GeolCarp_Vol62_No4_333

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA

, AUGUST 2011, 62, 4, 333—343 doi: 10.2478/v10096-011-0025-8

Introduction

The identification of the Cretaceous-Paleogene (K-T) bound-
ary  in  turbiditic  deposits  is  problematic,  mostly  because  of
the absence of index fossils, especially planktonic foramini-
fers,  and  because  of  redeposition  processes  disturbing  the
stratigraphic record. Only a few attempts can be found in the
literature,  where  the  boundary  is  determined  within  some
portion  of  the  section  (Melinte  1999;  Bubík  et  al.  2002;
Chira  et  al.  2009).  Gasiński  &  Uchman  (2009)  put  the
boundary within a 3 m thick interval of the Ropianka Forma-
tion  (Upper  Cretaceous—Paleocene)  section  in  the  Skole
Nappe  in  the  Polish  Flysch  Carpathians.  The  boundary  was
identified above the last occurrence of the planktonic Creta-
ceous  foraminifers,  including  the  index  taxon  Abathom-
phalus  mayaroensis,  and  below  the  occurrence  of  benthic
foraminifers typical of the Paleogene. As a result of new in-
vestigations in a better exposed section of the Ropianka For-
mation in the adjacent thrust sheet, not only the Cretaceous
but also the Paleogene index planktonic foraminiferids have
been  found  that  enabled  us  to  recognize  the  K-T  boundary
with the accuracy to two beds for the first time in these tur-
biditic  deposits.  Micropaleontological  analysis  of  this  sec-
tion, and the K-T boundary in particular, are the main aim of
this paper.

Geological setting

The Skole Nappe is the most external major nappe of the

Polish Flysch Carpathians (Fig. 1A). It is composed of Low-
er Cretaceous—Miocene deep-sea, mostly flysch sediments

The Cretaceous-Paleogene boundary in turbiditic deposits

identified to the bed: a case study from the Skole Nappe

(Outer Carpathians, southern Poland)

M. ADAM GASIŃSKI and ALFRED UCHMAN

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

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

(Manuscript received November 3, 2010; accepted in revised form February 4, 2011)

Abstract: The Cretaceous-Paleogene (K-T) boundary has been recognized in turbiditic sediments of the Ropianka
Formation in the Skole Nappe (Bąkowiec section) on the basis of planktonic foraminiferids with an accuracy of 40 cm.
Such precise determination of the K-T boundary for the first time in the Carpathians and in turbiditic flysch sediments
in general was possible due to the successive occurrence of the Early Paleocene planktonic taxa of the P1 Zone above the
latest Maastrichtian Abathomphalus mayaroensis Zone with the Racemiguembelina fructicosa Subzone. The trends in
composition of the latest Maastrichtian foraminiferal assemblages are similar to the Gaj section from the adjacent thrust
sheet, probably due to the influence of the same paleoenvironmental factors.

Key words: Paleocene, Maastrichtian, K-T boundary, Carpathians, paleoecology, biostratigraphy, turbidites,
foraminiferids.

that accumulated in the Skole Basin, a segment of the north-
ern Neotethys, and were folded and thrust northward during
the  Miocene.  The  Upper  Cretaceous—Paleocene  sediments
are distinguished as the Ropianka Formation, which was also
named  the  Inoceramian  Beds  for  a  long  time  (Kotlarczyk
1978).  They  are  overlain  by  the  Eocene  Variegated  Shale
Formation  (Rajchel  1990).  For  the  complex  history  of  re-
search  on  the  Ropianka  Formation  in  the  Skole  Nappe  see
Kotlarczyk (1978). SE of Rzeszów, Wdowiarz (1949) distin-
guished the lower, middle and upper levels in the Ropianka
Formation  (his  Inoceramian  Beds),  which  are  altogether
500 m  thick.  Kotlarczyk  (1978)  subdivided  the  Ropianka
Formation into the Cisowa Member (Turonian—Lower Cam-
panian),  Wiar  Member  (Lower  Campanian—Lower  Maas-
trichtian), Leszczyny Member (Lower Maastrichtian—Lower
Paleocene) and Wola Korzeniecka Member (Paleocene). For
further details see Gasiński & Uchman (2009) and references
therein.

The lower part of the studied section (GPS coordinates:

N49°59.040

’; E022°14.910’; ±9 m) starts along an un-

named stream, a tributary of the Handzlowski Potok Stream
(Sawa River in the lower part), the gorge of which is incised
into the southern slope of the Patria Hill (426 m a.s.l.) along
the  border  between  the  Husów  and  Handzlówka  villages,
and  continues  along  the  Handzlowski  Potok  Stream  in  the
Bąkowiec  forest  on  the  territory  of  the  Husów  village
(Fig. 1B). The outcrops are small and isolated (Figs. 1B, 2),
but consequent strikes and dips of beds suggest a monoclinal
structure  forming  a  part  of  the  Husów  Thrust  Sheet.  The
thrust sheet is disturbed by Variegated Shale occurring in a
narrow  stripe  stretching  along  the  Handzlowski  Potok
Stream (Wdowiarz 1949), which suggests an internal thrust.

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GEOLOGICA CARPATHICA, 2011, 62, 4, 333—343

Some tectonic reductions are possible here.
Nevertheless, the outcrops have stratigraphic
continuity.

The lower part of the section is composed

of  turbiditic  medium,  rarely  thick  or  thin
beds, which contain calcareous sandstones at
the  base  and  thick  layers  of  grey  and  grey-
bluish  marls  and  marly  siltstones  to  mud-
stones at the top (Fig. 2). In the middle part
of  the  section,  about  4 m  thick  debris  flow
deposits  containing  different  marls,  dark
shale and sandstone clasts occur. Higher up,
the contribution of thick sandstone and mar-
ly  beds  increases.  Along  the  Handzlowski
Potok  Stream,  where  the  upper  part  of  the
section  is  exposed,  thin  and  medium  beds
prevail and marly layers are replaced by cal-
careous shales in the higher part of this inter-
val.  The  K-T  boundary  was  identified  here
in  a  natural  scarp  on  the  right  side  of  the
stream, in a 15 m thick interval, which is not
tectonically  disturbed  (GPS  coordinates:
N49°58.706

’; E022°14.879’; ±11 m). Iso-

lated outcrops of red, non-calcareous shales,
with  intercalations  of  rare  sandstones  and
green shales along the stream belong already
to  the  Variegated  Shale  Formation.  Down
the  stream,  massive  or  indistinctly  bedded
calcareous  mudstones  occur.  They  probably
belong  to  the  Babica  Clay  (Paleocene),
which  is  a  unit  within  the  Variegated  Shale
Formation,  composed  mostly  of  mud  flow
deposits  (Kotlarczyk  1978;  Rajchel  1990
and references therein).

The boundary interval (Fig. 3) includes

two  turbiditic-hemipelagic  rhythms.  The
first  rhythm  is  composed  of  a  15 cm-thick,
fine-grained,  grey  sandstone  with  rusty  co-
louration,  which  rests  on  a  grey  marlstone,
displays  a  sharp  base  and  a  transition  to
greenish-grey  marly  mudstone  at  the  top.
The marly mudstone is 8.5 cm thick and dis-
plays  rusty  spots.  The  second  rhythm  con-
tains  very  fine-grained,  sharply  based  grey
sandstone,  5.5—6 cm  thick,  which  passes
into  a  greenish-grey  marlstone.  The  marl-
stone  is  8—11 cm  thick.  It  is  overlain  by  a
loaded,  3.5—7.5 cm  thick,  very  fine-grained,
laminated,  grey  sandstone  passing  into  a
greenish-grey mudstone.

Stratigraphically, the studied deposits are

an equivalent of the Leszczyny Member and,
in its lowest part, possibly of the uppermost
part  of  the  Wiar  Member  of  the  Ropianka
Formation  sensu  Kotlarczyk  (1978,  1988).
The  lithology  of  the  Leszczyny  Member
is  very  variable  and  includes  marl-rich
olistostromes.  It  is  not  clear  whether  the
Wiar Member or the Leszczyny Member can

Fig. 1. Location map. A – Location of the study area in the Skole Nappe (simplified
after Kotlarczyk 1988). B – Map of the study area. Tectonic unit designation and
range of the Variegated Shale after Wdowiarz (1949), completed and modified. Loca-
tion of samples (Bak 1, etc.) and orientation of beds indicated.

336

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GEOLOGICA CARPATHICA, 2011, 62, 4, 333—343

be distinguished in the study area, however a general fining
up section is one of the typical features of the Leszczyny
Member (Kotlarczyk 1978) and these members are recog-
nized west of the study area (J. Kotlarczyk, personal commu-
nication, 2008).

The K-T boundary in turbiditic sediments of the

Carpathians

Globally, the Cretaceous-Paleocene (K-T) boundary is pre-

cisely located at the base of the so-called “boundary level”,
as  defined  mainly  in  pelagic  and  hemipelagic  sequences
(MacLeod  &  Keller  1996;  Apellániz  at  al.  1997;  Kaiho  &
Lamolda 1999; Arenillas et al. 2004; Keller 2004; Molina et
al.  2006,  and  others).  This  boundary  is  situated  between  the
Abathomphalus mayaroensis (latest Maastrichtian) and Guem-
belitria  cretacea  (earliest  Paleocene)  Biozones  (Robaszynski
& Caron 1995; Premoli-Silva et al. 2004, and others).

In turbiditic dominated sequences of the deep Alpine

flysch basins, the K-T boundary is very difficult to identify
due to the rare occurrence of index planktonic foraminiferids
and strong redeposition causing the occurrence of mixed for-
aminiferal assemblages. Only in a few cases, the identifica-
tion  was  narrowed  to  some  relatively  thin  intervals.  The
boundary  occurs  within  about  a  meter  thick  interval  in  the
Magura Unit in Moravia, Czech Republic, based on dinocyst
assemblages  (Bubík  et  al.  2002).  In  the  Romanian  Car-
pathians, it was identified within tens of meters by means of
the  calcareous  nannoplankton  and  foraminiferids  (Melinte
1999; Chira et al. 2009).

The K-T boundary in the studied section

Recent studies of the Ropianka Formation of the Skole Unit

in the Husów area (Gaj section), Polish Carpathians (Gasiński
& Uchman 2009), based on 25 samples, allowed recognition
of the latest Maastrichtian Abathomphalus mayaroensis stan-
dard  Biozone  and  overlying  Paleogene  deposits.  The  K-T
boundary has been narrowed to a 3 m thick interval, where the
latest Cretaceous planktonic foraminiferids disappear and Pa-
leogene  benthic  agglutinated  foraminiferids  (relatively  long
ranging species) appear. So far, it was the most precisely iden-
tified  K-T  boundary  in  the  Polish  Carpathians.  More  precise
work in this section is limited due to its poor exposition.

In the better exposed Bąkowiec section, in the adjacent

thrust  sheet,  58  samples  from  the  fine-grained  parts  of  tur-
biditic-hemipelagic  beds  were  analysed  in  our  study.  The
majority  of  them  contain  relatively  rich  and  well-preserved
foraminiferal assemblages. They can also be seen in thin sec-
tions  from  the  sandstone  beds.  Similarly  to  the  Gaj  section
(Gasiński  &  Uchman  2009),  the  Gansserina  gansseri  and
Abathomphalus  mayaroenesis  standard  Biozones  were  rec-
ognized (Fig. 4). The intermediate Racemiguembelina fructi-
cosa  Zone  is  also  distinguished,  the  meaning  of  which  is
discussed below.

Moreover, the appearance of the Paleocene foraminiferids

Subbotina  cancellata  Blow  (Fig. 5M),  Subbotina  triangu-
laris (White) (Fig. 5N), Eoglobigerina cf. edita (Subbotina)
(Fig. 5O) point to the earliest Paleocene zone (P1 Zone sensu
Olsson  et  al.  1999)  (Fig. 6).  The  latest  Maastrichtian  (A.
mayaroensis)  and  the  lowest  Paleocene  foraminifers  occur
within  a  40  cm  thick  interval  (Figs. 3,  7)  limited  to  two
depositional turbiditic-hemipelagic rhythms. Thus, this is the
most  precisely  determined  K-T  boundary  in  turbiditic
sediments.

From the base of the studied section, the Gansserina gans-

seri Zone (after Robaszynski & Caron 1995; Premoli-Silva et
al. 2004) can be recognized. Planktonic foraminiferal assem-
blages contain the index species (Fig. 4). The first appearance
(FO) of Abathomphalus mayaroensis (Bolli) is noted from the
sample  Bak 2a  (Figs. 4,  8M,N)  and  it  delineates  the  base  of
the A. mayaroensis Zone (Fig. 6). The FO of Racemiguembeli-
na fructicosa Egger (Fig. 4R) in sample Bak 2a and its last oc-
currence  (LO)  in  sample  Bak 7  (Fig. 4)  allowed  us  to
recognize  the  Racemigeumbelina  fructicosa  Zone  (Fig. 6),
which is used by some authors (Gradstein et al. 2004) as the
Partial  Range  Zone  within  the  lower  part  of  A.  mayaroensis
Zone. The LO of A. mayaroensis in sample Bak 13 below the
FO of Subbotina cancellata Blow, S. triangularis (White) and
Eoglobigerina  edita  (Subbotina)  in  sample  Bak 14A  (Fig. 7)
has been interpreted as the latest Maastrichtian (A. mayaroensis
Zone). The latter three taxa indicate the P1 Zone of the  Early
Paleocene  (Olsson  et  al.  1999)  (Fig. 6).  It  should  be  under-
lined  that  the  K-T  boundary  is  indentified  within  a  sequence
that is only 40 cm thick (Fig. 3). The rusty layer overlain by
the dark boundary layer, known from pelagic and hemipelagic
sections are not recognized here, but this can be explain by the
turbiditic deposition.

The nearest located deep-sea K-T boundary outside the

Carpathians was identified in “turbiditic and partly hemipe-

Fig. 3. Detail of the K-T boundary section, with indication of sam-
ples and the boundary interval. The key samples in bold.

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Fig. 6. Biostratigraphical ranges of the studied planktonic index taxa. Ranges of species and biozones plotted (combined) after Robaszynski
et al. (1984), Caron (1985), Robaszynski & Caron (1995), Olsson et al. (1999) and Premoli-Silva & Verga (2004). The grey area indicates
biozones recognized in the studied material.

lagic  sediments”  of  the  Gosau  Group  in  the  Eastern  Alps
(Austria;  Rotwandgraben  section;  Lahodynsky  1988;  Peryt
et al. 1997); however, it is not clear whether the boundary is
in  the  turbiditic  or  hemipelagic  sediments.  In  an  other  sec-
tion of the Gosau Group at Gams, the K-T boundary is rec-
ognized  in  hemipelagic  sediments  of  a  series  composed  of
siliciclastic and mixed siliciclastic-carbonate strata deposited
at the middle bathyal paleodepth (Egger et al. 2004, 2009).

Paleoecology

Qualitative analysis of the studied foraminiferal assem-

blages is presented in Fig. 9. Index and typical foraminifer-
ids  are  shown  in  Figs. 5,  8.  The  planktonic/benthic  ratio,
relation of epipelagic to bathypelagic taxa among planktonic
foraminiferal  assemblages,  numbers  of  agglutinated  in  rela-
tion  to  calcareous  foraminiferids  within  the  benthic  assem-
blages  and  amount  of  suspension  feeders  (tubular  forms)
within the agglutinated foraminiferids assemblages were cal-
culated.

Charts showing the mentioned coefficients clearly fluctu-

ate (Fig. 9). Close to the K-T boundary foraminiferal assem-
blages  of  samples  from  Bak 11  to  Bak 14A  (14A1—14A7)
display rapid quantitative changes considered as an ecologi-
cal  event.  Before  this  event,  planktonic  taxa,  which  were
abundant  (Bak 11),  suddenly  decrease  in  numbers  (Bak 12,
12C).  Similarly,  epipelagic  forms,  abundant  among  plank-
tonic  assemblages,  form  about  50 %  in  Bak 11  decrease  to
about  25 %  in  Bak 13.  Increasing  number  of  epipelagic
(non-keeled taxa, r-strategists, opportunistic species) among
planktonic  assemblages  confirms  a  shallower  depositional
environment  (Gasiński  1997;  Gasiński  et  al.  1999,  2001).
However,  any  sedimentological  signal  of  shallowing  sug-
gests redeposition of sediments from a shallower zone.

In contrast, agglutinated species, especially suspension

feeders, formerly relatively scarce among benthic assem-
blages (Bak 13) sharply increase in number (Bak 14A). Ag-
glutinated foraminiferids are more abundant in coarser
sediments of clearly turbiditic origin. In turbiditic sediments,
the suspension feeder morphological group dominates.

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GEOLOGICA CARPATHICA, 2011, 62, 4, 333—343

Drastic changes of foraminiferal assemblages have also

been observed in the K-T boundary sections in the pelagic/
hemipelagic facies (MacLeod & Keller 1996; Apellániz et al.
1997; Kaiho & Lamolda 1999; Arenillas et al. 2004; Keller
2004, and others).

Conclusions

1. The K-T boundary was identified in the turbiditic sedi-

ments with the accuracy of 40 cm for the first time.

2. The Gansserina gansseri, Abathomphalus mayaroensis

(Late Maastrichtian) and P1 (Early Paleocene) standard bio-
zones were recognized in the studied section on the basis of
planktonic foraminiferids.

3. The Racemiguembelina fructicosa Zone as the Partial

Range Zone within the lower part of A. mayaroensis Zone
has been determined for the first time in the Carpathians and
the flysch sediments.

4. Drastic qualitative and quantitative fluctuations among

the studied foraminiferal assemblages were recognized around
the K-T boundary similar to those indicated in the Gaj section
(next thrust sheet).

Acknowledgments: The researches were supported by the
Jagiellonian University (DS funds). The authors greatly ap-
preciate Eustoquio Molina (Zaragoza University), Ján Soták
(Slovak Academy of Sciences) and an anonymous reviewer
for their critical remarks. Waldemar Obcowski (Jagiellonian
University) prepared the photographic figures.

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