GeolCarp_Vol60_No4_283

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA, AUGUST 2009, 60, 4, 283—294 doi: 10.2478/v10096-009-0020-5

Latest Maastrichtian foraminiferal assemblages from the
Husów region (Skole Nappe, Outer Carpathians, Poland)

M. ADAM GASIŃSKI and ALFRED UCHMAN

Institute of Geological Sciences, Jagiellonian University, Oleandry Str. 2a, PL-30-063 Kraków, Poland;

adam.gasinski@uj.edu.pl; alfred.uchman@uj.edu.pl

(Manuscript received August 25, 2008; accepted in revised form December 18, 2008)

Abstract: The Ropianka Formation (also known as the Inoceramian Beds) in the marginal part of the Skole Nappe
(Husów region, the Gaj section) contains abundant, diverse and well preserved assemblages of Maastrichtian planktonic
and benthic foraminiferids, assigned to the middle-upper part of the Gansserina gansseri Zone and to the Abathomphalus
mayaroensis Zone. The composition of the assemblages indicates fluctuations of organic matter flux to the marginal
part of the Skole Basin floor in the studied interval. The studied taxa are typical of the “transitional zone” between the
Tethyan and the Boreal domains. The disappearance of planktonic foraminifers in the uppermost part of the section and
appearance of some agglutinated taxa (Rzehakina fissistomata; abundant Conglophragmium irregularis and Glomospira
charoides) points to a Paleocene age.

Key words: Maastrichtian, flysch, transitional zone, paleoecology, biostratigraphy, foraminiferids.

Introduction

Terminal Maastrichtian foraminiferal assemblages in the Flysch
Carpathians  are  represented  by  mostly  poorly  diagnostic
benthic  agglutinated  taxa.  The  foraminiferal  zones  based  on
them (Geroch & Nowak 1984; Olszewska 1997) are broad in
duration. As a consequence a precise stratigraphy of this inter-
val is very difficult, and determination of the K/T boundary is
imprecise.  Exceptionally,  some  taxa  of  the  youngest  Creta-
ceous  planktonic  foraminiferal  Abathomphalus  mayaroensis
Zone  have  been  found  in  a  few  sections  of  the  Subsilesian
Unit  (Gasiński  et  al.  1999,  2001)  and  the  Skole  Nappe  (see
chapter

Micropaleontological analysis

Very rich assemblages of planktonic and benthic foramini-

fers of youngest Maastrichtian age occur in flysch sedi-
ments of the marginal thrust sheet in the Skole Nappe, SE
of Rzeszów in the Husów region (Fig. 1). Their description
and interpretation are the main aim of the paper.

The biostratigraphy of the Cretaceous in the study area is

so far poorly recognized, without modern micropaleontolog-
ical  research.  Such  abundant,  very  diverse  and  well  pre-
served  Maastrichtian  planktonic  foraminiferal  assemblages
are  very  rarely  found  in  the  Polish  Flysch  Carpathians
(Gasiński  et  al.  1999,  2001,  2003).  Commonly,  only  some
index taxa are listed but not illustrated. For the first time in
the  Skole  Unit,  the  planktonic  foraminiferal  assemblage  al-
low  the  recognition  of  recently  proposed  latest  Cretaceous
biozones.  Moreover,  the  microfauna  of  the  Skole  Unit  con-
tributes  to  our  understanding  of  migration  “gates”  between
the  Boreal  and  Tethyan  biogeoprovinces  (Gasiński  1997,
1998; Marcinowski & Gasiński 2002). The marginal part of
the Skole Unit of the Polish Carpathians was located near the
Boreal-Transitional  domain  (Kollmann  &  Zapfe  1992)  in
proximity  to  the  so-called  Lviv  Gate  (Marcinowski  &
Gasiński  2002).  Therefore,  micropaleontological  data  from

this area are very important for reconstructions of the Late
Cretaceous plankton paleobiogeography.

Geological setting

The Skole Nappe SE of Rzeszów has been studied since the

century. Tietze (1883) distinguished the Ropianka Beds

in the vicinity of Albigowa and ascribed all the flysch deposits
SE of Rzeszów to the “older Tertiary”, and Hilber (1885) as-
signed them  to the Neocomian. Friedberg (1900) also distin-
guished  the  Ropianka  Beds  at  Albigowa  and  Husów.
Wdowiarz  (1936,  1949)  characterized  the  lithostratigraphy
and  tectonics  of  the  Cretaceous  and  younger  deposits  of  this
area. He recognized the Inoceramian Beds (formerly known as
the  Ropianka  Beds),  subdivided  them  into  the  lower,  middle
and upper levels, estimated their thickness at 500 m, and dated
them  to  the  Senonian—Paleocene  by  analogy  to  other  areas.
They are overlain by the Eocene Variegated Shale. For a com-
prehensive  history  of  research  on  the  Ropianka  Beds  (latter
Ropianka Formation or Inoceramian Beds) in the Skole Nappe
see  Kotlarczyk  (1978).  Bromowicz  (1974)  described  the  li-
thology  and  distinguished  four  lithological  complexes  in  the
Inoceramian Beds in the area SE of Rzeszów, the total thick-
ness of which was estimated at about 400 m. Bromowicz de-
termined that their sediments were transported from the NW.
West  of  the  study  area,  Malata  (2001)  distinguished  the  Fu-
coid Marl Member, Leszczyny Sandstone Member (Maastrich-
tian)  and  the  Makówka  Slump  Debris  (Late  Maastrichtian)
within  the  Ropianka  Formation  which  was  renamed  as  the
Rybotycze Formation.

At first in the 19

century, the studied deposits of the Skole

Nappe were named the Ropianka Beds, which were originally
distinguished in the Magura Nappe (Paul 1869). Later, these
deposits were called the Inoceramian Beds (Uhlig 1888;

284

GASIŃSKI and UCHMAN

Wdowiarz 1949). Kotlarczyk (1978) applied the oldest name
to  the  Inoceramian  Beds  of  the  Skole  Nappe  and  established
the Ropianka Formation with its neostratotype in the Przemyśl
area, which he (see also Kotlarczyk 1979, 1985) subdivided
into  the  Cisowa  Member  (Turonian—Lower  Campanian),
Wiar  Member  (Lower  Campanian—Lower  Maastrichtian),
Leszczyny  Member  (Lower  Maastrichtian—Lower  Paleo-
cene)  and  Wola  Korzeniecka  Member  (Paleocene)  (Fig. 2).

This lithostratigraphic scheme was a matter of controversies
(Haczewski 1986; Ślączka & Miziołek 1995; Malata 1996,
2001) but new propositions, if present (Malata 1996, 2001),
are also problematic. These problems require clarification
that is beyond the scope of this study.

The oldest biostratigraphic data in the studied area come

from the 19

century. Hilber in Uhlig (1883) and Grzybowski

(1903)  found  inoceramid  bivalve  fragments  at  Husów  (their
Hussow)  pointing  to  the  Cretaceous.  Friedberg  (1901,  1903)
determined the foraminifers Dendrophrya excelsa Grzybowski,
D. robusta Grzybowski and D. robusta var. maxima from in-
tercalations  of  sandstones  and  shales  at  Albigowa,  probably
from  the  Inoceramian  Beds.  Friedberg  (1908)  determined
Inoceramus salisburgensis Fugger & Kastner from Husów.

The studied section occurs along the Gajowy stream, in

the Gaj forest between the territories of the villages of

Fig. 1. Location map. Tectonic unit designation, Carpathian margin
and range of the Variegated Shale after Wdowiarz (1949). Location
of samples (Gaj 1, etc.) indicated.

Fig. 2. Stratigraphic scheme of the Skole Nappe. Based on Kot-
larczyk (1988), Rajchel (1990), Rajchel & Uchman (1998), Ślączka
& Kaminski (1998), with further corrections based on further data
by Gedl (1999) and Kotlarczyk et al. (2007). The investigated in-
terval indicated by “!”. The time scale is after Gradstein et al. (2004).
TRShMb – Trójca Red Shale Member, VSh – Variegated Shale,
ChSMb – Chmielnik Striped Sandstone Member.

285

LATEST MAASTRICHTIAN FORAMINIFERAL ASSEMBLAGES (HUSÓW REGION, POLAND)

Husów, Handzlówka and Albigowa (Fig. 1). The outcrops are
small  and  isolated  (sections  A—D  in  Fig. 3),  but  the  conse-
quent strikes and dips of beds suggest a limb of a regular anti-
cline with its axis dipping to the west. The anticline is a part of
the  Marginal  Thrust  Sheet,  the  structure  of  which  is  more
complex  to  the  NW  (Wdowiarz  1949).  The  Marginal  Thrust
Sheet is overthrust to the NE onto the Miocene of the Stebnik
Unit  (or  Zgłobice  Unit  according  to  Kotlarczyk  1988)  or  on
the  autochthonous  Miocene  of  the  Carpathian  Foredeep.  To
the SE, the Ropianka Formation of the Marginal Thrust Sheet
is bound by a belt of Eocene Variegated Shale, which also be-
longs to the Marginal Thrust Sheet. Further to the South, the
Husów  Thrust  Sheet  is  present,  which  is  overthrust  onto  the
Marginal Thrust Sheet (Wdowiarz 1949).

The studied outcrops are composed of turbiditic deposits

with a great contribution of marls and marly shales interca-
lated  with  fine-  to  medium-grained  calcareous  sandstones
(Fig. 3). The lower part of the studied sequence (sections A
and  B)  contains  more  sandstones,  with  beds  up  to  30 cm
thick.  The  upper  part  (sections  C,  D)  contains  less  sand-
stones,  with  thinner  beds.  These  deposits  contain  the  trace
fossils  Ophiomorpha  rudis  (especially  in  thicker  beds),
Chondrites  targionii,  and  rarely  Nereites  irregularis  and
Phycosiphon  incertum.  Stratigraphically,  the  studied  depos-

its are an equivalent of the Leszczyny Member and possibly
of the uppermost part of the Wiar Member of the Ropianka
Formation  sensu  Kotlarczyk  (1978,  1988)  (Fig. 2).  The  li-
thology  of  the  Leszczyny  Member  is  very  variable  and  in-
cludes  marl-rich  olistostromes.  It  is  not  clear  whether  the
Wiar  Member  or  the  Leszczyny  Member  can  be  distin-
guished  in  the  study area, however  a general  fining-up  sec-
tion is one of the typical features of the Leszczyny Member
(Kotlarczyk 1978) and these members are recognized west of
the  study  area  (J.  Kotlarczyk,  personal  communication,
2008).  The  divisions  recognized  by  Malata  (2001)  in  the
same tectonic units, namely the Leszczyny Sandstone Mem-
ber  (thick-bedded  sandstones  at  least  100 m  thick)  and  the
Makówka Slump Debris Member, which can be expected to
occur in the studied section because of their stratigraphic po-
sition, are not recognized here.

Micropaleontological analysis

Biostratigraphy

Twenty five samples from the section studied area have

been analysed (see: Figs. 3, 4). Some of these contain well

Fig. 3. Lithological column with location of the samples.

287

LATEST MAASTRICHTIAN FORAMINIFERAL ASSEMBLAGES (HUSÓW REGION, POLAND)

and very well preserved planktonic and benthic foraminifer-
ids  (Figs. 4,  5).  The  stratigraphic  ranges  of  the  index  taxa
point to a Maastrichtian age. The middle to upper part of the
Gansserina  gansseri  to  Abathomphalus  mayaroensis  stan-
dard  zones  were  distinguished  according  to  the  zonation
published  by  Caron  (1985),  Robaszynski  &  Caron  (1995;
Fig. 5). These zones have been recognized on the basis of in-
dex planktonic foraminiferids as well as characteristic fora-
miniferal  assemblages.  The  Abtahomphalus  mayaroensis
Zone is a Taxon Range Zone. It was recognized between sam-
ple Gaj 4.1, where the first appearance (FO) of A. mayaroensis
(Bolli)  is  noted,  and    sample  Gaj 5.7,  where  its  last  occur-
rence (LO) is observed (Fig. 5). Gansserina gansseri (Bol-
li) is not present in the analysed material, probably due to
its more Tethyan paleobiogeographic preferences. Neverthe-
less, the stratigraphic ranges of other planktonic species, such
as:  Pseudotextularia  elegans  (Rzehak),  Globigerinelloides
prairiehillensis  Pessagno,  Hedbergella  holmdelensis  Olsson,
Globotruncana aegyptiaca Nakkady, G. bulloides Vogler and
G. stuartiformis (Dalbiez), and the absence of Abathomphalus
mayaroensis (Bolli) in sample Gaj 1 to Gaj 4 (below its FO)
points to the underlying Gansserina gansseri Zone (Fig. 4).

Abathomphalus mayaroensis is rarely noted from the tur-

biditic sequences of the Outer Carpathians (e.g. Liszkowa &
Morgiel 1981; Gasiński et al. 2001). However, this species is
never abundant and occurs in assemblages together with oth-
er planktonic species, such as Heterohelix navarroensis

Ehrenberg, H. striata (Ehrenberg), Pseudotextularia elegans
(Rzehak),  Racemiguembelina  fructicosa  (Egger),  Globige-
rinelloides  prairiehillensis  Pessagno,  Hedbergella  holmde-
lensis  Olsson,  H.  monmouthensis  (Olsson),  Globotruncana
aegyptiaca  Nakkady,  G.  arca  (Cushman),  G.  bulloides  Vo-
gler, Globotruncanita stuarti (de Lapparent), G. stuartiformis
(Dalbiez), Globotruncanella havanensis (Voorvijk), G. peta-
loidea  (Gandolfi),  or  Contusotruncana  contusa  (Cushman)
(Fig. 4).  All  the  diagnostic  species  as  well  as  some  taxa
which  are  typical  of  the  studied  foraminiferal  assemblages
are illustrated in Figures 7—9. Their stratigraphic ranges are
reported  after  Robaszynski  et  al.  (1984),  Caron  (1985),
Robaszynski  &  Caron  (1995),  Premoli-Silva  &  Rettori
(2002) and Premoli-Silva & Verga (2004).

Foraminiferal assemblages from sample Gaj 5.7A to sam-

ple  Gaj 6A  (Fig. 4)  are  composed  mainly  of  agglutinated
taxa,  with  a  small  admixture  of  calcareous  benthic  forms.
They  do  not  contain  any  planktonic  taxa.  Therefore,  it  is
impossible to determine their precise biostratigraphical posi-
tion  to  a  particular  biozone,  however  some  suggestions
based  on  composition  of  the  agglutinated  foraminiferal  as-
semblages can be made. Samples Gaj 5.7A, 5.8 and 5.9 con-
tain among others the agglutinated index species  Rzehakina
fissistomata  (Grzybowski),  which  ranges  from  the  ?Maas-
trichtian  to  the  Paleocene  (Kaminski  &  Gradstein  2005).
Liszkowa & Morgiel (1981) have dated an agglutinated for-
aminiferal assemblage with Rzehakina fissistomata from the

Fig. 5. Biostratigraphical ranges of the studied planktonic index taxa. Ranges of species
and biozones plotted (combined) after Robaszynski et al. (1984), Caron (1985), Robaszyns-
ki & Caron (1995), Premoli-Silva & Rettori (2002) and Premoli-Silva & Verga (2004). The
grey area indicates biozones recognized in the studied material.

Krasice section of the Skole Unit as Pa-
leocene. Sample Gaj 6 does not contain
index  taxa,  but  the  increased  abundance
of Conglophragmium irregularis (White)
and  Glomospira  charoides  (Parker  &
Jones)  points  to  the  Paleogene.  The
same  concerns  sample  Gaj 6A,  which
additionally contains Karrerulina con-
versa  (Grzybowski)  and  K.  horrida
(Mjatliuk).  The  higher  abundance  of
shales  in  this  part  of  the  section
(Figs. 3, 4) suggests a change in depo-
sitional conditions.

Abathomphalus mayaroensis (Bolli)
in the Skole Nappe

Abathomphalus mayaroensis (Bolli)

(formerly  Globotruncana  mayaroensis
Bolli)  has  been  recognized  by  Bukowy
& Geroch (1957) in the K. Wójcik col-
lection of foraminiferids from the exot-
ic conglomerates at Kruhel Wielki near
Przemyśl.  Morgiel  (1959)  and  Szyma-
kowska  (1961)  mentioned  the  occur-
rence of this species in the Babica Clay.
The Babica Clay is composed mostly of
debris flow deposits and is dated to the
Paleocene

(Bukowy

1956,

1957;

Geroch & Kotlarczyk 1963). It seems
that A. mayaroensis in this unit is rede-
posited from Maastrichtian sediments.

288

GASIŃSKI and UCHMAN

Other findings of Abathomphalus mayaroensis come from

the Ropianka Formation of the Skole Nappe but these obser-
vations  are  rarely  supplemented  by  detailed  localization.
Morgiel & Żgiet (1961) mentioned G. mayaroensis in sam-
ples from the borehole at Dydnia (their Inoceramian Beds of
the  Subsilesian  and  Skole  Units  transitional  zone).  Glo-
botruncana  mayaroensis  is  listed  among  the  foraminiferal
assemblages of the Ropianka Formation (Inoceramian Beds)
as  well  as  those  of  the  Węgierka  Marls  (upper  part  of  the
Ropianka  Formation)  (Gucik  1962,  1987;  Gucik  &  Wójcik
1982;  Kotlarczyk  1988).  It  was  also  listed  by  Bieda  et  al.
(1963)  from  the  Węglówka  Marl  and  the  Żegocina  Marl  of
the  Subsilesian  Unit.  Vialov  et  al.  (1967)  and  Zhurakovsky
(1971) reported findings of G. mayaroensis in the Ukrainian
part of the Skole Nappe. Morgiel in Wdowiarz et al. (1974)
mentioned  it  from  the  Cisowa  IG-1  borehole.  Morgiel  &
Liszkowa (1981) informed about relatively numerous speci-
mens of A. mayaroensis within  foraminiferal assemblages of
the  Frydek  Marl-type  sediments  of  the  Subsilesian  Unit  as
well as from the so-called Baculites Marls (an equivalent of
the Węgierka Marls in the Skole Nappe).

Abathomphalus mayaroensis and associated planktonic and

benthic foraminifers have also been found in the Leszczyny
Member in the Przemyśl area (Kotlarczyk 1988, p. 44). Mor-
giel in Żytko & Zimnal (1997) noted A. mayaroensis from the
foraminiferal association of the Smorż stream section.

Paleoecology

On the basis of washed residues of the collected samples, a

quantitative analysis has been performed (Fig. 6). All speci-
mens,  including  those  with  broken  tests,  were  counted.  For
the  planktonic  assemblages,  the  parameters:  planktonic/
benthic  ratio  and  epipelagic/bathypelagic  ratio  are  consid-
ered as indicators of paleobathymetry and offshore distance
(cf. Sliter 1972; Sliter & Baker 1972; Olsson & Nyong 1984;
and others). Within the benthic associations, the agglutinat-
ed/calcareous  benthic  taxa  ratio  and  the  suspension-feeders
(tubular  forms  such  as  Rhabdammina  or  Nothia)/other  ag-
glutinated taxa ratio were counted. These results point to the
organic flux (OF) to the basin floor by turbiditic currents and
to  its  quantitative  aspect  (cf.  Kaminski  &  Kuhnt  1995;
Gasiński  1998).  A  distinct  negative  correlation  between  an
increase in planktonic and especially epipelagic species and
a  reduction  in  suspension  feeders  is  noted  (Fig. 6).  Only  in
sample Gaj 5.4A does this relation change rapidly; plankton-
ic  species  became  very  scarce,  whereas  suspension  feeders
dominate.  This  could  reflect  an  increase  in  OF,  which  may
have  been  caused  by  increased  productivity  or  redeposition
of organic matter from the shallower part of the basin due to
a relative sea-level fall. However, the latter possibility is not
marked by any sedimentological change, such as coarsening
of sediments. The relative increase in abundance of the sus-
pension feeder morphological group in relation to relatively
scarce epipelagic taxa is observed in sample Gaj 1. Another
rapid increase in suspension feeder abundance and diminish-
ing abundance of epipelagic planktonic taxa is noted in sam-
ple  Gaj 5.5.  Such  rapid  changes  among  foraminiferal
assemblages  of  samples  Gaj 5.4A  and  Gaj 5.5  can  be  inter-

preted as an episode of rapid increase in sea-surface produc-
tivity (especially distinct in sample Gaj 5.4A). The increased
availability of organic matter caused the rapid appearance of
tubular  agglutinated  taxa  (for  the  feeding  strategy  of  fora-
miniferal  suspension  feeders  see:  Jones  &  Charnock  1985;
Nagy  1992;  Kaminski  &  Kuhnt  1995;  Gasiński  1998).  It
should  be  stressed  that  from  sample  Gaj 6  (Fig. 6)  aggluti-
nated  foraminiferids  dominate,  which  indicates  a  drastic
change in environmental conditions resulting in a change of
composition of foraminiferal assemblages toward decreasing
planktonic taxa. Of course, the activity of turbiditic currents
taking  place  in  the  studied  part  of  the  Skole  Basin  strongly
influenced such processes.

Discussion

Biostratigraphy

The chronostratigraphy of the Abathomphalus mayaroen-

sis  and  Gansserina  gansseri  Zones  has  been  provided  by
Robaszynski  &  Caron  (1995).  In  their  scheme,  the  Maas-
trichtian  comprises  the  whole    of  the  A.  mayaroensis  Zone
and  the  upper  part  of  the  G.  gansseri  Zone.  Robaszynski  et
al. (1984) and Caron (1985) proposed a different scheme, in
which  the  underlying  G.  aegyptiaca  and  the  G.  helvetica
Zones are also included into the Maastrichtian. According to
the  subsequent  schemes  by  Robaszynski  &  Caron  (1995)
and Premoli-Silva & Rettori (2002), these zones belong into
the upper Campanian. In the current Cretaceous Time Scale,
Gradstein et al. (2004) proposed a Racemiguembelina fructi-
cosa Zone situated between the A. mayaroensis and G. gans-
seri Zones. Racemiguembelina fructicosa (Egger) is present
in  the  studied  material  (Fig. 8.3—6),  however  its  occurrence
together  with  A.  mayaroensis  (Fig. 4)  does  not  allow  us  to
separate  the  Racemiguembelina  fructicosa  Zone.  Racemi-
guembelina fructicosa is rarely noted in foraminiferal assem-
blages of the Tethyan domain (cf. Nederbragt 1991).

It should be mentioned that the Cretaceous/Paleocene

boundary (traditionally named K/T) is placed between the last
occurrence of Abathomphalus mayaroensis (Bolli) and first
abundant appearance of Guembelitria cretacea Cushman,
which constitutes the Partial Range P0 Zone sensu Olsson et
al. (1999) and Gradstein et al. (2004). It is located between the
samples Gaj 5.7 amd Gaj 5.7A of the studied section (Fig. 3),
which are 3 m apart. So far, this is the most precise location of
the K/T boundary in the Polish Carpathians.

Provenience of the studied planktonic assemblage

The Maastrichtian foraminiferal assemblages analysed

from the Husów area (this study) and those from the Węgier-
ka Marls of the Skole Unit (Kotlarczyk 1978; Geroch et al.
1979)  display  a  distinct  similarity.  The  Kropiwnik  Fucoid
Marl  in  the  Wiar  Member  (Kotlarczyk  1978,  1985,  1988)
also contains some similar species of foraminiferids, among
them a few index species such as: Globotruncana arca, Glo-
botruncanita  stuarti,  Globotruncanella  havanensis,  and
Contusotruncana contusa.

292

GASIŃSKI and UCHMAN

Fig. 9. Other microfossils from the Gaj section. 1 – Globotruncanita stuartiformis Dalbiez, sample Gaj 5.2. 2 – Globotruncana linneiana
(de Lapparent), sample Gaj 3. 3 – Globotruncana arca Cushman, sample Gaj 5. 4 – Aragonia ouezzensis (Rey), sample Gaj 5. 5 – Cibi-
cides sp., sample Gaj 5.4. 6 – Quadrimorphina allomorphinoides (Reuss), sample Gaj 5.4. 7 – Ostracoda, sample Gaj 5.4. 8 – ?Nodosa-
ria sp., sample Gaj 5.4A.

Leszczyny Members. However, the problem of migration pro-
cesses of microfauna between Tethyan Carpathian basins and
Boreal domain is still unsolved.

The connection between the Skole Basin and the adjacent

epicontinental  sea  has  been  suggested  for  quite  some  time.
Wawryk (1939) noted a similarity of the more or less coeval
sediments  of  the  so-called  Łopuszka  Marls  and  Węgierka
Marls (about 20 km E of the studied section) to the marls ex-
posed  near  Lviv  (the  so-called  Lviv  Opoka).  Kotlarczyk
(1988) mentioned that the Leszczyny Member marls resem-
ble  the  Upper  Cretaceous  marls  from  the  Eastern  European
Platform.  These  suggestions  are  confirmed  by  the  studied
foraminiferal assemblage composition.

The possible migration gates of biota between the Boreal

and Tethyan provinces during the Late Cretaceous have been
discussed  by  Hanzliková  (1972),  Fuchs  &  Wessely  (1996),
Gasiński  (1998)  and  Marcinowski  &  Gasiński  (2002).  The
processes  of  migration  and  strategies  of  foraminiferal  “mi-
grants”  have  been  suggested  by  Gasiński  (1997,  1998)  and
Marcinowski & Gasiński (2002). In the later publication the
so-called “Lviv Gate” is suggested as the migration pathway
to  the  Carpathian  basins  from  the  North  (Marcinowski  &
Gasiński 1992, p. 109).

Conclusions

1. The studied deposits of the Ropianka Formation in the

Gaj section are here correlated with the Maastrichtian (part
of the Gansserina gansseri Zone and the Abathomphalus ma-
yaroensis Zone). The uppermost part of the section is dated
to the Paleocene. The K/T boundary is located within a 3 m
thick part of the Gaj section.

2. Foraminiferal assemblage composition indicates fluctu-

ations in organic matter flux to the marginal part of the Skole
Basin floor in the studied interval.

3. The studied foraminiferal assemblages are typical of the

“transitional zone” between the Tethyan and the Boreal do-
mains.

Acknowledgments:  The  authors  greatly  appreciate  Janusz
Kotlarczyk (Academy of Mining and Metallurgy; Cracow) for
his constructive criticism and helpful remarks. We would like
to  thank  Michael  A.  Kaminski  (University  College  London)
and  Ryszard  Marcinowski  (Warsaw  University)  for  their  re-
viewer  comments    and  suggesstions.  Jagiellonian  University
provided the support (DS funds).

References

Bieda F., Geroch S., Koszarski L., Książkiewicz M. & Żytko K.

1963: Stratigraphie des Karpates externes polonaises. Biul.
Inst. Geol. 181, 1—210.

Bromowicz J. 1974: Facial variability and lithological character of

Inoceramian Beds of the Skole Nappe between Rzeszów and
Przemyśl. Prace Geologiczne, Polska Akademia Nauk, Oddział
w Krakowie, Komisja Nauk Geologicznych 84, 1—83 (in Polish
with English summary).

Bukowy S. 1956: Observations on sedimentation of the Babica

clays (Palaeocene) in the Middle Carpathians. Bull. Polish
Acad. Sci. Cl. 3, 4(9), 631—635.

Bukowy S. 1957: Remarks on the sedimentation of the Babica

clays. Rocznik Polskiego Towarzystwa Geologicznego 26 (for
1956), 147—155 (in Polish).

Bukowy S. & Geroch S. 1957: On the age of exotic conglomerates

at Kruhel Wielki near Przemyśl (Carpathians). Ann. Soc. Geol.
Pol. 26, 297—329 (in Polish with English summary).

293

LATEST MAASTRICHTIAN FORAMINIFERAL ASSEMBLAGES (HUSÓW REGION, POLAND)

Burzewski W. 1966: Baculites marls on the lithostratigraphy back-

ground of the upper Inoceramian Beds of the Skiba Carpathians.
Zeszyty Naukowe AGH, Geol. 7, 89—115 (in Polish).

Caron M. 1985: Cretaceous planktonic foraminifera. In: Bolli H.M.,

Saunders J. & Perch-Nielesn K. (Eds.): Plankton stratigraphy.
Cambridge University Press, Cambridge, 17—86.

Friedberg W. 1900: Geological investigations of the vicinity of

Rzeszów and Łańcut. Kosmos 24, 289—311 (in Polish).

Friedberg W. 1901: Foraminiferids of the Inoceramian Beds of the

vicinity of Rzeszów and Dębica. Rozpr. Wydziału Matematyc-
zno-Przyrodniczego Akademii Umiejętności, Serya 3, Tom 1,
Dział B, Nauki Biologiczne 41, 601—668 (in Polish only).

Friedberg W. 1903: Geological Atlas of Galicia. Tekst do Zeszytu

Szesnastego. Wydawnictwa Komisyi Fizyograficznej Akademii
Umiejętności, Kraków, 1—147 (in Polish only).

Friedberg W. 1908: Small contribution to the Inoceramian Beds

fauna. Sprawozdanie Komisji Fizjograficznej Akademii Umie-
jetności 42, 58—63 (in Polish only).

Fuchs R. & Wessely G. 1996: The autochthonous Cretaceous at the

southern edge of the Bohemian Massif (Austria). In: Wessely
G. & Liebl (Eds.): Oil and gas in Alpine thrustbelts and basins
of Central and Eastern Europe. Geol. Soc. London, European
Assoc. Geosci. and Engineers, Spec. Publ. 5, 249—253.

Gasiński M.A. 1997: Tethyan-Boreal connection: influence on the

evolution of mid-Cretaceous planktonic foraminiferids. Creta-
ceous Research 18, 505—514.

Gasiński M.A. 1998: Campanian—Maastrichtian palaeoecology and

palaeobiogeography of the Andrychów Klippes, Outer Car-
pathians, Poland. Uniwersytet Jagielloński, Rozprawy Habili-
tacyjne 333, 1—90.

Gasiński M.A., Jugowiec M. & Ślączka A. 1999: Late Cretaceous

foraminiferids and calcareous nannoplankton from the
Węglówka Marls (Subsilesian Unit, Outer Carpathians, Po-
land). Geol. Carpathica 50, 1—11.

Gasiński M.A., Leśniak T. & Piotrowski M. 2001: Latest Maas-

trichtian foraminiferal Abathomphalus mayaroensis Zone in
the Subsilesian Unit (Polish Outer Carpathians). Bull. Polish
Acad. Sci., Earth Sci. 49, 89—97.

Gasiński M.A., Leśniak T. & Wróbel A. 2003: Biostratigraphy and

palaeoenvironmental analysis of the Żegocina Marls in the
Żegocina Tectonic Window (Subsilesian Unit, Polish Outer
Carpathians). Bull. Polish Acad. Sci., Earth Sci. 51, 1—9.

Gedl E. 1999: Lower Cretaceous palynomorphs from the Skole Nappe

(Outer Carpathians, Poland). Geol. Carpathica 50, 75—90.

Geroch S. & Kotlarczyk J. 1963: Remarks about the age of the Babice

Clay marls from the Bircza vicinity. Przegl. Geol. 11, 286—287
(in Polish).

Geroch S. & Nowak W. 1984: Proposal of zonation for the Late Ti-

thonian—Late Eocene based upon arenaceous foraminifera from
the Outer Carpathians, Poland. In: Oertli (Ed.): Benthos ’83:
2nd International Symposium on Benthic Foraminifera (Pau,
France). Elf-Aquitaine, ESSO REP and Total CFP, Pau & Bor-
deaux, 225—239.

Geroch S., Jednorowska A., Książkiewicz M. & Liszkowa J. 1967:

Stratigraphy based upon microfauna in the Western Polish
Carpathians. Biul. Inst. Geol. 211, 186—282.

Geroch S., Krysowska-Iwaszkiewicz M., Michalik M., Prochazka

K., Radomski A., Radwański Z., Unrug Z., Unrug R. & Wie-
czorek J. 1979: Sedimentation of the Wegierka marls. Ann.
Soc. Geol. Pol. 49, 105—133 (in Polish with English summary).

Gradstein F., Ogg J. & Smith A. 2004: A geologic time scale. Cam-

bridge University Press, Cambridge, 1—589.

Grzybowski J. 1903: Geological Atlas of Galicja. Tekst do Zeszytu

Czternastego. Wydawnictwa Komisyi Fizyograficznej Aka-
demii Umiejętności, Kraków, 1—91 (in Polish only).

Gucik S. 1962: Geology of the northern part of the Skole unit be-

tween Pruchnik and Ujkowice. Kwart. Geol. 4, 794—795 (in
Polish only).

Gucik S. 1987: Explanations to the Geological Map of Poland

1 : 50,000. Sheet Krzywcza. Wydawnictwa Geologiczne,
Warszawa, 1—77 (in Polish only).

Gucik S. & Wójcik A. 1982: Explanation to the Geological Map of

Poland 1 : 200,000. Sheet Przemyśl—Kalników. Wydawnictwa
Geologiczne, Warszawa, 1—91 (in Polish only).

Haczewski G. 1986: The place and role of marker lithological hori-

zons in litho- and chronostratigraphy. Przegl. Geol. 34, 247—250
(in Polish with English summary).

Hanzliková E. 1969: The Foraminifera of the Frydek Formation

(Senonian). Sbor. Geol. Věd 11, 7—84.

Hanzliková E. 1972: Carpathian Upper Cretaceous Foraminifera of

Moravia (Turonian—Maastrichtian). Rozpr. Ústř. Úst. Geol. 39,
1—160.

Hilber V. 1885: Randtheil der Karpathen bei Dębica, Ropczyce und

Łańcut. Jb. Geol. Reichsanst. 35, 407—428.

Jones R.W. & Charnock M. 1985: “Morphogroups” of agglutinated

foraminifera. Their life position and feeding habits and poten-
tial applicability in (paleo) ecological studies. Rev. Paleobiolo-
gie 4, 311—320.

Kaminski M.A. & Gradstein F.M. 2005: Atlas of Paleogene cosmo-

politan deep-water Foraminifera. Grzybowski Found. Spec.
Publ. 10, 1—547.

Kaminski M.A. & Kuhnt W. 1995: Tubular agglutinated foramin-

ifera as indicators of organic carbon flux. In: Kaminski M.A.,
Geroch S. & Gasiński M.A. (Eds.): Proceedings of the Fourth
International Workshop on Agglutinated Foraminifera. Grzy-
bowski Found. Spec. Publ. 3, 141—144.

Kollmann H.A. & Zapfe H. (Eds.) 1992: New aspects on Tethyan

Cretaceous fossil assemblages. Österr. Akad. Wiss. Schriften-
reihe der Erdwissenschaftlischen Kommissionen 9, 1—240.

Kotlarczyk J. 1978: Stratigraphy of the Ropianka Formation or of Inoc-

eramian Beds in the Skole Unit of the Flysch Carpathians. Prace
Geol., Polska Akad. Nauk, Oddział w Krakowie, Komisja Nauk
Geologicznych 108, 1—82 (in Polish with English summary).

Kotlarczyk J. 1979: Stratigraphy of the Ropianka Formation of the

Skole unit. Materiały Terenowej Konferencji Naukowej w Prze-
myślu, Przemyśl, 28—29 czerwca 1979 r. Sekcja Sedymentolo-
giczna Polskiego Towarzystwa Geologicznego, Kraków, 7—16
(in Polish).

Kotlarczyk J. 1985: An outline of the stratigraphy of marginal tec-

tonic units of the Carpathian Orogen in the Rzeszów-Przemyśl
area. In: Kotlarczyk J. (Ed.): Geotraverse Kraków—Baranów—
Rzeszów—Przemyśl—Ustrzyki Dolne—Komańcza—Dukla. Guide
to excursion 4. Carpatho-Balkan Geological Association XIII
Congress. Cracow, Poland 1985. Geol. Inst., Warszawa, 39—63.

Kotlarczyk J. 1988: Outline of the stratigraphy of the marginal tec-

tonic units of the Carpathian orogen In: Kotlarczyk J., Pękala K.
& Gucik S. (Eds.): Przewodnik 59 Zjazdu Polskiego Towarzyst-
wa Geologicznego, Karpaty Przemyskie, 16—18 września 1988.
Wydawnictwo AGH, Kraków, 23—62 (in Polish).

Kotlarczyk J., Jerzmańska A., Świdnicka E. & Wiszniowska T.

2007: A framework of ichtyofaunal ecostratigraphy of the Oli-
gocene-Early Miocene strata of the Polish Outer Carpathian
Basin. Ann. Soc. Geol. Pol. 76, 1—111.

Liszkowa J. 1956: Microfauna of the Subsilesian unit. Przegl. Geol.

10, 463—469 (in Polish).

Liszkowa J. & Morgiel J. 1981: Microfauna of the Frydek type in

Outer Carpathians, Poland. Biul. Inst. Geol. 331, 83—100 (in
Polish with English summary).

Malata T. 1996: An analysis of formal lithostratigraphic divisions

and a proposition of the subdivision of the Skole Unit of the Pol-
ish Flysch Carpathians. Przegl. Geol. 44, 509—514 (in Polish).

Malata T. 2001: The Skole Unit east of Rzeszów. Posiedzenia

294

GASIŃSKI and UCHMAN

Naukowe Państwowego Instytutu Geologii, 57(9), 60—63 (in
Polish).

Marcinowski R. & Gasiński M.A. 2002: Cretaceous biogeography

of  epicratonic  Poland  and  Carpathians.  In:  Michalík  J.  (Ed.):
Tethyan/Boreal  Cretaceous  Correlation.  Mediterranean  and
Boreal  Cretaceous  paleobiogeographic  areas  in  Central  and
Eastern Europe. Veda, Publishing House of the Slovak Acade-
my of Sciences, Bratislava, 95—115.

Morgiel J. & Żgiet J. 1961: Upper Cretaceous deposits at Dydynia

borehole (Sanok Carpathians). Kwart. Geol. 5, 993—994 (in
Polish).

Nederbragt A.J. 1991: Late Cretaceous biostratigraphy and develop-

ment of Heterohelicidae (planktic foraminifera). Micropaleon-
tology 37, 329—372.

Olsson R.K. & Nyong E.E. 1984: A paleoslope model for Campa-

nian—lower Maestrichtian foraminifera of New Jersey and Del-
aware. J. Foram. Res. 14, 50—69.

Olsson R.K. & Wise S.W. 1987: Upper Maastrichtian to middle

Eocene stratigraphy of the New Jersey slope and coastal plain.
In: van Hinte J.E., Wise S.W. et al. (Eds.): Initial Reports of
the Deep Sea Drilling Project 93, 1243—1365.

Olsson R.K., Hemleben C., Berggren W.A. & Huber B.T. 1999: At-

las of Paleocene planktonic foraminifera. Smithsonian Contri-
butions to Paleobiology 85, 1—252.

Paul K.M. 1869: Die geologischen Verhaltnisse des nördlichen Sa-

roser and Zempliner Comitates. Jb. K.-Kön. Geol. Reichsanst.
19, 156—280.

Premoli-Silva I. & Rettori R. (Eds.) 2002: Practical manual of Cre-

taceous planktonic Foraminifera. International School on
Planktonic Foraminifera, Perugia 18—22 February, 2002. Di-
partimento di Scienza della Terra, Universita di Perugia, Pe-
rugia, 1—462.

Premoli-Silva I. & Verga D. 2004: Practical manual of Cretaceous

planktonic Foraminifera. International School on Planktonic
Foraminifera. 3

Course: Cretaceous. Verga et Rettori eds.

Universites of Perugia and Milano, Tipografia Pontfelcino,
Perugia, 1—283.

Rajchel J. 1990: Lithostratigraphy of the Upper Paleocene and

Eocene deposits in the Skole Unit. Zeszyty Naukowe AGH,
Geol. 48, 1—112 (in Polish with English summary).

Rajchel J. & Uchman A. 1998: Ichnological analysis of an Eocene

mixed marly-siliciclastic flysch deposits in the Nienadowa
Marls Member, Skole Unit, Polish Flysch Carpathians. Ann.
Soc. Geol. Pol. 68, 61—74.

Robaszynski F. & Caron M. 1995: Foraminiferes planctoniques du

Crétacé: commentaire de la zonation Europe-Méditerrané.
Bull. Soc. Géol. France 6, 681—692.

Robaszynski F., Caron M., Gonzales J.M. & Wonders A.H. (Eds.)

1984: Atlas of Late Cretaceous globotruncanids. Rev. Micro-

paleontologie 26, 145—305.

Scheibnerova V. 1971: Foraminifera and the Mesozoic biogeoprov-

inces. Geol. Surv. New Soth Wales 13, 135—174.

Sliter W.V. 1972: Upper Cretaceous planktonic foraminiferal zoo-

geography and ecology-eastern Pacific margin. Palaeogeogr.
Palaeoclimatol. Palaeoecol. 12, 15—31.

Sliter W.V. & Baker R.A. 1972: Cretaceous bathymetric distribu-

tion of benthic foraminiferids. J. Foram. Res. 2, 167—183.

Szymakowska F. 1961: A new locality with “Palaeocene” sediments

from the Skole Unit at Kamienica Dolna and Gorzejowa (Car-
pathians). Kwart. Geol. 5, 613—629 (in Polish with English
summary).

Ślączka A. & Kaminski M.A. 1998: A guidebook to excursions in

the Polish Flysch Carpathians. Grzybowski Found. Spec. Publ.
6, 11—71.

Ślączka A. & Miziołek M. 1995: Geological setting of Ropianka

Beds in Ropianka (Polish Carpathians). Ann. Soc. Geol. Pol.
65, 29—41.

Tietze E. 1883: Beiträge zur Geologie von Galizien. Jb. K.-Kön.

Geol. Reichsanst. 33, 443—560.

Tshakreen S.O. & Gasinski M.A. 2004: Cretaceous-Paleogene

boundary problem in Libya: the occurrence of the foraminifer-
al species Abathomphalus mayaroensis (Bolli) in the Western
Sirt Basin. Geol. Quart. 48, 77—82.

Uhlig V. 1888: Ergebnisse geologischer Aufnahmen in den westgal-

izischen Karpathen. I. Theil. Die Sandsteizone zwischen dem
penninischen Klippenzuge und dem Nordrande. Jb. K.-Kön.
Geol. Reichsanst. 38, 83—264.

Vialov O.S., Dabagian N.W. & Zhurakovsky A.G. 1967: Description

of the Cretaceous Flysch section along the Dniestr river between
Tershevo and Spas. Geol. J. 27, 3—15 (in Ukrainian).

Wawryk W. 1930: L’analyse petrographique de la marne de Lwów

et des marnes de Łopuszka et de Węgierka. Kosmos A, 54,
889—915 (in Polish with French summary).

Wdowiarz S. 1936: Report of geological investigations in the Car-

pathians in 1936 in the area of SE from Rzeszów. Spraw.
Państw. Inst. Geol. 45, 20—22 (in Polish).

Wdowiarz S. 1949: Structure géologique des Karpates Marginales

au sud-est de Rzeszów. Biul. Państw. Inst. Geol. 11, 1—51.

Wdowiarz S., Wieser T., Szczurowska J., Morgiel J. & Szotowa W.

1974: Geological structure of the Skole unit and its basement
in the column of the Cisowa IG 1 Borehole. Biul. Inst. Geol.
18, 1—94 (in Polish with English summary).

Zhurakovsky A.G. 1971: Stratigraphy of the Cretaceous deposits of

the northern slope of the Ukrainian Carpathians. Materialy po
Geologii i Neftegazonosnosti Ukrainy 26, 85—96 (in Russian).

Żytko K. & Zimnal Z. 1997: Explanations to the Geological Map of

Poland 1 : 50,000. Sheet Ustrzyki Dolne. Wydawnictwa Geo-
logiczne, Warszawa, 1—44 (in Polish).