w apienie m argliste z w kładką brekcji sedym entacyjnej i frakcjonow a­

nych piaskowców) i środkowego paleocenu (czerwone łupki i m argle łupkow ate) o m ałej miąższości, z obfitą, w przewadze planktoniczną, m ikrofauną otwornicową. Facjalnie osady te są różne od osadów suk­

cesji skałkowych w Polsce. Odpowiadają one strefie znanej w Słowacji jako strefa „peri-skałkow a” lub bruzda m yjaw ska, która w utjęciu pa- leotektonicznym znajdow ała się na południe od basenu skałkowego i je­

go południowego malsywiu egzotycznego, natom iast na północ od sfałdo- w anych jednostek centralnokarpackich (reglowych i wierchowych).

W istrefie 'tej je st możliwe ciągłe przejście od utw orów kredow ych do palleoceń^kich, jednakże — jak dotychczas — osady dolnego paleocenu (danu i m ontu) nie zostały w Polsce rozpoznane na podstaw ie zespołów m ikrofauny.