CRETACEOUS AND PALAEOGENE LITHOSTRATIGRAPHIC
UNITS OF THE MAGURA NAPPE, KRYNICA SUBUNIT, CARPATHIANS
Krzysztof Birkenmajer1 & Nestor Oszczypko2
1Institute o f Geological Sciences. Polish Academy o f Sciences, Tectonic Laboratory, ul. Senacka 3.
31-002 Kraków
2Institute o f Geological Sciences. Jagellonian University, ul. Oleandry 2a. 30-063 Kraków
Birkenmajer, K. & Oszczypko, N ., 1989. Cretaceous and Palaeogene lithostratigraphic units o f the Magura Nappe, Krynica Subunit, Carpathians. Ann. Soc. Geol. Polon.. 59: 145—181.
A b s t r a c t: The paper presents formal lithostratigraphic standard lor the Cretaceous and Palaeogene deposits o f the Magura Nappe, Krynica Subunit, Western Carpathians. It includes nine formations belonging to two groups. The Cretaceous through Lower Paleocene marine deposits (deep-water shales, flysch) belong to the Grajcarek Group and include the Hulina Form ation, the M alinowa Shale Formation, the Hahiszowa Formation and the Jarmuta Formation. The M iddle Paleocene through Lower Oligocene marine deposits (mainly flysch) belong to the Beskid Group which includes the Szczawnica Formation, the Frydman Formation, the Zarzecze Formation, the Magura Formation, and the M alcov Formation, moreover eight members; these are mainly new or redefined units.
K e y w o r d s: Magura Nappe, Krynica Subunit, Cretaceous, Palaeogene, lithostratigraphy, Carpathians.
Manuscript received April 5, 1988, accepted M ay 5, 1988
INTRODUCTION
T h e paper presents a form al lithostratigraphic stan d ard for the C retaceous th ro u g h Palaeogene stra ta o f the K rynica Subunit, M agura N appe, in the O u ter (Flysch) C arp ath ian s. A p art o f form al lithostratigraphic units in this stan d ard has already been in use for the southern p a rt o f the M agura N appe Palaeogene since 1979 (see B irkenm ajer et al., 1979; B irkenm ajer & D udziak, 1981), an d for the U p p er C retaceous o f this nappe since 1977 (M ag u ra Succession o f th e G rajcarek U nit: B irkenm ajer, 1977).
T he M agura N ap p e is the largest, highest and innerm ost o f the T ertiary thrust-sheets o f the O uter W est C arpathians. In its northen and m iddle p arts, it is com pletely u p ro o ted and th ru st over m ore external units, its lowest stra ta
10 - Annales Societ Geolog. Pol. 1-2/89
being represented by variegated shales (C enom anian —T u ronian), som etim es also by spotty shales an d m arls (A ptian — A lbian). Low er C retaceous and Jurassic deposits o f the M agura Basin have been preserved in m ore or less continuous sequences along the southern m argin o f the basin, within the
Laram ian G rajcarek U nit incorporated into the Pieniny K lippen Belt.
F o u r facies-tectonic subunits have been distinguished in the T ertiary M agura N appe o f the Polish W est C arp ath ian s (see Książkiewicz, 1948. 1958a;
Świdziński, 1953, 1961a; Sikora, 1960, 1970; Sikora & Ż ytko, 1959; Węcławik, 1969a; Oszczypko, 1973; K oszarski et al., 1974). These are, from no rth to south: The Siary ( = n o rth ern G orlice) Subunit, the R aca ( = southern Gorlice) Subunit, the Bystrica ( = Sącz) Subunit, and the K rynica S ubunit (see Fig. 1.)
Fig. 1. Geological sketch-map o f the Magura Nappe in the Dunajec River and the Poprad River valleys (after Burtan et. al., 1981, simplified and modified). Inset shows position o f the area in Poland. / — Pieniny Klippen Belt (including Grajcarek Unit); 2 —13 — Magura Nappe:
2 — Malinowa Shale Formation; 3 — “inoceramian beds” ; 4 — Szczawnica and Zarzecze formations; 5 — Frydman Formation; 6 — Palaeogene variegated shales; 7 — “ Beloveza beds” ,
“ hieroglyphic beds” and “Łącko beds” ; 8 — Magura Formation o f the Krynica Subunit;
9 — Magura Formation o f the Sącz Subunit (“ Maszkowce beds”); 10 — Magura Formation o f the Gorlice Subunit; 11 — variegated shales with Cyclammina amplectens (Mniszek Shale Member in the Krynica Subunit; „Jazowsko beds” in the Sącz Subunit); 12 — M alcov Formation; 13 — Eocene-Oligocene beds o f the Grybów Unit; 14 — Miocene o f the Sącz Basin and Mioce- nc-Pliocenc o f the Nowy Targ Basin: 15 — Mioccne andesitc intrusions; 16 — main transversal faults: 17 — main overthrusts: 18 — overthrust o f the Bystrzyca Subunit; 19 — overthrust o f the
Krynica Subunit
T his scheme is correlatable with th a t o f the Slovak C arp ath ian s. A general tendency to m ore shaly developm ent tow ards the n o rth , and increase o f sand co n ten t tow ards the south, are recognizable across these units.
T he m ajority o f lithostratigraphic units described in this p ap er have been defined after type localities situated within the Polish territory o f the M agura N appe: K rynica S ubunit and the Pieniny K lippen Belt (G rajcarek U nit). F o r som e units whose geographical nam e derived from the neighbouring area o f the Slovak C arp ath ian s, we propose form al designations, bearing how ever in m ind th a t p ro p er definition according to lithostratigraphical code rules should be coined by o u r Slovak colleagues.
F o rm al lithostratigraphic stan d ard s introduced for the Pieniny K lippen Belt (B irkenm ajer, 1977), and for the T a tra M ou n tain s (Lefeld et al., 1985) proved to be o f great help for geologists in p rom oting uniform , com parable description o f particu lar M esozoic units in the W estern C arpathians. We hope th a t the new stan d ard presented here for the K rynica S ubunit o f the M agura N ap p e o f the W estern O uter C arp ath ian s (Flysch C arpathians) will help in tro duce som e o rd er into hitherto quite unruly stratigraphic description o f this p a rt o f the Flysch C arp ath ian s, and will stim ulate sim ilar revisions o f lith o stratig rap h y in o th er p arts o f the M ag u ra N appe b oth in P oland and a b ro a d , and the rem aining p arts o f the Flysch C arp ath ian s as well.
T he present p ap er is a con trib u tio n to the Intern atio n al Geological C orrelation Project No. 198: “Northern Margin o f the Tethys".
LITHOSTRATIGRAPHIC GROUPS, FORMATIONS AND MEMBERS
T hree ranks ^of form al lithostratigraphic units will be used: groups, form ations and mem bers. O ur form ations, as a rule, are m appable units; the sam e m ay be said o f m any mem bers, how ever difficulties with detailed stratig rap h y in some unfossiliferous or p o o r in fossils flysch strata will often severely limit the practical use o f the m em bers in som e areas. Only new form al lithostratigraphic units will be described in full. T hose already defined and in c u rren t use, will be treated briefly an d reference will be m ade for p ro p er publications.
GRAJCAREK GROUP
R e m a r k s . The G rajcarek G ro u p has been defined by B irkenm ajer (1977) to include the following Low er an d U p p er C retaceous lithostratigraphic units o f fo rm atio n rank, in the area o f tectonic co n tact o f the M ag u ra N appe (southern p a rt o f this unit) with the Pieniny K lippen Belt (G rajcarek Unit): (1) the W ronine F o rm atio n (A lbian); (2) the H ulina F o rm atio n (A lbian —Ceno-
m anian); (3) the M alinow a Shale F o rm atio n (C enom anian — C am panian); (4) the H ałuszow a F o rm atio n (C am panian?), and (5) the Ja rm u ta F o rm atio n (M aastrichtian, possibly also highest C am panian). F u rth e r w ork has added m ore in form ation as to stratigraphic age-ranges o f p articu lar form ations; this will be m entioned below w ith respect to those form ations w hich are also distinguishable in the K rynica Subunit o f the M agura N appe, i.e., the H ulina F o rm atio n , the M alinow a F o rm atio n , the H ałuszow a F o rm atio n , an d the Ja rm u ta F o rm atio n (T ab. 1).
H ULIN A FORM ATION
R e m a r k s . T he H ulina F o rm atio n (B irkenm ajer, 1977) includes two m em bers: the G ro ń R adiolarite an d the U bocz Shale M em ber. T he Groń Radiolarite M ember (lower) consists o f black to green radiolarites and rad io laria shales o f small thickness (2 — 6 m). T he Ubocz Shale M ember (upper) consists o f black, grey an d green argillaceous shales w ith m enilite-type-, bentonitic-, an d m anganese-oxide-coated shale intercalations o f equally small thickness (1.5 — 5 m). These tw o m em bers are typically developed in the G rajcarek U n it along the n o rth ern b o rd er o f the Pieniny K lippen Belt where they represent A lbian an d C enom anian.
In th e K rynica S u b u n it o f the M ag u ra N appe, the H ulina F o rm atio n has been encountered in the O bidow a IG-1 borehole (2453 — 2510 m, see Ciesz
kowski & Sikora, 1976): here belong green spotty shales and d ark m udstones with infrequent intercalations o f thin-bedded, fine-grained m icaceous san d stones with T bc Boum a sequences.
In the Sącz S ubunit o f the M ag u ra N appe, the only equivalents to the H ulina F o rm atio n seem to be represented by green sp otty m arls know n from the southern m argin o f th e M szana D o ln a T ectonic W indow (B u rtan et al., 1978; B urtan & Ł ydka, 1978) believed to represent the A lbian (?) and C eno
m anian.
M ALINOW A SH ALE FO RM ATION
R e m a r k s . T he M alinow a Shale F o rm atio n (B irkenm ajer, 1977) is re
presented by red and green, often alternating, argillaceous, som etim es also m arly shales, w ith thin greenish fine-grained turbidite-sandstone intercalations.
T here occur also, locally, biotite-feldspar tuffite intercalations. T he age o f the M alinow a Shale F o rm atio n is well established on m icrofauna, m ainly arenace
ous foram inifera w ith scarce plan k to n ie ones, in the G rajcarek U n it o f the Pieniny K lippen Belt: there it represents the L ate C enom anian th ro u g h Early C am panian tim e span (B irkenm ajer & G eroch, 1961; Jednorow ska, 1980).
F o u r stratigraphically im p o rtan t successive foram iniferal assem blages have been distinguished (B irkenm ajer et al., 1987):
I ! OUJ
V) t—
if)
ZONE
N P I N D EX
P I E N I N Y K L I P P E N B E L T
M A G U R A N A P P E ' - K R Y N I C A S U B U N I T
P E R I - K L I P P E N Z O N E I SOUTHERN - CENTRAL ZONE I NORTHERN ZONE
N P
S p h e n o lith u s cip e ro en sis S p h e n o lith u s
_ d is te n tu s___
S p h e n o lith u s __p r e diste n t us H e licosphaera
__ re t i c u la ta E r ic s o n ia
s u b d is tic h a
1---T ' !
i ! i ■' : r_H~r
i ! 1 i ' i ■: i ! i
j j ( u n k n o w n ) I
I T T
I .
S p h enolithus pseudoradians Is th m o lith u s
r e c u rv u s
I I
C h ia s m o lith u s ___ o o m o ru e n sis D iscoaste r __ soipanensis
C h ia s m o lith u s __ s o litu s ___
Chiphragm alithus a I a t us____
Discoaster sublodoensis Discoaster
__ lodoensis _ M arthasterite s ____ tribrachiatus
i u n k n o w n )
; : . h ' I ! I .11
M A L C O V F O R M A T IO N S M E R E C Z E K S H A L E MBR M A LC O V F O R M A T IO N LE LU C H rfW MARL MBR
P O P R A D S A N D S T O N E M E M B E R
I I 1 I II
Discoaster binodosus
______ L —l 7 i l j . i l x . L L M A G U R A F O R M A T IO N : PIW N IC 2N A SA ND STO NE
___v M EM BER
M N IS Z E K
(?) S H A L E
M E M B E R
PIWNICZNA
S A N D S T O N E M E M B E R
10 Marthasterites contortus Discoaster __ m ult i r adigtus H e liolithus
n e d e li D iscoaster
__ gemm e u s ___
H eliolithus Klei n p e l l i __
Fasciculithus tympgnifprmis E liipsol ithus __m acellus ____
Chiasm olithus danrcus Cruciplacol ithus
tenuis_____
M arkalius inversus
t/jC K O MRL
Z A R Z E C Z E / s z cZ A Wn'iCA - FORMATION / FO RM ATIO N
(ZtA T N E MBR)
| M b a s a l c o n g l . ! , !
■ i ; j 11! | 1 i 11; ; ■! ,
( f o l d i n g a n d e r o s i o n ) I I
■ i ;! i
FRYDMAN
>
P I W N I C Z N A S A N D S T O N E M E M B E R
x ---\ <ŁĄCK0 MRt> ZARZECZE /K R Y N IC A V
<ŻYCZĄNgW > --- F O R M A T IO N \ MBR
t\C K O MRL
S Z C Z A W N I C A F O R M A T I O N
! ! '
LATE
MIDDLE EARLY
Abathomphalus mgygroensis Gansserina
gansseri __
Globotruncana ta lsostuarti
i , .
J A R M U T A FORMATION
( fo ld in g b a s a l r Pu STELN,‘A i ; ' congl. j MARL MBR
a n d T' j' ~
J A R M U T A
F O R M A T I O N
LATE
MIDDLE
EARLY
G lobotruncana c a lc a rg ta ___
G lobotruncana __ v e n tn co sa __
G lo b o tru n ca n ita e le v a ta
e r o s i o n )
(?).
J .
( f o l d i n g a n d .
e r o s i o n ) - j HAŁUSZOWA
'FORMATION
I
D ic a rin e lla ___ asymmet r i c a
iPUSTELNIA I MARL MBR K L IP P E N S U C C E S S IO N S
M A L I N O W A S H A L E F O R M A T I O N
J A R M U T A
F O R M A T IO N
H A Ł U S Z O W A FO RM ATIO N
M A LIN O W A S H A L E F O R M A T IO N
V e rtica l h a tchin g denotes lack o f the deposits
A n n ulcs S o c ieta tis G e o lo g o ru in 1 89
(1) L a t e C e n o m a n i a n : the oldest is the Rotalipora cushmani Z one with infrequent planktonic foram inifera Rotalipora cushmani (M orrow ), Praeg- lobotruncana delrioensis (Plum m er) and P. stephani (G andolfl), an d w ith m ore frequent benthic arenaceous foram inifera, am ong others, Hippocrepina depres- sa (Vasicek), Haplophragmoides gigas minor N auss, Thalmannammina neoco- miensis G eroch and Plectorecurvoides irregularis G eroch, m oreover with Recurvoides godulensis H anzlikova, R. primus M jatliuk and R. variabilis H anzlikova;
(2) T u r o n i a n : the next assemblage is characterized by the presence o f p lanktonic foram inifera Dicarinella hagni (Scheibnerova) know n from the T u ro n ian , and by a m ass occurrence o f arenaceous benthos w ith Uvigerinam- mina jankoi M ajzon, the latter also characteristic o f the T uronian;
( 3 ) C o n i a c i a n —S a n t o n i a n : the foram iniferal assem blage o f this age is characterized by the occurrence o f scarce calcareous plankton with Marginot- runcana coronata (Bolli), M. sinuosa P o rth au lt and M. undulata (Lehm ann);
(4) E a r l y C a m p a n i a n : this is the youngest foram iniferal assem blage of the M alinow a Shale F orm ation, belonging to the Globotruncanita elevata Zone. It includes, besides scarce planktonic zonal index (7. elevata (Brotzen), num erous arenaceous benthic foram inifera with Gov sella rugosa H anzlikova and Hormosina ovulum gigantea G eroch.
T he M alinow a Shale F o rm atio n crops o u t in the K rynica Subunit o f the M ag u ra N appe a t several localities, the best exposures recognized between Zlockie and Jastrz^bik (Fig. 8A, B) where the form ation is a t least 100 m thick (Oszczypko et al., in press); the m axim um thickness o f this form ation in the G rajcarek U nit o f the Pieniny K lippen Belt am ounts to 180 m (Birkenm ajer,
1977).
A t Zlockie and Jastrz?bik stream s, the lower p a rt o f the form ation yielded T u ro n ian and Early Senonian foram iniferal assemblages, while L ate Senonian arenaceous m icrofauna has been recognized in the Szczawniczek Stream (Oszczypko et al., in press). The M alinow a Shale F o rm atio n occurred also in deep borehole O bidow a IG-1 a t 2453-2350 m (see Cieszkowski & Sikora,
1976).
H ALUSZOW A FORM ATION
R e m a r k s . T he H aluszow a F orm ation o f the G rajcarek U nit (B irken
m ajer, 1977) represents a unit transitional from the M alinow a Shale F o r
m ation to the Jarm u ta F orm ation, developed further o ff the Pieniny C ordil
lera. It is up to 100 m thick. The form ation is represented m ainly by grey m arly shales alternating with calcareous sandstones (flysch facies); in its upper part, there appear grey-greenish m arls, 2 — 5 m thick.
T he C am panian, respectively M iddle-Late C am panian age o f the for
m atio n is based m ainly on its stratigraphic position between the M alinow a Shale F orm ation (Early C am panian Globotruncanita elevata Z one is the
youngest zone recognized there) and the Jarm u ta F o rm atio n (M aastrich- thian —Lower Paleocene). The occurrence o f scarce coccoliths (Birkenm ajer et al., 1979): Tetralithus pyramidus G ard et and T. obscurus D eflandre, is in agreem ent with the above conclusion (B irkenm ajer et al., 1987).
The H aluszow a F o rm atio n has been recognized above variegated shales o f the M alinow a Shale F o rm atio n in the Jastrz?bik Stream section near Zlockie (Fig. 8A, B), in the K rynica Subunit o f the M ag u raN ap p e (Oszczypko et al., in press). This is a 100-m thick complex o f thin-bedded bluish-grey calcareous sandstones alternating with greenish-grey, usually non-calcareous shales o f similar thickness. This complex did n o t yield any stratigraphically valuable foram inifera or coccoliths thus far. Its U pper Senonian age is suggested by its position between the M alinow a Shale F o rm atio n and the Ja rm u ta F orm ation.
JARM UTA FORMATION
R e m a r k s . The Jarm u ta F o rm atio n (Birkenm ajer, 1977) in the G rajcarek U nit is developed as flysch deposits up to 500 m thick: thick-, m edium to thin-bedded, fine- to coarse-grained calcareous sandstones alternating with m arly shales (usually subordinate with respect to sandstones), with cong
lom erate and sedim entary breccia (olistostrom e) intercalations and horizons, with a b u n d an t m aterial from Jurassic and C retaceous rocks o f the Pieniny K lippen Belt. The form ation often acquires wildflysch character close to the Pieniny C ordillera, becom ing m ore sandy further o ff it (northw ards).
F rom the flysch o f the Jarm u ta F orm ation in the G rajcarek U nit comes a p o o r assemblage o f large foram inifera: Lepidorbitoides socialis Leymerie, Pseudosiderolites vidali (Douville) and Orbitoides cf. media (d’A rchiac) deter
mined by Bieda (1935). It indicates a M aastrichtian or U pper C am panian to M aastrichtian age o f the deposit (Birkenmajer, 1977). Late Senonian small foram inifera assemblage includes arenaceous benthos Hormosina ovulum gigantea G eroch, Spiroplectammina dentata (Alth), Dorothia trochoides (M ars- son) and Marssonella oxycona (Reuss), and very scarce calcareous plankton:
Globotruncana linneiana (d’O rbigny), IGlobotruncanita cf. stuarti (L apparent) and Rosita fornicata (Plumm er) (B irkenm ajer & G eroch, 1963).
From a lower-middle p art o f the Jarm u ta F o rm atio n flysch comes a poor assemblage o f coccoliths: Tetralithus obscurus D eflandre, T. descriptus M artini and Marthas ter ites inconspicuus D eflandre (Birkenm ajer et al., 1979), in
dicating a Senonian age (B irkenm ajer et al., 1987).
F orm the upper p a rt o f the Jarm u ta F orm ation flysch with olistostrom e intercalations comes an assemblage o f coccoliths characteristic o f the NP-5 Fasciculithus tympaniformis Zone (base M iddle Paleocene): Fasciculithus tym- paniformis H ay et M ohler, Coccolithus pelagicus (W allich), C. cf. pelagicus (Wallich), C. cavus H ay et M ohler, Chiasmolithus consuetus (Bram lette et Sullivan), Markalius astroporus (Stradner), Prinsius bisulcus (Stradner), Eric- sonia sp., etc., with an adm ixture o f strongly dam aged, possibly recycled
Palaeogene forms Braarudosphaera bigelowi (G ran et B raarud) and Micran- tholithus sp., m oreover with recycled Late C retaceous coccoliths: Watznaueria barnesae (Black) and Biscutum supracretaceum (R einhardt). This assem blage is associated with single planktonie foram inifera Globigerina triloculinoides Plum m er (Birkenm ajer et al., 1987). The NP-1 through N P-4 zones o f Early Paleocene age, have n o t been recognized so far in the Ja rm u ta Form ation.
The Jarm u ta F orm ation has been distinguished in the K rynica S ubunit o f the M agura N appe in the Jastrzębik Stream section near Zlockie as a 30-m thick complex o f thick-bedded, often conglom eratic calcareous sandstones alternating with grey shale, above the H aluszow a F orm ation (Oszczypko et al., in press) (Fig. 8B). A ppearance o f red shales with Senonian-Paleocene m icrofauna above these sandstones in the Jastrzębik Stream section may suggest th a t the Jarm u ta F o rm atio n wedges o u t tow ards the no rth w ithin deep-w ater variegated shale complex.
BESK ID G R O U P (new group)
N a m e . A fter Beskid Sądecki Range, Polish and Slovak C arpathians, where the group is well exposed. P o l i s h n a m e . G ru p a beskidzka (gr).
S u b d i v i s i o n . The Beskid G ro u p is subdivided into five form ations (T ab. 1): the Szczawnica F o rm atio n , the F rydm an F o rm atio n , the Zarzecze F o rm atio n , the M agura F orm ation, and the M alcov F o rm atio n , spanning the tim e from M id-Paleocene through Early Oligocene inclusively. Some new form ations m ay be added to this scheme if other subunits o f the M agura N appe, m ore n orthern th an the K rynica Subunit, will be considered.
T h i c k n e s s . 3000 — 3500 m in the K rynica S ubunit o f the M agura N appe.
D o m i n a n t l i t h o l o g y . C alcareous sandstones and shales (sandy to shaly flysch) with subordinate coarse-grained sandstone and conglom erate inter
calations predom inate in the lower p art o f the group; massive sandstones (sandy flysch), with subordinate green and variegated shale horizons predom i
nate in the middle p art o f the group; shale-sandstone flysch strata with subordinate horizons o f m arls and m enilite-type shales (at the bottom ) occur in the upper p a rt o f the group.
B o u n d a r i e s . Lower boundary usually tectonic against the G rajcarek G ro u p in the southern p a rt o f the K rynica Subunit. Sedim entary contact, possibly with a stratigraphic hiatus, against the G rajcarek G ro u p has been recognized in the n orthern p a rt o f the K rynica Subunit.
A sedim entary hiatus corresponding to the NP-6 Zone (middle M id-Paleocene) recognized between the Ja rm u ta F o rm atio n and the Szczaw
nica F orm ation close to the Pieniny K lippen Belt (Birkenm ajer et al., 1987) m ay be an expression o f the L ate L aram ian folding in the G rajcarek U nit: the original, pre-M iocene, relationships between the Beskid an d the G rajcarek lithostratigraphic groups could have been o f angular unconform ity type.
Low er boundary transgressive in the Pieniny K lippen Belt: angular unconform ity against folded and eroded K lippen Successions and the Jarm u ta F orm ation.
Upper boundary erosional: the M alcov F o rm atio n is the term inal unit o f the flysch succession in the southern p a rt o f the M agura Basin.
A g e . M iddle Paleocene th rough Low er Oligocene.
E q u i v a l e n t s . N one.
SZCZAW NICA FORM ATION
H i s t o r y . T he Szczawnica F o rm atio n has been distinguished as the Szczawnica beds (Birkenm ajer, 1956, 1957); it included a southern facies — the Z łatne beds in the Pieniny K lippen Belt (Birkenm ajer, 1954), and a n o rth ern facies — the K luszkowce beds in the M agura N appe (B irkenm ajer, 1958, 1960a, 1962a). It has been renam ed the Szczawnica F o rm atio n by Birkenm ajer (in Birkenm ajer et al., 1979) and know n un d er this nam e since then (e.g., Birkenm ajer, 1970, 1979; B irkenm ajer & D udziak, 1981).
N a m e . A fter health-resort Szczawnica, Pieniny M ountains (Figs 1, 2).
P o l i s h n a m e . F orm acja szczawnicka (fm).
Fig. 2. Location o f type exposures o f Upper Cretaceous and Palaeogene lithostratigraphic units dealt with in the present paper, within the Pieniny Klippen Belt and the peri-Pieniny zone o f the Magura Nappe. 1 — Grajcarek Unit; 2 — Klippen Successions; 3 — Magura Palaeogene o f the Magura Nappe and the Pieniny Klippen Belt; 4 — Podhale Palaeogene o f the Podhale Depression and the Pieniny Klippen Belt; 5 — Main Tertiary overthrusts in the Pieniny Klippen Belt;
6 — Main Tertiary transversal faults; 7 — location o f type exposures; F — Frydman Formation;
H — Hulina Formation; HA — Hahiszowa Formation; J — Jarmuta Formation; M — Malinowa Shale Formation; S — Szczawnica Formation; Z — Złatne Member
T y p e a r e a . The type area o f occurrence o f the form ation is between Szczawnica and K rościenko (Fig. 2).
R e f e r e n c e s e c t i o n s . K rościenko-Łąkcica, section o f the right b an k o f th e D unajec River exposes an up p er p a rt o f the form ation (Fig. 2); the section a t Życzanowski (R zeczanowski) Stream , trib u tary to the P o p rad River, exposes m iddle p a rt o f the form ation (Fig. 3); the section in the Biała W oda
Fig. 3. Type and reference sections o f the Piwniczna Sandstone Member (PM), Zarzecze Formation (Z F ) and Życzanów Member (Ż M ) in the Poprad Valley near Rytro
Stream near Jaw orki exposes a lower p a rt o f the form ation (Fig. 2). F o r com parison see Birkenm ajer (1979, Figs 78, 79, 87), B irkenm ajer & Jednorow s- ka (1979), B irkenm ajer & D udziak (1981), Oszczypko (1973, Fig. 4; 1979, Fig. 5), Oszczypko et al. (in press, Figs 2, 4).
S u b d i v i s i o n . The southern condensed facies o f the Szczawnica F o r
m atio n within the Pieniny K lippen Belt has long been separated as the Z łatne M em ber. The n o rth ern facies o f great thickness has been treated as the K luszkow ce m em ber; for this the nam e Szczawnica F o rm atio n applies in its full extent.
T he Życzanów M em ber see p. 157 is distinguished as a form al unit in the Szczawnica F o rm atio n o f the K rynica S ubunit in the M agura N appe (Fig.
8B-E). Intercalations and lenses o f m arls com m only know n as the Ł ącko marls will be distinguished as local lithosom es w ithout form al designation (Tab. 1).
T h i c k n e s s . 20 — 70 m in the Pieniny K lippen Belt (Z łatne M em ber), m ore than 500 m in the K rynica Subunit o f the M agura N ap p e along the n o rth ern boundary o f the Pieniny K lippen Belt between K rościenko, Szczawnica and Jaw orki; m ore th an 1200 m in the PD -9 borehole a t Szczawnica (Birkenm ajer et al., 1979).
D o m i n a n t l i t h o l o g y . In the K rynica S ubunit o f the M agura N appe along the Pieniny K lippen Belt, this is a fine-rhythm ical flysch consisting o f calcareous sandstones alternating with carbonate-free or slightly calcareous (marly) shales, grey, bluish or black. The sandstones are usually fine-grained, fine- to m edium -bedded turbidites rich in cu rren t m arkings and trace fossils.
Intercalations o f fine-grained conglom erates and coarse-grained sandstones contain Lithothamnium detritus, M esozoic rock fragm ents from the Pieniny Klippen Belt, and exotic elements (Alexandrowicz et al., 1965, 1966). A ch arac
teristic feature o f the lower and m iddle parts o f the form ation close to the contact w ith the Pieniny K lippen Belt is its strong folding and brecciation resulting in a tectofacies rich in calcite veins.
In the Pieniny K lippen Belt, the thickness o f the form ation is strongly condensed: the shale intercalations become subordinate with respect to num m ulite-bearing medium - to coarse-grained calcareous sandstones (Zlatne M ember). The contact with the folded units o f the Pieniny Klippen Belt (K lippen Successions) is transgressive, often with coarse to fine conglom erate consisting m ainly o f local m aterial, 1.5 to 5 m thick, at the base (Birkenm ajer,
1954, 1958, 1970).
B o u n d a r i e s . Lower boundary — transgressive contact and angular unconform ity a t the base o f the Z latne M em ber o f the Szczawnica F o rm atio n against folded and eroded K lippen successions and the Ja rm u ta F o rm atio n in the Pieniny K lippen Belt. Low er b o undary usually tectonic due to Early M iocene folding in the n o rth ern b o undary zone o f the Pieniny K lippen Belt:
originally, there could be an angular unconform ity and a stratigraphic hiatus corresponding to the N P-6 Zone (m iddle M id-Paleocene — see B irkenm ajer et al., 1987). Sim ilar unconform ity probably occurs between the Szczawnica F orm ation and the Jarm u ta F orm ation in the n orthern p art o f the K rynica Subunit near Złockie (Oszczypko et al., in press).
Upper boundary — transition to the Zarzecze F o rm atio n b o th in the Pieniny K lippen Belt and the K rynica S ubunit o f the M agura N appe.
T ransition to the F ry d m an F o rm atio n in the K rynica Subunit between C zorsztyn and Frydm an.
F o s s i l s a n d a g e . In the Pieniny K lippen Belt, the form ation yielded num erous large foram inifera collected from fine conglom erates and co ar
se-grained sandstones o f the Zlatne M em ber: Operculina ammonea Leymerie, Nummulites planulatus L am arck, N. irregularis de la H arpe, N. nitida de la H arpe, and Assilina granulosa d ’A rchiac, indicating a Low er Eocene age o f
these beds (Bieda, 1929, 1946; see also B irkenm ajer & D udziak, 1981). The coccolith assemblages indicate the presence o f the N P-9 Z one (upper Late Paleocene) and the N P-10 Z one (lowest Early Eocene). The coccolith assem b
lage o f the N P-9 Zone includes: Discoaster gemmeus S tradner (m ost num e
rous), D. multiradiatus B ram lette et Riedel, D. barbadiensis T an Sin H ok, D.
binodosus M artini, D. ornatus S tradner, D. salisburgensis S tradner, Coccolithus eopelagicus (B ram lette et Riedel), C. pelagicus (W allich), Chiasmolithus bidens B ram lette et Sullivan, Ch. grandis B ram lette et Riedel and Heliolithus kleinpelli Sullivan. The assemblage o f the N P-10 Z one includes M arthasterites contortus (Stradner), Discoaster barbadiensis T an Sin H ok, D. multiradiatus B ram lette et Riedel, D. ornatus Stradner and Coccolithus pelagicus (W allich) — Birken
m ajer & D udziak (1988b).
In the Krynica S ubunit o f the M agura N appe, the best palaeontologi- cal-stratigraphical characteristics based on large and small foram inifera and on coccoliths comes from the area between Kluszkowce and Jaw orki, along the n o rth ern border o f the Pieniny K lippen Belt (Bieda, 1946, Birkenm ajer, 1958;
B irkenm ajer & Jednorow ska, 1979; Birkenm ajer et al., 1979; Birkenm ajer
& D udziak, 1981). The age-range o f the Szczawnica F o rm atio n is there from th e N P-7 Z one (upper M id-Paleocene) through the NP-11 Zone (m iddle Early Eocene).
The N P-7-8 zones yielded a t C zarna W oda the following coccolith assemblage: Coccolithus pelagicus (W allich), Cyclococcolithus formosus K am pt- ner, Discoaster gemmeus Stradner, Heliolithus riedeli Bram lette et Sullivan, etc.
(B irkenm ajer & D udziak, 1981), m oreover small foram inifera (m ainly cal
careous benthos) w ith planktonie form s Globigerina triloculinoides Plum m er a n d G. linaperta Finlay (Birkenm ajer & Jednorow ska, 1979), and large foram inifera Nummulites cf. fraasi de la H arpe (Bieda, 1929, 1935).
The NP-9 Zone (upper Late Paleocene) has been recognized on the basis o f p o o r coccolith assemblage from the Ł ącko m arl intercalations in the middle p a rt o f the Szczawnica F o rm atio n near H aluszow a: Discoaster multiradiatus Bram lette et Riedel and D. salisburgensis Stradner (Birkenmajer & D udziak, 1988b). T o this zone probably belongs also an assemblage o f large foram inife
ra collected from coarse- and m edium -grained sandstone intercalations, determ ined by Bieda (in Birkenm ajer, 1958; see also B irkenm ajer, 1960a, 1963a, 1965, 1979) as: Nummulites exilis Douville, N. subplanulatus H antken et M ad aras, N. praelucasi Douville, N. solitarius de la H arpe, N. pernotus Schaub, Operculina couizaensis D oncieux etc.
The N P-10 Z one (base o f Early Eocene), higher part, has been recognized on p o o r coccolith assemblages from Szczawnica and K rościenko: Discoaster multiradiatus B ram lette et Riedel, D. barbadiensis T an Sin H ok, D. binodosus M artini, M arthasterites tribrachiatus (B ram lette et Riedel), M . contortus (Stradner), etc. (B irkenm ajer & D udziak, 1981).
The N P -1 1 Zone (middle Early Eocene) has been recognized at Biała W oda (R ogacz Stream near O bidza, below Radziejow a M ount), a t the co n tact with
the Piwniczna Sandstone M em ber o f the M agura F orm ation: Coccoiithus pelagicus (W allich), Discoaster multiradiatus B ram lette et Riedel, Marthas- terites tribrachiatus (B ram lette et Riedel), etc. (B irkenm ajer & D udziak, 1981).
D i s t r i b u t i o n . The Szczawnica F o rm atio n is a com m on basal m em ber (Złatne M em ber) o f the M agura-type Palaeogene in the Pieniny K lippen Belt o f Poland. In the K rynica S ubunit o f the M agura N appe, it is well distributed along the n o rth ern border o f the Pieniny K lippen Belt in Poland, between Biała W oda-Jaw orki in the east, th rough Szczawnica and K rościenko, to Czorsztyn-K luszkow ce an d H u b a in the west (see, e.g., B irkenm ajer, 1963b, c,
1970, 1979).
In the n o rth ern p a rt o f the K rynica S ubunit o f the M agura N appe, the form ation crops o u t in the lower course o f the P o p rad River valley (Życzanów, Złockie) — see Oszczypko (1973, 1979), Oszczypko et al. (in press).
E q u i v a l e n t s . Szczawnica beds (F orm ation), Kluszkowce beds (M em ber), Zlatne beds (M em ber) o f Birkenm ajer (papers published between 1954 and 1979), Birkenm ajer et al. (1979, 1987), Birkenm ajer & D udziak (1981) are exact equivalents o f the Szczawnica Form ation as described in the present paper.
N ordliche G renzbildungen o f Uhlig (1890) and equivalent term s o f S.
M ałkow ski an d L. H orw itz (see discussion by Birkenm ajer, 1954, 1956, 1957) correspond partly to the Szczawnica F orm ation. A p a rt o f the “ Beloveza beds” , “ sub-M agura beds” and “ inoceram ian beds” o f Bogacz an d W ęcławik (1962; in Birkenm ajer et al., 1965; in U nrug et al., 1979) correlate with the Szczawnica F o rm atio n o f the present paper.
Zlatne Member H i s t o r y . See Szczawnica F orm ation.
N a m e . A fter Z łatne M o u n t (know n also as M o u n t Cisów ka) near N iedzica, Pieniny K lippen Belt (Fig. 2). P o l i s h n a m e : Ogniwo złatniańskie (og).
T y p e a r e a . M o u n tain ridge between M t Cisów ka (Z łatne M o u n t on older topographic m aps) an d T obór, near the Niedzica village (see Birkenm ajer, 1960b).
R e f e r e n c e s e c t i o n s . N one specified. The m em ber is poorly exposed in the Pieniny K lippen Belt. The m ost representative areas outside N iedzica are:
Szlachtowski W ierch south o f Szlachtowa, Stachurów ka and D urbaszka mount s near Jaw orki (Birkenm ajer & Pazdro, 1968; Birkenm ajer, 1970).
T h i c k n e s s . 20 — 70 m.
D o m i n a n t l i t h o l o g y . See under Szczawnica F o rm atio n , Pieniny K lip
pen Belt.
B o u n d a r i e s . See under Szczawnica F o rm atio n , Pieniny K lippen Belt.
F o s s i l s a n d a g e . See under Szczawnica F o rm atio n , Pieniny K lippen Belt.
D i s t r i b u t i o n . Pieniny K lippen Belt. The m em ber is well distributed, but generally poorly exposed, between N iedzica and C isów ka in Polish Spisz (see
Birkenm ajer, 1960b), then between Szafranów ka and W ierchliczka in the M ałe Pieniny (Little Pieniny) R ange (see B irkenm ajer & Pazdro, 1968; Birkenm ajer,
1970, 1979).
E q u i v a l e n t s . Złatne beds (M em ber) o f B irkenm ajer (1954—1979), Złat- ne M em ber (B irkenm ajer & D udziak, 1988b).
Życzanów Member
(new name)
H i s t o r y . The term “ sandstones and conglom erates o f Ż yczanów ” was used by Oszczypko (1979) for thick-bedded sandstones and conglom erates w hich ap p ear w ithin the Szczawnica F o rm atio n o f the K rynica Subunit. The sam e rocks were previously distinguished as “ thick-bedded sandstones” within the “ inoceram ian beds” ( = R o p ian k a beds) o f the K rynica S ubunit (Oszczyp
ko, 1973). These rocks were distinguished near Piwniczna an d Ł om nica as
“ sandstones and conglom erates o f K rynica” w ithin the “ Beloveza beds”
(C hrząstow ski & O strow icka, 1978; O strow icka, 1979) an d as the “ K rynica sandstones” w ithin the “ R o p ian k a beds” (Alexandrow icz et al., 1984).
N a m e . A fter Życzanów (or Rzeczanów) village and stream near R y tro on the P oprad River (Figs 1, 3). The Życzanów Stream is a right trib u tary to the
P o p rad River. P o l i s h n a m e . Ogniwo życzanowskie (og).
T y p e s e c t i o n . Życzanów, canyon in the lower course o f the Życzanów Stream (Oszczypko, 1973, fig. 4; Oszczypko & Porębski, 1985, fig. 88; 1986, fig. 50).
R e f e r e n c e s e c t i o n s . Ł om nica Stream a t Ł om nica Z drój an d W ier- chom la Stream a t W ierchom la (O strow icka, 1979); right bank o f the D unajec R iver at Ł ącko, above boat-crossing (Oszczypko, 1979, fig. 2).
T h i c k n e s s . F ro m a b o u t 80 m at Życzanów Stream (Oszczypko, 1973;
O szczypko & Porębski, 1985, 1986) to a b o u t 300 m on the southern slopes o f R adziejow a (according to A lexandrow icz et al., 1984).
D o m i n a n t l i t h o l o g y . T he m em ber is form ed o f conglom erate-sand- stone complexes o f the M agura F o rm atio n sandstone lithotype separated by thin- to m edium -bedded turbidite complexes o f the Szczawnica F o rm atio n lithotype. The thickness o f the sandstone-conglom erate complexes is up to 40 m, the intervening Szczawnica F orm ation-type turbidite complexes are m axim um 20 m thick. Individual layers o f conglom erate-sandstone sets are up to 5 m thick, their bases are sharp, w ith large flute an d groove casts indicating sedim ent supply from E and SE. B oum a sequences T ab dom inantę, m ore seldom are T abc, the grain size varies from fine gravel dow n to m edium sand.
C lay clasts, som etimes “ arm o u red ” , up to a dozen or so centim etres in diam eter occur. Q uartz is the dom in an t m ineral, lithoclasts and feldspar are
second in frequency, the m atrix is calcareous.
B o u n d a r i e s . Lower boundary sharp, placed at the b o tto m o f a conglo
m eratic sandstone several m etres thick, above thin- to m edium -bedded
turbidites o f the Szczawnica F orm ation lithotype. Upper boundary — transi
tion from conglom eratic sandstone to thin- and m edium -bedded turbidites o f the Szczawnica F o rm atio n lithotype (Fig. 8D).
Ag e . Paleocene, after m icrofaunal assemblages (Oszczypko, 1973; O stro- wicka, 1979; M alata in Oszczypko et al., in press); Lower Eocene, N P -10/11 Zone (D udziak in Oszczypko et al., in press).
D i s t r i b u t i o n . M ainly in the n orthern p a rt o f the K rynica Subunit, but traceable also in some areas o f the southern p a rt o f this unit close to the Pieniny K lippen Belt.
E q u i v a l e n t s . “ K rynica conglom erates and sandstones” sensu lato (Chrząstow ski & O strow icka, 1978; O strow icka, 1979; Alexandrow icz et al..
1984). In the O chotnica G ó rn a area, G orce Range, a probable equivalent is represented by thick-bedded m icaceous sandstones distinguished within the
“ inoceram ian beds” by Sikora and Żytko (1968). In the Sącz ( = Bystrica) S ubunit and the G orlice ( = R aca) Subunit, the Życzanów M em ber finds its equivalents in thick-bedded sandstones o f a higher p a rt o f the “ inoceram ian beds” (R o p ian k a beds). In the Bardejov area, E astern Slovakia (Bystrica Subunit), o u r m em ber m ay find an equivalent in the Tvarozec sandstone (N em ćok, 1980).
R e m a r k s . L enticular form o f occurrence o f the Życzanów M em ber (sandstone and conglom erate complexes) may be interpreted in term s of distributary channel sedim ent heralding the first appearance o f coarse-clastic sedim entation o f the M agura F orm ation-type sandstones (Oszczypko & P orę
bski, 1985, 1986).
ZA R ZEC ZE FORM ATION (new name)
H i s t o r y . The term “ Zarzecze beds” has been introduced by Oszczypko (1979) for the flysch stra ta in the K rynica S ubunit previously distinguished as the “ upper Paleodictyon beds” (N ow ak, 1924), “ Beloveza beds” (Świdziński, 1953, 1972), “ hieroglyphic beds” (Bogacz & Węcławik, 1969; Węcławik, 1969a,b;
Oszczypko, 1973) or “ sub-M agura beds” in the peri-Pieniny zone (Birken- m ajer, 1960a, 1962b, 1963b,c; Birkenm ajer & D udziak, 1981; sheet K rościen
ko, 1965) and in the Pieniny K lippen Belt (Birkenm ajer, 1960a,b, 1970, 1979;
Birkenm ajer & Pazdro, 1968).
N a m e . A fter Zarzecze village near Ł ącko on the D unajec River where one o f the best sections o f this form ation is exposed (Figs. 1, 4). P o l i s h n a m e . Form acja z Zarzecza (fm).
T y p e s e c t i o n . Steep right b an k o f the D unajec River valley between Ł ącko and Zarzecze village (Oszczypko, 1979, Fig. 2).
R e f e r e n c e s e c t i o n s . M iddle course o f the Życzanów Stream near R ytro (Fig. 3), “ Pod Skocznią” (below ski-jum p) Stream at K rynica (Fig. 5A).
Fig. 4. Type and reference sections o f the Piwniczna Sandstone Member (PM) and the Zarzecze Formation (Z F ) in the Dunajec River Valley between Łącko and Ochotnica
S u b d i v i s i o n . The K rynica M em ber m ay be locally distinguished within the Zarzecze F o rm atio n (Fig. 8D -F, T ab. 1).
D o m i n a n t l i t h o l o g y . A lternating calcareous sandstones, siltstones and m arly shales, grey-greenish, w eathered to yellow-orange. The sandstone to shale ratio is 1 :2 o r 1:1. T he sandstones are thin- and m edium -bedded, fine- an d very-fine-grained, with T abc and T bc B oum a sequences in the lower p a rt o f the unit, being replaced in the upper p a rt by thin and very thin turbidites with T c or, m ore seldom, T bc types. T he shales are silty, often resem bling soft m arls.
C u rren t m arkings and trace fossils are ab u n d an t, the clastic supply was from SE.
C onglom erates, pebbly m udstones and thick-bedded sandstones (K rynica M em ber) ap p ear locally in the upper p a rt o f the form ation.
T h i c k n e s s . 10 — 80 m in the Pieniny K lippen Belt, 100 — 200 m in the peri-Pieniny zone o f the K rynica S ubunit on the west (Czorsztyn —D ębno), 20 — 30 m near K rościenko, completely disappearing near Jaw orki — Biała W oda; grow ing to 600 m in the n o rth ern p a rt o f the K rynica S ubunit (Fig. 8E).
B o u n d a r i e s . Lower boundary — gradual transition to the Szczawnica F o rm atio n , placed w ithin colour change from bluish and steel-grey (calcareous m edium -bedded turbidites o f the Szczawnica F orm ation) to grey-green
1000m 0 1 2 3 4km
I_____ I_____ I_____ I_____ I_____ I
Fig. 5. Type and reference sections o f the Krynica Member (KM). Malinowa Shale Formation (MaF), Malcov Formation (MF) and Szczawnica Formation (SF) in the Poprad River Valley
(thin-bedded turbidites o f the Zarzecze F orm ation). Upper boundary — p as
sage to the M agura F o rm atio n , placed a t the transition from thin-bedded green-grey flysch to thick-bedded m uscovite sandstones (M agura Form ation).
A g e . In the n o rth ern p a rt o f the K rynica S ubunit the form ation represents Lower Eocene, as based on foram inifera (Oszczypko, 1979; M alata, in Oszczypko et al., in press); nannopl ankt on zones NP-10 through N P-13/14 (D udziak, in Oszczypko et al., in press). In the southern p a rt o f the K rynica Subunit, in the peri-Pieniny zone, the form ation represents the Low er Eocene, N P-10 to NP-11 zones (Birkenm ajer, & D udziak, 1981). In the Pieniny K lippen Belt, the form ation belongs to a lower p art o f Lower Eocene, N P-9/10 to NP-11 (lower p art) zones (B irkenm ajer & D udziak, 1988b).
D i s t r i b u t i o n . T he m ost extensive occurrence o f the form ation is in the n o rth ern p a rt o f the K rynica Subunit. T o the south, in the southern p a rt o f the K rynica Subunit, in the peri-Pieniny zone, an d the Pieniny K lippen Belt, the form ation is strongly reduced in thickness an d m ay altogether disappear, being replaced by the Piwniczna Sandstone M em ber o f the M agura F orm ation.
In the Sącz ( = Bystrica) Subunit, the Zarzecze F o rm atio n is replaced by variegated shales from Ł abow a, an d by thin-bedded flysch o f the “ Beloveza beds” .
E q u i v a l e n t s . In the K rynica Subunit, n o rth ern and central parts
— “ Zarzecze beds” , “ hieroglyphic beds” , “ Beloveza beds” , pars (see the H istory); in the K rynica Subunit, peri-Pieniny zone — “ sub-M agura beds” . The Frydm an F orm ation is a partial age equivalent o f the Zarzecze F o r
m ation, developed close to the Pieniny K lippen Belt between Czorsztyn and Frydm an. In the Pieniny Klippen Belt - “ sub- Magura beds". In Eastern Slovakia (C erhov and K ochanovce zones), the “ Beloveza beds” (Bystricka et al., 1970) are a p artial equivalent to the Zarzecze F orm ation o f the n orthern p a rt o f the Krynica Subunit.
R e m a r k s . The Zarzecze F orm ation is represented by thin-bedded distal turbidites interpreted as sediments o f outer subm arine fan (Oszczypko, 1979;
Oszczypko, 1985, 1986); they are being replaced to the south by thick-bedded turbidites o f the M agura F o rm atio n (deposits o f m iddle fan and its lobes). To the north, in the Sącz Subunit, the Zarzecze Formation is being replaced by the
“ Beloveza beds” , its lithofacies analogue, and by variegated shales from Ł abow a, representing hemipelagic sedim ent o f basin plain.
Krynica M em ber
(new name)
H i s t o r y . The “ sandstones and conglom erates o f K rynica” have been distinguished by Świdziński (1953, 1972) within the “ Beloveza beds” o f the Krynica Subunit. A nalogous deposits have also been distinguished within the
“ hieroglyphic beds” by M ochnacka and W ęcławik (1967) and W ęcławik (1969a,b), and w ithin the “ transitional beds” by Oszczypko (1973).
A thick complex o f the K rynica-type sandstones near Ł ącko has been included to the “ Piwniczna beds” by Oszczypko (1979), and distinguished as the “ Tylicz conglom erate” by W ęcławik (1986). These units have been distinguished n o t only within various lithostratigraphic units o f higher rank (“ beds” ), but also in various tectonic-facies subunits o f the M agura N appe.
W ęcławik (1969a,b) initially attributed them to the “ transitional Tylicz su b u n it” , and recently — to the southern p a rt o f the Sącz S ubunit (W ęcławik, 1986; M ochnacka & W ęcławik, 1986), while Świdziński (1953, 1972), Oszczyp
ko (1975, 1979), A lexandrowicz et al. (1984) and Cieszkowski and Oszczypko (1986) — to the Krynica Subunit.
Taking into account th a t the “ K rynica conglom erates” occur within the Zarzecze Formati on lithofacies but not within the Szczawnica Formation lithofacies, the K rynica M em ber has been distinguished in the Zarzecze F orm ation only (Oszczypko et al., in press).
N a m e . A fter K rynica health-resort where this unit has been first distin
guished and nam ed, and is know n from several good sections. P o l i s h n a m e . O gniw o krynickie (og).
T y p e s e c t i o n . K rynica, right bank o f the “ Pod Skocznią" Stream , being the right trib u tary o f the K ryniczanka Stream (Fig. 5A; see Świdziński, 1972, figs. 3, 5).
U - Annales Sociel Geolog. Pol. 1-2/89
R e f e r e n c e s e c t i o n s . Łosie village, Łosiański Stream (M ochnacka
& W ęcławik, 1986); Tylicz, left bank o f the M uszynianka Stream (W ęcławik, 1969b); Zarzecze near Ł ącko (Oszczypko, 1979, Fig. 2).
T h i c k n e s s . F rom a score or so m etres near Słotwina, K rynica area, to 200 m at Zarzecze, and 400 —500 m n ear Zlockie and Jastrzębik.
D o m i n a n t l i t h o l o g y . T hick-bedded conglom erates, pebbly m udstones and thick-bedded sandstones alternating with thin complexes o f thin-bedded green-grey turbidites. Individual pebbly m udstone beds, from 1 to 5 — 6 m thick, are often disturbed by subm arine slumping. They consist o f exotic pebbles, usually 1 — 10 cm in diam eter, well rounded, discoidal or spherical, scattered in blue-grey sandy-silty-m arly m atrix.
The conglom eratic sandstones and coarse-grained sandstones occur usually as layers from one to several m etres thick. B oum a’s sequences T ab, m ore seldom T abc, are predom inant. M axim um size o f granules and fine pebbles does n o t exceed 1 cm. M edium - to fine-grained sand grades prevail in to p p arts o f the layers, the m atrix is o f calcareous-silty type. The exotic m aterial consists m ainly o f milky quartz, plutonie, effusive and m etam orphic rocks, with a considerable adm ixture o f carb o n ate M esozoic rock fragm ents (Oszczypko, 1975). C u rren t m arkings and im brication o f pebbles indicate clastic supply from SE.
B o u n d a r i e s . Lower boundary sharp, placed a t the base o f coarse-clastic complex (often at the base o f pebbly m udstone bed), above thin-bedded turbidites. Upper boundary — gradual transition from thick-bedded sandstones to thin-bedded turbidites (with a variegated shale intercalation a t Zarzecze).
A g e . Lower Eocene, as based on small foram inifera (M alata, in Oszczypko et al., in press) and on calcareous n an n oplankton: from the NP-10/11 Z one at Zarzecze, to the N P-13/14 Z one a t K rynica (D udziak, in Oszczypko et al., in press).
D i s t r i b u t i o n . T he K rynica M em ber is characteristic o f the n o rth ern area o f the K rynica Subunit. T ow ards the south, it probably interfingers with the M agura F orm ation (Piwniczna Sandstone M em ber). In the Sącz Subunit, the K rynica M em ber wedges o u t completely.
E q u i v a l e n t s , see H istory.
R e m a r k s . The conglom erates and sandstones o f the K rynica M em ber probably represent deposits o f distributary channels w ithin m iddle subm arine fan which interm ittently supplied coarser m aterial to the outer fan deposits o f thin-bedded turbidites.
FRYDM AN FORM ATION
H i s t o r y . The u n it has been distinguished by B irkenm ajer (1954) as the
“ flysch beds o f F ry d m an ” (see also Birkenm ajer, 1963c), later distinguished as the F rydm an F o rm atio n (Birkenm ajer, 1979; B irkenm ajer & D udziak, 1981), between Czorsztyn-Ciechorzyn and Frydm an, along the D unajec River Valley.
N a m e . A fter F rydm an village on Polish Spisz (Figs. 2, 6). P o l i s h n a m e . F orm acja frydm ańska (fm).
T y p e s e c t i o n . A bandoned q u arry near the road from F rydm an to Falsztyn.
R e f e r e n c e s e c t i o n s . Exposures along the right bank o f the D unajec R iver between F rydm an and Falsztyn (Blahuty), and along the left bank o f this river between C iechorzyn an d Brzeziny near C zorsztyn (see Birkenm ajer, 1963b, 1979; Birkenm ajer & D udziak, 1981, Figs. 2B, 3A).
T h i c k n e s s . A b o u t 400 m.
Fig. 6. A. Type scction o f the Frydman Formation (F) near Frydman. 1 — Quaternary covcr.
2 — Frydman Formation; 3 — Grajcarek Unit o f the Pieniny Klippen Bell; 4 — overthrust. B.
Location o f reference sections o f the Szczawnica Formation in geological map o f Krościenko (based on Birkenmajer, 1979). 1 — Quaternary cover; 2 — Miocene andesite intrusions;
3 — Magura Formation, Piwniczna Sandstone Member; 4 — Łącko marl intercalations;
5 — Zarzecze Formation-type intercalations within the Piwniczna Sandstone Member and Zar/ecvc Formation: 6 — Szczawnica Formation: 7 — Grajcarek Unit: 8 - Klippen Successions;
y main Tertiary faults; JO — main Tertiary ovcrlhrusts; I I — relercncc sections o f the Szczawnica Formation
D o m i n a n t l i t h o l o g y . There is an altern atio n o f lithotypes, one corres
ponding to the Szczawnica F o rm atio n lithotype, and the o ther to the Zarzecze F o rm atio n lithotype: greenish, m edium - to thin-bedded, coarse, m edium - to fine-grained sandstones alternate w ith greenish to bluish m arly shales, with intercalations o f bluish calcareous, m edium - to fine-grained sandstones. There is a w ealth o f current m arkings indicating clastic supply from N E (in greenish sandstoness o f the Zarzecze F o rm atio n lithotype) and from S (in bluish sandstones o f the Szczawnica F o rm atio n lithotype), an d o f trace fossils.
G raded layers are com m on, som etimes with large foram inifera at fi
ne-conglom eratic soles, subm arine slum ping and convolutions m ay often be found.
B o u n d a r i e s . Lower boundary against the Szczawnica F o rm atio n is transitional, b u t n o t well defined due to insufficient exposures. Upper boundary
— tectonic against the n o rth ern b o u n d ary fault o f the Pieniny K lippen Belt:
originally probably transition to the M agura F orm ation.
A g e . M iddle p a rt o f the Lower Eocene, N P-11/12 and N P-12 zones (B irkenm ajer & D udziak, 1981). This age is also su pported by large foram ini
fera determ ined by Bieda (in B irkenm ajer, 1954): Nummulites pernotus paraburdigalensis Schaub, Operculina couizaensis D oncieux, Discocyclina sp.
etc.
D i s t r i b u t i o n . T he F rydm an F o rm atio n occurs between F rydm an and C zorsztyn along the n o rth ern border o f the Pieniny K lippen Belt (see Birkenm ajer, 1963b).
E q u i v a l e n t s . “ Flysch beds o f F ry d m an ” (B irkenm ajer 1954, 1963b).
R e m a r k s . The F rydm an F o rm atio n is a regional, peri-Pieniny sand- stone-shale flysch corresponding to a peripheral zone o f two overlapping fans:
the Piwniczna Sandstone M em ber (southern p a rt o f the K rynica Subunit;
Pieniny Klippen Belt) fed from the N E or E sources, and the Szczawnica F o rm atio n fan fed from the southern sources.
M AGURA FORM ATION (new name)
H i s t o r y . T he nam e “ M agura S andstein” has been introduced by Paul (1868) for thick-bedded sandstone complex o f the O ravska M agura R ange (W est Slovakia), and attrib u ted to the Oligocene (Paul, 1869). As a result, many thick-bedded sandstones o f supposedly Oligocene age were subsequently term ed the “ M agura sandstones” in the O uter (Flysch) C arpathians, e.g, those later distinguished as the “ K rosno sandstones” , “ Istebna sandstones” , “ Czar- nohora sandstones", etc., notw ithstanding the fact th a t they differed from P aul’s “ Magur a S andstein” not only in lithology and p etrographic characters, b u t also in age. U hlig (1888) restricted the use o f P aul’s term to the inner p a rt o f the W estern Flysch C arp ath ian s (“ B ergland” ). Later, after the separation o f the M agura N ap p e by Lim anowski (1905), the term “ M agura sandstone” was
restricted to the youngest lithostratigraphic unit o f this nappe only. A n o th er term , based on the original denom ination, b u t taking into account various subordinate lithologies, was the “ M agura beds” (Świdziński, 1934a; Książ- kiewicz, 1935).
Tw o m utually intertonguing lithofacies have been distinguished w ithin the
“ M ag u ra sandstone” o f the Polish W estern C arpathians by Książkiewicz (1953, 1958a): a n o rth ern one — glauconitic, and a southern one — m us
covite-bearing. The glauconitic facies o f the “ M agura sandstone” has also been recognized to the east o f the D unajec River valley (Sikora, 1960).
Since N o w ak ’s (1924) geological studies in the K rynica area, it was ap p a re n t th a t considerable facies changes take place in the M ag u ra N appe, including the “ M agura sandstone” as well. F o u r facies zones have been distinguished (Książkiewicz, 1948, 1958a; Świdziński, 1953, 1961a; Sikora, 1960, 1970; Sikora & Ż ytko, 1959; W ęcławik, 1969a; Oszczypko, 1973), com parable to those recognized in C zechoslovak C arp ath ian s (M atejka
& R oth, 1950; F usan et al., 1963) and in T ran scarp ath ian U kraine (Calyj, 1965), and shown in the tectonic m ap o f the C arp ath o -B alk an area (see K oszarski et al., 1974). These are, from n o rth to south: the Siary ( = n o rth ern G orlice) Subunit; the R aca ( = southern G orlice) Subunit; the Bystrica ( = Sącz) Subunit, and the K rynica Subunit.
In the Siary Subunit, the “ M agura sandstone” is developed in glauconitic facies (eastern part) o r as a mixed glauconitic-m uscovite facies (western unit).
In the rem aining subunits o f the M agura N appe the m uscovite facies occurs.
T he base o f the sandstone unit is diachronous, being the oldest in the K rynica Subunit and the youngest in the G orlice S ubunit (Bieda et al., 1963, 1967;
Sikora, 1970; O szczypko, 1973, 1979). T he m uscovite facies was fed from a source situated on SE, while the glauconite facies — from the N E and N sources (Książkiewicz, ed., 1962). The “ M agura sandstones” o f the K rynica Subunit and the southern p a rt o f the Sącz Subunit, belong to the same facies zone, and were fed by the same sources; their relation to the “ M agura sandstone” (m uscovite facies) o f the R aca S ubunit has n o t been solved: it is possible th a t these tw o lithosom es were separated in the n orthern p a rt o f the Sącz S ubunit by the Ł ącko m arl lithofacies (see Oszczypko et al., in press).
This was one o f the reasons to restrict ou r lithostratigraphic stan d ard to the K rynica Subunit, a t the present state o f investigation.
N a m e . A fter O ravska M agura in W est Slovakia (cf. Paul, 1869; Potfaj, 1983, fig. 2). P o l i s h n a m e : F orm acja m agurska (fm).
T y p e a r e a . O ravska M agura (Czechoslovakia), G orce and Beskid Sądec
ki ranges (Poland) — Fig. 1.
T y p e s e c t i o n (Poland). “ B aszta” C rag, a t the outlet o f the O chotnica Stream to the D unajec River, a t Tylm anow a (Figs 1, 4). See Oszczypko and Porębski (1985, figs 89, 90; 1986, figs 53, 54).
R e f e r e n c e s e c t i o n s . Z abrzeź on the D unajec River (Oszczypko, 1979), m iddle p a rt o f the Życzanów Stream (Oszczypko, 1973, fig. 4).
