GeolCarp_Vol63_No4_267

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA

, AUGUST 2012, 63, 4, 267—294 doi: 10.2478/v10096-012-0022-6

Sarmatian paleoecological environment of the Machów

Formation based on the quantitative nannofossil analysis –

a case study from the Sokołów area

(Polish Carpathian Foredeep)

MARTA OSZCZYPKO-CLOWES, DOMINIKA LELEK and NESTOR OSZCZYPKO

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

m.oszczypko-clowes@uj.edu.pl; dominika.lelek@uj.edu.pl; nestor.oszczypko@uj.edu.pl

(Manuscript received November 22, 2011; accepted in revised form March 13, 2012)

Abstract: The Machów Formation belongs to a supra-evaporitic succession of the Polish Carpathian Foredeep Basin
(PCFB). Our studies were concentrated in the eastern part of the PCFB, north of Rzeszów. 33 samples were collected
from five boreholes, at depth intervals as follows: Stobierna 2 – 1016—1338 m; Stobierna 3 – 715—1669 m;
Stobierna 4 – 1016—1238 m; Stadnicka Brzóza 1 – 350—356 m and 1043—1667 m; Pogwizdów 2 – 1161—1390 m. The
obtained biostratigraphical data gave evidence for the upper part of the NN6 (the Early Sarmatian) and for the NN7 (the
lowermost part of the Late Sarmatian) Zones. All the nannofossil assemblages from Stobierna 2, Stobierna 4 and
Pogwizdów 2 were assigned to the NN6 Zone. In the Stobierna 3 borehole the interval 1669—1113 m was assigned to NN6,
whereas assemblages from depth interval 843—715 m belong to NN7 Zone. In Stadnicka Brzóza 1 interval 1667—1043 m
belongs to NN6 Zone and interval 350—356 m to NN7 Zone. The Discoaster exilis Zone (NN6) was defined by the pres-
ence of Reticulofenestra pseudoumbilica, Sphenolithus abies, Helicosphaera walbersdorfensis and absence of Discoaster
kugleri. The Discoaster kugleri Zone (NN7) assignment was based on the abundance of Coccolithus miopelagicus ( > 10 µm),
used as an alternative species essentially confined to that interval, and absence of Catinaster coalithus. The observed
nannoplankton assemblages are predominantly composed of a high number of redeposited material, abundant long-
ranging taxa and taxa resistant to carbonate dissolution. General assemblage compositions, obtained from quantitative
data, indicate shallow near-shore environment and could confirm basin isolation.

Key words: Miocene, Polish Carpathian Foredeep, paleoecology, biostratigraphy, calcareous nannofossil quantitative
and qualitative analysis.

Introduction

The  Polish  Carpathian  Foredeep  Basin  (PCFB)  (Fig. 1)
about  320 km  long  and  up  100 km  wide  is  part  of  the  big
sedimentary basin, which extends from the Danube River in
Austria  to  the  Iron  Gate  on  the  Danube  River  in  Romania
(see  Oszczypko  1998;  Oszczypko  et  al.  2006).  The  Polish
Carpathian  Foredeep,  developed  at  the  front  of  the  overrid-
ing  Carpathian  nappes,  is  predominantly  filled  with  marine
clastic sediments of the Miocene age up to 3 km thick. These
deposits are underlain by the basement of the West and East
European Platform, composed of Precambrian, Paleozoic and
Mesozoic  rocks.  According  to  geophysics  and  well  data,  the
platform  basement  with  Miocene  molasse  cover  dips  south-
wards underneath the Outer Carpathian nappes to a distance of
at  least  50 km  (Oszczypko  &  Ślączka  1985;  Oszczypko
2006).  The  PCFB  can  be  subdivided  into  inner  and  outer
foredeep. The inner foredeep, composed mainly of the Lower
Miocene  deposits,  is  now  buried  beneath  the  Carpathian
nappes, while the outer foredeep, composed exceptionally of
Middle/?Upper  Miocene  deposits,  is  located  north  of  the
Carpathian frontal thrust.

The Miocene deposits of the PCFB are poorly exposed. A

few, natural exposures of the Miocene strata are situated

mainly along the northern margin of the foredeep. As a re-
sult, our present knowledge on the geological structure and
stratigraphy of the PCFB is based on the borehole and seis-
mic survey for hydrocarbon exploration.

In the course of these investigations the Sokołów-

Smolarzyny,  the  gas-bearing  area  located  NE  of  Rzeszów,
have  been  thoroughly  recognized  (Figs. 2,  3)  by  3D  seismic
survey,  several  boreholes  and  well  logs  (Krzywiec  et  al.
2008).  The  afore-mentioned  studies  enabled  the  construction
of  a  new  depositional  model  of  this  part  of  the  Polish
Carpathian Foredeep Basin (op. cit.). The aim of our study is
to supplement this model with the results of the analysis of pa-
leoecological environments based on calcareous nannofossils.

Previous works

The history of geological research on the Neogene depos-

its in the Southern Poland is almost 200 years old. A detailed
review  of  these  studies  and  the  current  state  of  knowledge
have  been  presented  by  Peryt  &  Jasionowski  (2004).  In  the
outer  part  of  the  Carpathian  Foredeep  the  beginning  of  the
Miocene  sedimentation  is  associated  with  the  Early  Bade-
nian transgression and the deposition of the Dębowiec trans-

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gressive conglomerates (see also Oszczypko et al. 2006),
known from the Cieszyn and Wadowice area, both at the front
of the Carpathian overthrust as well as beneath the Carpath-
ians. The Middle Miocene marine transgression, flooded both
the foredeep and marginal parts of the Carpathians.

The Badenian deposits in the outer part of the foredeep are

traditionally subdivided into Lower Badenian (sub-evaporit-
ic),  Middle  Badenian  (evaporites)  and  Upper  Badenian  (su-
pra-evaporitic)  beds  (Fig. 4).  This  subdivision  differs  from
the  recent  Early/Middle  Miocene  integrated  stratigraphy  of
the Central Paratethys (Piller et al. 2007; Hohenegger et al.
2009,  2011,  see  also  Oszczypko  &  Oszczypko-Clowes
2011).  According  to  these  new  propositions,  the  Badenian
stage  should  be  subdivided  as  follows:  Early  Badenian
(16.30—14.89 Ma),  Middle  Badenian—Moravian  (Lower  and
Upper  Lagenid  Zone;  14.89—13.82 Ma),  and  Late  Badenian
(Wielician 13.82—13.65 Ma and Kosovian: Bulimina-Bolivina
Zone  –  13.65—12.73 Ma).  In  this  scheme,  the  boundary

Fig. 1. Sketch-map of the Polish Carpathians and their foredeep (after Oszczypko 2006). Abbreviations: Su – Siary, Ru – Rača, Bu – By-
strica, and Ku – Krynica subunits of the Magura Nappe. Boreholes: A3 – Andrychów 3; A4 – Andrychów 4; A6 – Andrychów 6;
La – Lachowice 1; Z1 – Zawoja 1; SIG1 – Sucha IG1; Kł1 – Kłaj 1; Ła1– Łapanów 1; WR2 – Wola Raniżowska 2; P1 – Palikówka 1;
K1 – Kuźmina 1; CIG1 – Cisowa IG1; Ch1 – Chotyniec 1; KW1 – Kobylnica Wołoska 1; C4 – Cetynia 4. Main groups of tectonic
units of the Outer Western Carpathians: Marginal Group (external): Borislav-Pokuttya, Stebnik (Sambir) and Zgłobice Units; Middle
Group (central): Grybów, Fore-Magura, Dukla, Silesian, sub-Silesian and Skole Units and Magura Group (internal).

Fig. 2. Locality of boreholes (after Krzywiec et al. 2008, simplified).

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NN4/NN5 at 14.89 Ma is located inside Helicosphaera am-
liaperta LO (15.50—14.53 Ma), while the NN5/NN6 bound-
ary (13.65 Ma) coincides with Sphenolithus heteromorphus
LO. Subsequently, the Badenian/Sarmatian boundary is
placed at 12.73 Ma.

The Badenian strata rest directly on the platform base-

ment,  except  in  the  inner  foredeep,  where  they  cover  the
Lower  Miocene  deposits.  Usually,  the  “Lower  Badenian”
(Ney 1968) begins with a thin layer of conglomerates; how-
ever,  in  the  western  part  of  the  foredeep  the  Dębowiec
Conglomerates attain thicknesses of up to 100 m. The conglom-
erates  pass  upwards  into  dark,  clayey-sandy  sediments  of  the
Skawina  Formation.  The  thickness  of  the  “Lower  Bade-
nian”  deposits  is  variable,  reaching  up  to  1000 m  in  the
western  inner  foredeep  (Fig. 4),  whereas  in  the  remaining
parts  of  the  foredeep  it  rarely  exceeds  30—40 m  (Ney  et  al.
1974).  The  sedimentation  of  the  Skawina  Formation  began
in the inner foredeep with the Praeorbulina glomerosa Zone
(N8),  whereas  in  the  outer  foredeep  it  started  with  the
Orbulina  suturalis  (N9  or  N10)  Zone  (Garecka  et  al.  1996;
Oszczypko  1998; Oszczypko et al. 2006). South of Kraków,
the  Skawina  Formation  has  been  pierced  by  the  borehole
Łapanów 1 (Fig. 1) beneath the Carpathian overthrust, at the
depth  of  1458—1765.5 m.  This  formation  transgressively
covers Jurassic limestones of the lower plate.

In the western part of the foredeep the Dębowiec Con-

glomerates are overlain by the Skawina Formation, while in
other  parts  of  foredeep  this  formation  overlies  directly  the
platform basement. In the Cieszyn-Bielsko area the thickness
of  this  formation  reaches  1000 m,  while  in  the  rest  part  of
PCFB  it  decreases  to  30—40 m  or  less.  In  the  north-eastern
part of the PCFB the Baranów Beds are an equivalent of the
Skawina Formation (see Oszczypko et al. 2006). On the ba-
sis  of  foraminiferal  studies  the  Skawina  (Baranów)  Forma-
tion  has  been  included  in  the  “early  Badenian”,  whereas
according  to  calcareous  nannoplankton  investigation  the
lower part of the formation belongs to the NN5 Zone, while

the upper (sub-salt) part of the formation belongs to the NN6
Zone (Garecka et al. 1996; Andreyeva-Grigorovich et al.
1999, 2003; Peryt 1999; Peryt & Gedl 2010).

Higher up in the succession we find evaporites, which are

developed  in  the  sulphate—anhydrite  and  gypsum  (Krzyżano-
wice Formation) and chloride (salt) facies (Wieliczka Forma-
tion)  (Garlicki  1968)  (Fig. 4).  The  sulphate  facies  strongly
predominates  in  the  entire  Carpathian  Foredeep,  and  its
thickness ranges from 10—30 m, but usually does not exceed
several meters. Both autochthonous and allochthonous chlo-
ride facies occur in a narrow peri-Carpathian zone and to the
east of Tarnów also beneath the Carpathian nappes. Accord-
ing  to  nannoplankton  studies  the  evaporites  belong  to  the
lower  part  of  the  NN6  Zone  (Peryt  1997;  Peryt  et  al.  1997,
1998;  Andreyeva-Grigorovich  et  al.  2003,  2008;  Peryt  &
Gedl 2010).

In the Bochnia Mine, the Wieliczka Salt Formation con-

tains  the  WT-3  tuffite  horizon,  located  ca.  37 m  above  the
top  of  the  Skawina  Formation.  The  radiometric  age  of  this
tuffite has been determined at 13.60+/ —0.07 Ma (De Leeuw
et  al.  2010,  see  also  Bukowski  et  al.  2010).  The  evaporites
are overlain by a sandy-silty series that are attributed to the
Upper Badenian (Kosovian) and Sarmatian (Fig. 4).

Between Kraków and Tarnów the Chodenice Beds occur

above the evaporites. They comprise marly claystones with
sporadic sandy intercalation. The upper part of the Chodenice
Beds contains several tuffite layers (Van Couvering et al.
1981).

In the Sułków brick yard directly above the tuffite layers,

nannoplankton  belonging  to  the  NN6/7  Zone  (Andreyeva-
Grigorovich et al. 1999) may indicate the boundary between
the  Badenian  and  Sarmatian.  Between  Tarnów  and  Dębica
the lower part of the Chodenice Beds up to 600 m thick con-
tain numerous sandy intercalations (Krzywiec 1997). To the
north the thickness of the Chodenice Beds decreases to a few
dozen  meters.  At  the  same  time  these  beds  are  replaced  by
marly  claystones  (Spirialis-Pecten  beds).  Between  Kraków

Fig. 3. Stobierna-Wydrze geological cross-section (after Krzywiec et al. 2008). Lithofacies: 1 – evaporites, 2 – lower fine-grained com-
plex, 3 – turbiditic, 4 – lower deltaic deposits, 5 – inner-deltaic deposits, 6 – upper deltaic deposits, 7 – lagoonal and shallow marine
deposits, 8 – Quaternary and uppermost Sarmatian (undivided).

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and Tarnów the Chodenice Beds are overlain by the sandy
layer of Grabowiec Beds, several hundred meters thick. In the
Kraków area the basal part of the Grabowiec Beds are devel-
oped as the Bogucice Sands (Porębski & Oszczypko 1999).

East of the Dunajec River the evaporites are overlain by

clayey  sandy  deposits  known  as  the  Machów  Formation
(Alexandrowicz  et  al.  1982).  The  youngest  member  of  this
formation  belongs  to  the  Krakowiec  shales  (beds).  Their
thickness  ranges  from  several  hundred  meters  in  the  region
of Tarnów to over 2500 m in the vicinity of Przemyśl. These
beds  were  traditionally  included  in  the  Lower  Sarmatian.

More recent studies by Paruch-Kulczycka (1999) show that
the upper part of these beds belongs to the Late Sarmatian
(Chersonian, cf. Gaździcka 1994; Król & Jeleńska 1999).

The problem of the Badenian / Sarmatian boundary in the

PCFB  has  been  recently  discussed  by  Nejbert  et  al.  (2010)
(see also Oszczypko & Oszczypko-Clowes 2011). It was in-
troduced by results of the Babczyn 2 borehole, drilled in the
NE  part  of  the  PCF  (near  the  Polish-Ukrainian  border).  In
this  borehole,  more  than  32 m  of  evaporite  gypsum  of  the
Krzyżanowice Formation (Wielician), the 9.4 m-thick Pecten
beds,  related  to  the  post-evaporate  Kosovian  transgression,

Fig. 4. Stratigraphic scheme of the Miocene deposits of the Polish Carpathian Foredeep Basin (after Oszczypko 1998; Oszczypko et al.
2006; Oszczypko & Oszczypko-Clowes 2011).

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and  the  12.6 m-thick  Sarmatian  Syndesmya  beds  were
drilled.  The  boundary  between  the  Pecten  and  Syndesmya
beds is roughly coincident with the appearance of the endemic
Sarmatian  foraminifera  Anomalinoides  dividens  Łuczkowska.
In the Pecten beds (3.4 m above the gypsum), a tuffite layer
was  found  and  dated  (

Ar/

Ar) to an average age of

13.06 ± 0.11 Ma (Nejbert et al. 2010).

In the Sokołów-Smolarzyny area (see Krzywiec et al. 2008)

cores  material  have  been  studied  from  the  following  wells:
Stobierna 2,  Stobierna 3,  Stobierna 4,  Brzóza  Stadnicka 1
and  Pogwizdów 2  (Fig. 2).  All  of  these  wells  have  been  lo-
cated on the Lower San High, within the so-called “anhydrite
missing  Rzeszów  Island”  (Komorowska-Błaszczyńska  1965;
Oszczypko et al. 2006). The drilled profiles of these wells be-
longed to the Machów Formation, up to 2000 m thick. On the
basis of core description, the following lithofacies were distin-
guished  as  follows:  hemipelagites,  thin-bedded  heteroliths,
classical turbidites and thick-bedded sandstones (Krzywiec et
al. 2008). The seismic, well data and core analysis enable us to
distinguish (from base to top of the formation) the following
lithofacies  complexes:  lower  fine-grained,  turbiditic,  lower
deltaic, interdeltaic, upper deltaic, nearshore to estuarine, and
upper undivided ones. On the basis of calcareous nannoplank-
ton studies, the Sarmatian (upper part of NN6 to NN7 Zones)
age of studied deposits were determined. Taking into account
the lack of core material, the lowermost and uppermost com-
plexes have not been studied (see Krzywiec et al. 2008).

Biostratigraphic studies of Machów Formation

One of the first references about the stratigraphic position

of the Machów Formation originated from Łuczkowska’s re-
search (1964). Assignment of the age as Late Badenian—Early
Sarmatian  was  based  on  foraminiferal  associations.  The
Sarmatian floor was associated with common occurrence of
Cycloforina stomata  and Anomalinoides dividens Łuczkowska
with simultaneous disappearance of the Late Badenian species.
In  1966  Odrzywolska-Bieńkowa  described  the  following
foraminiferal zones: Anomalinoides dividens and Elphidium
hauerinum  within  the  Krakowiec  beds.  Three  years  later
Jurkiewicz (in: Ney 1969) identified two Sarmatian foramini-
feral  zones  and  then  Odrzywolska-Bieńkowa  (1972)  and
Łuczkowska  (1972)  identified  zones  representing  the  Early
and  Middle  Sarmatian.  In  1994  in  the  Tarnobrzeg  area
(northeastern part of the Carpathian Foredeep) the calcareous
nannofossils  of  the  Machów  Formation  were  studied  by
Gaździcka.  On  the  basis  of  nannoplankton  assemblages  the
age  of  the  Machów  Formation  (the  Pecten  beds  and
Krakowiec clays distinguished) seems to be younger than the
NN7  Discoaster  kugleri  Zone  and  corresponds  to  the  NN8
Catinaster coalitus and NN9 Discoaster hamatus Zones. Ac-
cording  to  Czepiec  (1997),  the  age  of  the  Machów  Forma-
tion is assigned to the Late Badenian—Late Sarmatian, what
was based on foraminiferal associations (the Early Sarmatian
Anomalinoides  dividens  horizon  and  the  lower  part  of  the
Late Sarmatian Protelphidium subgranosum horizon).

Ślęzak (in Krzywiec 1997) assigned these deposits to the

NN5/NN6 Zones. More precise assignment was impossible
due to scarcity and low diversity of the Miocene species. In

SE Poland, calcareous nannoplankton from the Baranów Beds
was studied by Peryt (Peryt in Peryt et al. 1998). Described as-
semblages contained mainly the long-ranging species, where-
as  the  index  taxa  were  absent.  However,  the  nannofossils
assemblages from the anhydrite horizon (above the Baranów
Beds) indicate an age not younger than the NN6 Zone (Peryt
et al. 1998). In 1994 Gaździcka assigned the Baranów Beds to
the NN6 Zone on the basis of the presence of Calcidiscus lep-
toporus,  Coccolithus  pelagicus,  Discoaster  exilis,  Reticulo-
fenestra  minutula  and  Reticulofenestra  pseudoumbilica,
followed  by  the  absence  of  Sphenolithus  heteromorphus  and
Discoaster kugleri. Garecka & Jugowiec (1999) presented the
results  of  biostratigraphic  study  of  Miocene  deposits  in  the
Carpathian Foredeep concentrated on calcareous nannoplank-
ton.  The  Machów  Formation  deposits,  precisely  Krakowiec
Clays, are included in the NN5 Zone (Kupno area) and NN6
(Cegielnica/Dębica  area),  with  exceptions  concerning  poor
quality material, characterized by low diversity and high num-
bers  of  redeposited  specimens.  The  upper  part  of  the  Kra-
kowiec beds in the Jamnica S-119 borehole was assigned to
the Pannonian (the early Late Miocene) by Paruch-Kulczycka
(1999). Such age assignment was based on foraminifera and
the camoebians studies.

In 1999 Olszewska summarized previous micropaleonto-

logical research (1995—1998) in the Carpathian Foredeep area.
The  Machów  Formation  (Alexandrowicz  et  al.  1982),  de-
scribed  by  Olszewska  (1999),  includes  5  informal  subdivi-
sions:  the  Chodenice  Beds,  the  Grabowiec  Beds,  the  Pecten
beds,  the  Spirialis  Clays  Member,  and  the  Krakowiec  clays.
Olszewska (1999) considers foraminiferal associations  above
Anomalinoides  dividens  horizon  as  less  diagnostic  and  sug-
gests  revision  of  these  data  by  nannoplankton  assignment,
which  seems  to  be  more  precise.  On  the  basis  of  foramin-
ifera,  the  Krakowiec  clays  were  assigned  to  the  Late  Bade-
nian—Early Sarmatian (Olszewska 1999; Dziadzio 1999). The
next foraminiferal studies provided by Olszewska (Olszewska
in: Dziadzio et al. 2006) confirmed these results. Moreover,
the younger deposits were also described and qualified to the
Late Sarmatian (Anomalinoides dividens, Varidentella reussi
and Porosononion granosum horizons).

Subsequent research, based on calcareous nannoplankton,

was  conducted  by  Oszczypko-Clowes  in  the  Sokołów-
Smolarzyny  area  (Oszczypko-Clowes  in:  Krzywiec  et  al.
2008) and provided more accurate results. The obtained data
gave  evidence  for  the  NN6  Zone  in  the  lower  part  of  the
Machów Formation profile and for the NN7 Zone in the upper
part (Early and Late Sarmatian). The NN6 Zone was defined
by the absence of Sphenolithus heteromorphus and Discoaster
kugleri and by the presence of Helicosphaera walbersdorfen-
sis  and  Cyclicargolithus  floridanus.  Assignment  of  the  NN7
Zone was based on the presence of Coccolithus miopelagicus
and Calcidiscus macintyrei. The oldest deposits belonging to
the  lower  fine-grained  complex,  evaporites  and  possible
subevaporites,  were  not  studied  because  of  lack  of  bio-
stratigraphical documentation.

The latest micropaleontological studies (Garecka &

Olszewska 2011) of the Middle Miocene deposits in SE Poland
and Western Ukraine confirm the reliability of the foraminiferal
zones described by Łuczkowska (1964), and high correlation

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Fig. 5. Lithological log of the core material from the Stobierna 3 borehole.

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degree between Polish and Ukrainian assemblages, what was
also  indicated  by  Łuczkowska  (1964).  This  research  also
showed  the  similarity  of  calcareous  nannoplankton  associa-
tions  from  the  Polish  and  Ukrainian  part  of  the  Carpathian
Foredeep. In the assemblages of the upper part of the NN6 and
the lower part of the NN7  Zone  the gradual impoverishment
of species was noticed (Garecka & Olszewska 2011).

Geological setting

In 2006 the authors profiled and sampled for the calcareous

nannoplankton studies the core material from the boreholes:

Stobierna 3 (515—524 m to 1733—1737 m, together 51 boxes)
(Figs. 5, 6), Stobierna 4 (1016—1021 m to 1237—1238 m, to-
gether 22 boxes) (Figs. 7, 8), Stadnicka Brzóza 1 (350—356 m
to 1687—1991 m, together 28 boxes) (Fig. 9). The short char-
acteristic of core material is summarized in Table 1. We also
collected samples from the Stobierna 2 and Pogwizdów 2
boreholes.

The studied area is located mainly within the so-called

“Rzeszow anhydrite-less island” (Komorowska-Błaszczyńska
1965; Oszczypko et al. 2006). This allows us to include the
thick Miocene (Upper Badenian/Sarmatian) sequence: 1707 m
(Pogwizdów 2) to 1936 m (Stobierna 1) in the Machów For-
mation (Alexandrowicz et al. 1982; Jasionowski 1997).

Fig. 6. Photographs of the core material from the Stobierna 3 borehole. Thin-bedded heteroliths. A – depth interval 834—843 m, IV– fine-
grained silty heteroliths with discrete convolution; B – depth interval, 1113—1122 m, V – sandy/claystone thin-bedded heteroliths with hori-
zontal and diagonal through lamination; C – depth interval 1290—1299 m, I – silty/mudstone, thin-bedded heteroliths with diagonal, stripped
lamination; D – depth interval 1290—1299 m, V – silty/mudstone thin-bedded heteroliths with diagonal, stripped lamination; E – depth in-
terval 1660—1669 m, V – silty heteroliths with horizontal lamination; F – depth interval 1660—1669 m, VII – silty/mudstone horizontal
stripped lamination.

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In the Sokołów area the Badenian/Sarmatian boundary is

largely conventional, and coincides with the first appearance of
species Anomalinoides dividens (Łuczkowska 1964; Dziadzio
et al. 2006), which can be roughly correlated with the upper part
of the nannoplankton NN6 Zone (Marunteanu 1999; Kováč et
al. 2006; Oszczypko-Clowes in Krzywiec et al. 2008).

The described core material is characterized by a monoto-

nous lithology (Table 1, Figs. 5—9). Larger differences in
lithology are visibly only on the graphs of well logging.

On this basis, Papiernik (in Krzywiec et al. 2008) distin-

guished four lithofacies: sandy-FPC (clays 0—25 %), sandy/
clayey-FP/I (clays 25—50 %), clayey-sandy FI/P (clays 50—
75 %) and clayey FI (clays more than 75 %).

On the basis of the description of the borehole cores the

following lithofacies have been distinguished: hemipelag-
ites, thin-bedded heteroliths, classical turbidites and thick-
bedded sandstones (cf. Porebski & Warchoł 2006).

Hemipelagites (facies D2.3, Pickering et al. 1986) are repre-

sented by dark grey, marly, mudstones with discrete horizon-
tal lamination. Bright laminas 1—2 mm thick are formed from
fine  particles  of  quartz  and  muscovite.  Laminas  a  few  milli-
meter  thick  composed  of  very  fine-grained  sand  are  rare.  In
mudstones fine crushed thin-skinned fauna are ofen observed.
The thickness of mudstone intercalations are usually from 0.5
to 2—3 m. The thickest package of mudstone with a thickness
of  at  least  9 m  was  found  in  the  borehole  Stobierna 3  (depth
interval 715—724 m). These sediments were deposited by low-
density suspension currents or weak bottom currents.

Thin-bedded heteroliths (D2.1, Pickering et al. 1986), usu-

ally  intercalated  by  hemipelagites,  are  characterized  by
rhythmic intercalations of very thin-bedded sandstones, silt-
stones  and  mudstones.  The  sandstones  display  lenticular,
stripped  and  wavy  stratification.  Muddy/sandy  and  sandy/
muddy heteroliths can be distinguished in the studied cores.
The muddy/sandy heteroliths are characterized by layer-cake
of  mudstones  and  very-fine  sandstones  with  a  thickness  of
2 mm to 1.5—2.0 cm. The thicker laminas display low-angle
diagonal  lamination  and  small  load-casts.  In  sandy/muddy
heteroliths the thickness of thin layers of sandstone is greater
than  in  the  mudstone  variety.  At  the  top  of  sandstones,  the
accumulation of coalified plants is often observed. The het-
eroliths  were  deposited  by  low-density  currents  or  bottom
currents  with  suspension  traction.  Classical  turbidites
(C2.2—C2.3,  Pickering  et  al.  1986)  were  uncommonly  ob-
served. Almost always they were layers of fine-grained sand-
stone about 10 cm thick. These sandstones are characterized
by lime-muddy cement. The sandstones display typical Bou-
ma  sequence  of  stratification  typical  sequence:  ripple  cross
lamination,  convolution  and  the  upper  parallel  lamination.
The  thicker  sandstone  layers  (up  to  15 cm)  also  contained
turbidite Tbc + conv. The thin-bedded turbidites were depos-
ited by low-density turbidite flows.

Thick-bedded sandstones (0.4—1.0 m) (B1.1, Pickering et al.

1986) are usually structureless, brittle and poorly-cemented,
muscovitic, medium to fine-grained, with minor levels of
muddy clasts. Sometimes the top of fine-grained sandstone is
more strongly cemented than the basal part of beds. The sand-
stones were deposited by high-density suspension currents, by
rapid mass deposition as a result of intergranular collisions.

Fig. 7. Lithological log of the core material from the Stobierna 4
borehole.

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Fig. 9. Lithological log of the core material from the Stadnicka Brzóza borehole.

Fig. 8. Photographs of the core material from the Stobierna 4 borehole. Thin-bedded, layer-cake, muddy/silty/sandy heteroliths, with hori-
zontal laminations: A – depth interval 1229—1238 IV; B – depth interval 1229—1238 V; C – depth interval 1229—1238 VI; D – depth
interval 1229—1238 V. (A,B,C) and diagonal-stripped lamination.

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Lithofacies described by us can be roughly correlated with

those defined on the basis of well logging curves (Papiernik
in Krzywiec et al. 2008): hemipelagites = clayey facies;
heteroliths and thin-bedded turbidites = sandy/clay facies;
thick-bedded sandstones = sandy facies (Figs. 5—9).

Material and methods

Our studies of the Machów Formation were concentrated in

the eastern part of the PCFB, north of Rzeszów (Figs. 1, 2). In
this area, 33 samples were collected from five boreholes at the
following  depth  intervals:  Stobierna 2  (S-2):  1016—1338 m
(5  samples);  Stobierna 3  (S-3):  715—1669 m  (10  samples);
Stobierna 4  (S-4):  1016—1238 m  (7  samples);  Stadnicka
Brzóza 1 (SB-1): 350—356 m and 1043—1667 m (7 samples);
Pogwizdów  (P-2):  1161—1390 m  (4  samples).  The  upper-
most  (above  350 m)  and  lowermost  (beneath  1669 m)  parts
of the Machów Formation were not studied because of lack
of core material.

Table 1: Facies characteristic.

All samples were prepared using the standard smear slide

technique and analysed under light microscope Nikon
Eclipse E600POL (LM, 1000 magnification) with parallel
and crossed nicols. Several photographs of specimens taken
in LM are presented in Figs. 10—13.

The qualitative and the quantitative analyses were carried

out for all the samples. The traditional preparation technique
enabled  the  estimation  of  the  relative  abundance  determined
by  counting,  when  possible,  up  to  300  specimens  in  random
fields of view. In order to analyse and calculate the percentage
abundance  of  autochthonous  and  allochthonous  assemblages
the authors accepted the 5 % range error. The paleoecological
analyses  were  performed  on  autochthonous  assemblages.
Abundances were calculated for individual species with an er-
ror range of 0 % – the total amount of autochthonous species
in each of the slides is equal to 100 %. The calcareous nanno-
fossil distribution (nominal values as well for all species and
percentages only for the autochthonous species) in each bore-
hole is listed in Appendix and electronic edition of Tables 3—7
included at www.geologicacarpathica.sk.

Depth [m]

Facies characteristic

STOBIERNA 3

515 – 524
(1)

The laminated grey siltstone with intercalations of fine- to medium-grained muscovite, poorly cemented, massive medium (15 cm)
to thick-bedded (50 cm) sandstones, with fragments of crushed fauna.

715 – 724
(2)

The dark grey, marly claystones and mudstones with discrete horizontal lamination, numerous small fragments od crushed fauna.
(3 samples)

834 – 843
(3)

At the top 3 m thick packet thick-bedded (up 1.5 m) fine- to medium-grained, polimictic sandstones with fine muddy clasts. Below
the grey sand-muddy heteroliths with intercalations, thin-bedded fine-grained, muscovite sandstones with horizontal and ripple-
cross lamination. subordinate occur the medium to thick-bedded muscovitic sandstones (60 cm), with dispersed coalified plants,
low-angle cross-lamination, dish-structure. (1 sample)

1113 – 1122
(4)

Grey muddy-sandy heteroliths with laminated mudstones.

1290 – 1299
(5)

Grey sandy-muddy heteroliths with intercalation of thin-bedded (to 10 cm), fine-grained turbidites (Tc+konv+d). (1 sample)

1660 – 1669
(6)

Muddy-sandy heteroliths. Mudstones with horizontal lamination, thin-bedded, very-fine-grained sandstones with horizontal and
low-angle cross lamination, fine load casts.

1733 – 1737
(7)

Variegated (green and red) metaargilites (Lower Cambrian–Precambrian).

STOBIERNA 4

1016 – 1021
(1)

Very thin-bedded (2–4 cm), very fine-grained, muscovitic sandstones. Mudstones with horizontal lamination, sandstones with
horizontal and ripple cross-lamination. At the top of sandstones bed lenticular piritizidet coalified flakes.

1116 – 1125
(2)

Muddy-sandy heteroliths. Mudstones with horizontal lamination, fine-grained sandstones (up to 4 cm) with ripple-cross lamination.
Number of lamines up to 3 mm with coalified, pyrititizid plants.

1229 – 1238
(3)

Muddy-sandy heteroliths. Mudstones with horizontal lamination; thin-bedded (0.5–3.5 cm), fine-grained, muscovitic sandstones
with ripple cross-lamination.

STADNICKA BRZÓZA 1

350 – 356
(1)

Muddy-sandy heteroliths.

1043 – 1047
(5)

Grey laminated mudstones, crushed. (1 sample)

1175 – 1179
(6)

Muddy-sandy heteroliths, crushed. In last box 10 cm fine-grained sandstone with intercalations of laminated mudstones. Sample 1.

1327 – 1331
(7)

Sandy-muddy heteroliths. Fine-grained, muscovitic sandstones, up to 5 cm thick, with coalified flakes. Low angle cross lamination.

1498 – 1502
(8)

Sandy-muddy heteroliths. Fine-grained, muscovitic sandstones, up to 5 cm thick, with coalified flakes. Low angle cross-lamination.

1586 – 1590
(9)

Sandy mudstones, laminatem, with intercalations fine- to medium-grained, muscovitic, thin to thick-bedded sandstones (up 60 cm),
crushed sandstones with dispersed coalified flakes.

1625 – 1629
(10)

Fine-grained, thick-bedded (up 60 cm) sandstones with coalified flakes. Lower sandy-muddy heteroliths.

1663 – 1667
(11)

Muddy-sandy heteroliths with intercalations fine- and very fine-grained sandstones with horizontal lamination.

1687 – 1691
(12)

Metaargilites (Lower Cambrian–Precambrian).

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Fig. 10. LM microphotographs of the typical Miocene nannofossil assemblages. A, B – Braarudosphaera bigelowii (S-3 715-724 I);
C, D – Calcidiscus leptoporus (S-3 715-724 I); E, F – Calcidiscus premacintyrei (S-3 715-724 IX); G, H – Coccolithus miopelagicus
(S-3 715-724 I); I, J – Coccolithus miopelagicus (S-3 715-724II); K, L – Coccolithus pelagicus (S-3 715-724I); M, N – Coronocyclus ni-
tescens (S-3 715-724 I); O – Cyclicargolithus floridanus (S-4 1229-1238 V); P – Discoaster deflandrei (S-4 1116-1125 I); R – Discoaster
deflandrei (S-3 1113-1122 II); S – Discoaster variabilis (S-3 834-843 VIII); T – Helicosphaera carteri (S-3 715-724 IX); U – Helico-
sphaera carteri (S-4 1116-1125 I); W, Y – Helicosphaera carteri (S-4 1116-1125 I); Z, Ź – Helicosphaera intermedia (S-3 715-724 I).

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The relative abundance is a good indication of the general

assemblage character, but rare sampling, due to available core
material,  makes  paleoecological  interpretation  problematic.
Another significant issue results from the large amount of re-
deposited  material.  In  our  work  species  with  different  strati-
graphical  range  were  included  in  the  allochthonous  group.
Among  the  long-ranging  taxa  we  cannot  distinguish  whether
the specimen is autochthonous or not. The occurrence of taxa
resistant to carbonate dissolution may also improve their rela-
tive frequencies. That may strongly affect the real abundance.

Fig. 11. LM microphotographs of the typical Miocene nannofossil assemblages. A – Helicosphaera intermedia (S-3 715—724 II);
B – Helicosphaera walbersdorfensis (S-4 1229—1238 V); C – Helicosphaera walbersdorfensis (S-3 1113—1122 II); D – Pontosphaera dis-
copora (S-4 1116—1125 IX); E – Pontosphaera multipora (S-4 1116—1125 IX); F – small Reticulofenestra (S-4 1116—1125 I); G – Reticu-
lofenestra pseudoumbilica (S-4 1229—1238 VII); H, I – Solidopons petrae (S-3 715—724 II); J, K – Rhabdosphaera clavigera (S-3
834-843 IV); L, M – Sphenolithus abies (S-3 715—724 II); N – Sphenolithus moriformis (S-3 715—724 IX); O, P – Umbilicosphaera rotula
(S-4 1116—1125 IX).

Results

Autochthonous versus reworked nannofossils – assem-
blages description

The majority of the examined samples yielded abundant

and  relatively  well  preserved  assemblages.  Some  taxa  were
medium well or poorly preserved in the form of small frag-
ments  or  with  broken  elements  what  made  identification
questionable.  Traces  of  specimen  dissolution  were  not  ob-

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Fig. 12. LM microphotographs of the typical reworked nannofossil assemblages. A, B – Chiasmolithus bidens (S-3 715-724 VIII);
C, D – Chiasmolithus modestus (S-4 1016-1021 II); E, F – Chiasmolithus oamaruensis (S-3 834-843 VIII); G, H – Chiasmolithus solitus
(S-4 1229-1238 VII); I – Cyclicargolithus abisectus (S-3 715-724 I); J – Cyclicargolithus luminis (S-3 715-724 IX); K – Dictyococcites
bisectus (S-4 1016-1021 II); L – Discoaster barbadiensis (S-3 715-724 I); M – Discoaster multiradiatus (S-3 834-843 VIII); N – Dis-
coaster tanii nodifer (S-3 715-724 IX); O – Ericsonia fenestrata (S-3 834-843 VIII); P, R – Ericsonia formosa (S-4 1229-1238 V); S – Eric-
sonia subdisticha (S-4 1016-1021 II); T – Helicosphaera bramlettei (S-3 715-724 IX); U – Helicosphaera bramlettei (S-3 715-724 IX).

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Fig. 13.  Typical,  reworked  nannofossil  assemblages.  A  –  Helicosphaera  euphratis  (S-3  715-724 I);  B  –  Helicosphaera  recta  (S-3
1113-1122 II); C – Helicosphaera perch-nilseniae (S-3 715-724 I); D – Helicosphaera waltrans  (S-3 715-724 IX); E, F  – Isthmolithus
recurvus (S-3 834-843 IV); G – Lanternithus minutus (S-4 1116-1125 IX); H – Pontosphaera latelliptica (S-4 1116-1125 IX); I, J – Ponto-
sphaera plana (S-3 715-724 I); K – Pontosphaera plana (S-4 1229-1238 VII); L, M – Pontosphaera rothi (S-3 715-724 IX); N – Reticu-
lofenestra dictyoda (S-4 1229-1238 V); O – Reticulofenestra hillae (S-3 715-724 IX); P – Reticulofenestra lockerii (S-4 1229-1238 VIII);
R – Reticulofenestra ornata (S-4 1229-1238 VII); S – Reticulofenestra reticulata (S-4 1229-1238 V); T – Reticulofenestra umbilica (S-3
834-843 IV);  U – Sphenolithus conicus (S-3 834-843 VIII).

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served. Only 3 samples from S-3 (1660—1669 VI, 1660—1669 II
and 1290—1295 II) and 2 samples from S-4 (1229—1238 VII
and 1116—1125 IV) revealed relatively lower quantities of
specimens which resulted in their total number under 300.
These variations in the abundances could be associated with
volumetric differences in the amount of sampled material. In
the case of poor sampling, the odds of finding rare species is
thus reduced.

For each sample the autochthonous/reworked nannofossils

ratio was estimated (Fig. 14). The autochthonous assemblag-
es in each examined borehole, as mentioned above, were ac-
companied by frequently occurring reworked nannofossils of
Cretaceous, Paleogene and Early Miocene age. The percent-
age of allochthonous assemblages oscilates between 40 and
60 % and could be even higher due to unseparated long-liv-
ing forms (e.g. Coccolithus pelagicus, Cyclicargolithus
floridanus).

The distribution patterns of autochthonous nannofossils

are illustrated in electronic edition of Tables 3—7 included at
www.geologicacarpathica.sk.

The Miocene association in S-2 is formed by abundant oc-

currences  of  Coccolithus  pelagicus  and  Cyclicargolithus
floridanus  and  relatively  common  Helicosphaera  carteri,
Sphenolithus  moriformis,  Reticulofenestra  pseudoumbilica
and small reticulofenestrids. Assemblages are also character-
ized  by  the  frequent  presence  of:  Pontosphaera  discopora,
Pontosphaera  multipora,  Coccolithus  miopelagicus,  Heli-
cosphaera  walbersdorfensis,  Coronocyclus  nitescens,  Sphe-
nolithus  abies  and  Umbilicosphaera  rotula.  Sporadic
specimens  were  observed  of  Braarudosphaera  bigelowii,
Calcidiscus leptoporus, Calcidiscus macintyrei, Calcidiscus
premacintyrei, Discoaster variabilis, Discoaster exilis, Heli-
cosphaera intermedia and Helicosphaera stalis.

The nannoplankton assemblage from S-3, similarly to S-2,

is  mostly  represented  by  species  such  as  C.  pelagicus  and
Cy. floridanus, H. carteri, S. moriformis, R. pseudoumbilica,
small  reticulofenestrids.  The  following  were  also  observed
with  relatively  high  frequency:  P.  multipora,  S.  abies,  U.
rotula,  C.  nitescens,  C.  miopelagicus,  H.  walbersdorfensis,
P. discopora, H. intermedia and Cd. leptoporus in the upper
part of the profile (from 715—724 VIII). From 834—843 VIII
common occurrences of  C. miopelagicus  > 10 µm were no-
ticed.  Such  species  as  B.  bigelowii  and  Cd.  premacintyrei
were present in lower numbers. Discoaster variabilis and D.
deflandrei  were  recognized  only  in  a  few  samples.  In  three
samples  from  the  lower  part  of  the  profile  (1660—1669 VI,
1660—1669 II,  1290—1295 II)  with  a  lower  quantity  of
specimens, high numbers of C. pelagicus and Cy. floridanus
were observed.

In S-4 the assemblage is also characterized by common

presence of species such as: C. pelagicus and Cy. floridanus,
H.  carteri,  S.  moriformis  and  small  reticulofenestrids.  The
following  also  frequently  occurred:  P.  multipora,  S.  abies,
U.  rotula,  P.  discopora,  C.  nitescens,  C.  miopelagicus,  H.
walbersdorfensis, R. pseudoumbilica, H. intermedia, B. bige-
lowii and Cd. leptoporus. Irregularly occurring specimens of
Cd.  premacintyrei  and  Rhabdosphaera  clavigera  were  rec-
ognized only in 2 samples from the upper part of the profile
(1116—1125 I,  1016—1016—1021 II).  In  sample  1116—1125 I

with a total number of specimens under 300, the similar dis-
proportion of species percentage was noticed – common
species such as C. pelagicus and Cy. floridanus quantitatively
prevails over the other species.

Within the assemblage from SB-1, C. pelagicus and Cy.

floridanus  occurred  with  explicit  dominance  over  the  other
species. Species such as H. carteri, small reticulofenestrids,
S. moriformis, R. pseudoumbilica, P. multipora, P. discopo-
ra,  H.  walbersdorfensis,  C.  nitescens,  and  C.  miopelagicus
were observed frequently. U. rotula, S. abies, D. deflandrei
were noticed  in  lower  numbers.  Specimens  of  B.  bigelowii,
Cd. premacintyrei, D. variabilis, D. exilis, H. stalis, H. inter-
media, Triquetrorhabdulus rugosus, R. clavigera and Holo-
discolithus macroporus were recognized sporadically. In one
sample  from  the  uppermost  of  the  profile  350—356 I  a  few
specimens  of  C.  miopelagicus  >10 µm  and  D.  challengeri
were identified.

In P-2 the assemblage mostly consisted of C. pelagicus and

C.  floridanus.  Such  species  as  small  reticulofenestrids,  S.
moriformis, H. carteri, H. walbersdorfensis, P. multipora, P.
discopora, R. pseudoumbilica and C. nitescens with relatively
high occurrence were noticed. Specimens of B. bigelowii, Cd.
leptoporus, C. miopelagicus, D. deflandrei, H. stalis, H. inter-
media,  H.  macroporus,  U.  rotula,  Cd.  premacintyrei  and  S.
abies  occur  irregularly.  Cd.  macintyrei,  R.  clavigera,  D.
variabilis and T. rugosus were observed sporadically.

Biostratigraphy

The standard Miocene nannofossil zonation was constructed

mainly  on  the  basis  of  the  Discoasteraceae  representatives.
Distribution of this group is presumably controlled ecologi-
cally  and  depends  on  paleogeography.  Therefore  this  Mio-
cene  subdivision  is  easily  accomplished  in  low  latitudes
where  discoasters  are  common  in  the  open  oceanic  nanno-
plankton assemblages (Perch-Nielsen 1985). It is problemat-
ic in high latitudes, due to their absence or rare occurrence,
and  in  marginal  marine  assemblages  where  discoasters  and
other markers occur sporadically (Perch-Nielsen 1985). This
also  applies  to  other  index  species,  which  commonly  occur
only at lower latitudes. Therefore, the Miocene zonations of
Martini & Worsley (1970) and Bukry & Okada (1980) work
best for areas from low latitudes. Given the Miocene paleo-
biogeographical and paleoecological diversity of calcareous
nannoplankton,  a  number  of  regional  divisions  modifying
previously  formed  zonations  were  proposed  (Roth  et  al.
1971;  Műller  1978;  Raffi  &  Rio  1979;  Theodoridis  1984;
Raffi  et  al.  1995;  Fornaciari  &  Rio  1996;  Fornaciari  et  al.
1996; Young 1998; Švábenická 2002 and Ćorić & Švábenická
2004).  According  to  Báldi-Beke  (1982)  helicoliths  are
neither  strictly  oceanic  nor  typical  nearshore  nannofossils
(see Švábenická 2002). This fact resulted in their expansion
in  unstable  paleoecological  conditions  in  the  Carpathian
Foredeep and hence in increase of their biostratigraphical sig-
nificance (Švábenická 2002). The composition of nannoplank-
ton  assemblages  from  Stobierna 2,  Stobierna 3,  Stobierna 4,
Pogwizdów 2  and  Stadnicka  Brzóza 1  boreholes  allowed
authors to establish the presence of Zones NN6 and NN7. The
detailed description of these zones is given below.

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Discoaster exilis Zone (NN6)

Discoaster exilis zone assignment is based on the presence

of  Reticulofenestra  pseudoumbilica,  Sphenolithus  abies,
Helicosphaera  stalis,  Helicosphaera  walbersdorfensis  and
absence of species such as Sphenolithus heteromorphus and
Discoaster kugleri. From biostratigraphical point of view the
stratigraphic range of Helicosphaera walbersdorfensis is sig-
nificant.  Its  first  appearance  occurs  in  the  highest  part  of
NN5 and the last occurrence is near the NN6/NN7 boundary
(Fornaciari  et  al.  1996;  Young  1998,  see  also  Dudziak  &
Łaptaś  1991).  Müller  (1981)  was  the  first  who  noticed  the
utility of that species in Miocene biostratigraphy for the NN6
Zone. In addition the presence of Cyclicargolithus floridanus
is important due to its last common occurrence taking place in

Fig. 14. Percentage abundance of autochthonous and allochthonous
(reworked) species in samples from the Stobierna 2, Stobierna 3,
Stobierna 4, Pogwizdów 2, Stadnicka Brzóza 1 boreholes.

the  middle  part  of  the  NN7  Zone  with  an  age  of  13.33 Ma,
(Gradstein et al. 2004). In most samples bigger specimens of
Reticulofenestra pseudoumbilica were observed, as is charac-
teristic  for  the  NN6  Zone  (cf.  Fornaciari  &  Rio  1996).  The
smaller  representatives  of  Reticulofenestra  pseudoumbilica
were  already  recognized  in  the  NN2  Zone  (Marunteanu
1992,  see  also  Oszczypko-Clowes  2001;  Holcová  2005).
Moreover,  Sphenolithus  abies  and  Helicosphaera  stalis  are
very  significant  species  characteristic  for  the  higher  part  of
NN6 (cf. Young 1998). In all profiles, besides these above-
mentioned  species,  there  are  frequent  occurrences  of  such
species  as  Coccolithus  pelagicus,  Cyclicargolithus  florida-
nus,  Helicosphaera  carteri,  Sphenolithus  moriformis  and
Umbilicosphaera rotula, what is also characteristic for NN6
Zone.  Sporadic  Calcidiscus  leptoporus  and  Calcidiscus

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premacintyrei  were  observed.  The  estimated  age  for  the  top
regular occurrence of Cd. premacintyrei is 12.45 Ma (Gradstein
et  al.  2004).  According  to  the  standard  zonation  (Martini
1971)  the  LO  of  Sphenolithus  heteromorphus  marks  the
NN5/NN6  boundary.  It  is  important  to  notice  the  fact  that
these species were observed in the samples. However, taking
into  account  the  presence  of  Sphenolithus  abies,  Heli-
cosphaera  stalis  and  Coronocyclus  nitescens,  it  is  possible
to  assume  that  the  presence  of  Sphenolithus  heteromorphus
is due to reworking. The age of the top occurrence of C. nite-
scens is 12.45 Ma (Gradstein et al. 2004).

Discoaster kugleri Zone (NN7)

The Discoaster kugleri Zone (NN7) is usually defined by

the  first  occurrence  of  Discoaster  kugleri  (Martini  1971;
Bukry  &  Okada  1980)  to  the  first  occurrence  of  Catinaster
coalitus. It is worth noting that in borehole Stobierna 3 (depth
715—724 m)  and  Stadnicka  Brzóza 1  (depth  350—356  m)  the
first  appearance  of  Calcidiscus  macintyrei  and  Coccolithus
miopelagicus  ( > 14 µm)  takes  place.  Many  researchers  sug-

ually  decreases,  what  also  could  indicate  NN7  Zone.  Dis-
coaster  deflandrei  occurs  occasionally,  which  is  typical  for
this interval. Discoaster deflandrei becomes very rare and dis-
appears near the top of this zone (Perch-Nielsen 1985). Like-
wise  Calcidiscus  premacintyrei  occurs  rarely,  and  its  last
occurrence is established as the indicator of the NN7 Zone.

Paleoecology

The paleoecological analysis of the Machów Formation was

carried out on the basis of quantitative data of autochthonous
assemblages in S-2, S-3, S-4, SB-1 and P-2. Paleoecological
nannoplankton  preferences  were  considered  with  regard  to
temperature and nutrient availability (Table 2). According to
the  way  of  sampling,  restricted  to  particular  intervals,  the
assemblage  descriptions  are  divided  into  three  parts
(Figs. 15, 16).  The  first  considers  the  depth  between  1700
and 1550 m, the second from 1400 to 1000 m and the last the
depth between 850 and 700 m (Figs. 15, 16).

Temperature. According to Andreyeva-Grigorovich

(2002) the Late Badenian and Early Sarmatian calcareous

Temperature Trophism

Warm-water

species

Moderate

species

Cold-water

species

Others Eutrophic

species

Oligotrophic

species

Others

Stobierna 2
1190–1208 I

1190–1208 XVI

1208–1222 X

1320–1338 IV

1320–1338 XIII

Stobierna 3
715–724 I

715–724 II

715–724 VIII

715–724 IX

834–843 IV

834–843 VIII

1113–1122 II

1290–1295 II

1660–1669 II

1660–1669 VI

Stobierna 4
1016–1021 II

1116–1125 I

1116–1125 IV

1116–1125 IX

1229–1238 V

1229–1238 VII

1229–1238 VIII

Stadnicka Brzóza 1
350–356 I

1043–1047 II

1175–1179 III

1327–1331 II

1586–1590

1586– 1590 I

1663–1667 III

Pogwizdów 2
1161–1170 I

1161–1170 VIII

1381–1390 II

1381–1390 IX

Table 2: Percent abundance of main paleoecological groups.

gest using alternative indicators, such
as  the  last  common  occurrence  of
Calcidiscus  premacintyrei,  which
takes  place  just  before  the  first  oc-
currence of Discoaster kugleri (For-
naciari  et  al.  1996)  or  the  last
occurrence  of  Coronocyclus  nite-
scens and Calcidiscus premacintyrei
(Raffi  et  al.  1995).  This  is  because
of  the  absence  or  scarce  abundance
of the index species, especially Dis-
coaster kugleri. It regards especially
high  latitude  areas,  where  discoast-
ers or Catinaster coalitus are practi-
cally uncommon. That is the reason
why  assignment  of  the  NN7  Zone
was  based  mainly  on  large  speci-
mens  of  Coccolithus  miopelagicus
( > 14 µm) and Calcidiscus macinty-
rei. The age of the top occurrence of
Cd.  macintyrei  is  estimated  as
14.46 Ma  (Gradstein  et  al.  2004).
Presence  of  Coccolithus  miopelagi-
cus  ( > 14 µm)  is  essentially  con-
fined just to that interval, but its first
occurrence  is  gradational  (Young
1998). The first appearance of Calci-
discus macintyrei is a controversion-
al  issue.  According  to  Fornaciari  et
al. (1996) and Young (1998), it takes
place  near  the  NN6/NN7  boundary.
However  Švábenická  (2002)  and
Ćorić & Švábenická (2004) describe
this  species  as  early  as  from  the
NN6  and  even  from  NN5  Zone.
Specimens  of  Catinaster  coalitus
were  not  observed.  The  percentage
of Cyclicargolithus floridanus grad-

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Fig. 15.  Percentage  abun-
dance  of  taxa  with  different
temperature  preferences  ver-
sus  depth,  from  the  Stobier-
na 2, Stobierna 3, Stobierna 4,
Pogwizdów 2, Stadnicka Brzó-
za 1 boreholes.

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nannofossils  were  divided  into  7  ecogroups  depending  on
temperature preferences: the groups of tropical and subtropi-
cal  species  (I  –  Sphenolithus,  II  –  Discoaster,  III  –
Braarudosphaera), groups of moderate species (IV – Calci-
discus,  V  –  Helicosphaera)  and  groups  of  cold-water  spe-
cies (VI—VII – Coccolithus + Reticulofenestra). Among the
recognized  assemblages  the  warm-water  species  group  was
represented  by  B.  bigelowii,  C.  miopelagicus,  D.  challeng-
eri, D. deflandrei, D. exilis, D. variabilis, S. abies, S. mori-
formis  and  small  reticulofenestrids.  The  moderate  species
group consisted of such species as  Cd. leptoporus, Cd. ma-
cintyrei,  Cd.  premacintyrei,  H.  carteri,  H.  intermedia,  H.
stalis, H. walbersdorfensis. The cold-water species group in-
cludes: C. pelagicus, Cy. floridanus, and R. pseudoumbilica.

At the depth 1700—1550 m, samples were collected from

the  S-3  and  SB-1  boreholes.  In  the  S-3  borehole  (samples
1660—1669 VI  and  1660—1669 II)  the  assemblages  are  domi-
nated by cold-water species over the moderate and warm-wa-
ter species. The percentage abundance of cold-water species is
up to 65 % and 49 % respectively. Similarly in SB-1, in sam-
ples  from  the  lowermost  part  of  the  profile:  1663—1667 III,
1586—1590 I, 1586—1590, cold-water species are predominant
(50 %, 55 %, 70 % respectively) (Table 2, Fig. 15).

At the second depth interval, 1400—1000 m, samples from

each  profile  were  analysed  (Table 2,  Fig. 15).  In  P-2  at  the
depth 1381—1390 m, from IXth and IInd meter, paleoecological
groups  are  characterized  by  dominance  of  cold-water  species
participation (61 and 68 %), whereas warm-water and moderate
species percentages are comparable and do not exceed 15 %. A
similar  situation  is  found  in  SB-1  at  the  depth  1327—1331 II.
Cold-water  species  occur  with  high  abundance  reaching  up  to
65 %. In the S-2 borehole, in samples collected from the inter-
val  1320—1338 m,  XIIIth  and  IVth  meter,  likewise  in  S-3  at
the depth 1290—1295 II, the percentage of cold-water species
is prevailing (50 %, 73 % and 49 % respectively), whereas the
warm-water species group is more abundant than the moder-
ate-water species. In S-4 in samples collected from the interval
1229—1238 m,  from  VIIIth,  VIIth  and  Vth  meter,  differences
between  percentage  abundance  of  cold-  and  warm-water  spe-
cies  are  not  significant.  The  temperate  water  species  group  is
slightly less numerous in the lower part of the profile, but in the
upper part it equals the others in frequency. In S-2 in samples
from  1208—1222 X,  1190—1208 XVI  and  1190—1208 I,  cold-
water  species  abundance  oscillates  around  50 %  in  the  whole
autochthonous  assemblage,  whereas  warm-water  species  pre-
vail  over  moderate  ones.  In  SB-1  at  the  depth  1175—1179 III,
cold-water  species  are  still  predominant  (63 %),  temperate
reaching not more than 2 %. In P-2 at 1161—1170 m, from the
VIIIth  and  Ist  meter,  cold-water  species  percentage  is  around
50 %, whereas the contribution of warm-water species is twice
as much as temperate. In S-4 at the depth 1116—1125 I, at the
Xth, IVth and Ist meter, some variations were noticed. In the
sample from the IXth meter warm-water species slightly pre-
vail over cold ones, whereas at the IVth meter the percentage
of  cold-water  species  increased  to  60 %.  At  the  Ist  meter
warm-water species abundance increased to 33 % and temper-
ate  (26 %)  prevail  over  cold  ones  (17 %).  In  S-3  in  sample
1113—1122 II the cold-water/warm-water species ratio is 31 to
29 %,  with  lower  frequency  of  moderate  species  (14 %).  In

SB-1 in the sample collected from 1043—1047 II, cold-water
species prevail over the warm group (43 % to 29 %). In S-4 in
sample 1016—1021 II, warm-water species participation is
35 %, whereas cold ones is 20 %, likewise moderate – 20 %
(Table 2, Fig. 15).

The last depth interval between 850 and 700 m was sam-

pled  only  in  S-3  (Table 2,  Fig. 15).  At  the  depth  834—
843 VIII,  warm-  and  cold-water  species  participations  both
reach  36 %  (moderate – 10 %).  In  the  same  interval,  but
from  IVth  meter  warm-water  species  substantially  prevail
over the cold-water (32 %) and moderate (5 %) ones. In sam-
ples  715—724 IX  and  715—724 VIII  the  difference  between
participation of the cold- and warm-water groups is not signif-
icant.  In  the  upper  part  of  the  profile,  in  samples  715—724 II
and  715—724 I,  predominance  of  warm-water  species  group
was noticed with its participation twice as much as cold ones.

Trophic resources. With regard to nutrient availability,

two  paleoecological  groups  were  distinguished  among  the
autochthonous  assemblages:  species  preferring  eutrophic
and species preferring oligotrophic conditions (Wei & Wise
1990;  Aubry  1992;  Krhovský  et  al.  1992).  The  following
species were assigned to the former group:  B. bigelowii, C.
pelagicus, Cy. floridanus, P. discopora, P. multipora and R.
pseudoumbilica. The latter group includes species such as D.
challengeri, D. deflandrei, D. exilis, D. variabilis, H. carteri,
H.  intermedia,  H.  stalis,  H.  walbersdorfensis,  S.  abies,  S.
moriformis and small reticulofenestrids.

In the first analysed interval between 1700 and 1550 m

eutrophic  species  occurring  with  high  frequency,  prevail
over  oligotrophic  species  (Table 2,  Fig. 16).  In  S-3  at  the
depth  1320—1338 XIII  abundance  of  eutrophic  species
reached  up  to  70 %,  whereas  the  oligotrophic  group  consti-
tuted 19 %. At the IInd meter the percentage of oligotrophic
species  increased  to  36 %  with  constant  predominance  of
eutrophic ones (66 %). A similar situation was noticed in SB-1
at  the  depth  1663—1667 III,  1586—1590 I,  1586—1590.  The
abundance of eutrophic species is within the range 63—72 %.

At the second depth (Table 2, Fig. 16) interval, 1400—

1000 m,  in  the  P-2  borehole,  eutrophic  species  abundance
reached up to 62 and 72 % at the depth 1381—1390 m, at IXth
and IInd meter respectively. In the SB-1 borehole at the depth
1327—1331 II  the  percentage  of  eutrophic  species  is  around
70 %.  In  S-2  in  the  sample  from  interval  1320—1338 m,  col-
lected from XIIIth meter, the abundance of eutrophic species
is 54 %, with 38 % oligotrophic ones. At the IVth meter in this
interval,  the  percentage  of  eutrophic  species  increased  to
74 %.  In  S-3  at  the  depth  1290—1295 II  the  percentage  of
eutrophic  species  reached  up  to  53 %,  whereas  oligotrophic
ones  is  22 %.  In  S-4  at  the  interval  1229—1238,  within  three
analysed  samples  at  the  VIIIth  meter,  oligotrophic  species
slightly prevail over eutrophic group (43 to 34 % respective-
ly).  At  the  VIIth  meter  the  percentage  of  both  group  oscil-
lates  around  40 %,  and  then  at  the  Vth  meter  oligotrophic
species abundance increased to 47 % whereas eutrophic ones
is  32 %.  In  S-2  in  samples  from  the  depth  1208—1222 X,
1190—1208 XVI  and  1190—1208 I,  the  percentage  of
eutrophic  species  prevails  over  oligotrophic  and  varies  from
57—60 %. In SB-1 at the depth 1175—1179 III, eutrophic spe-
cies abundance is 68 %, whereas oligotrophic is 18 %. In P-2

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Fig. 16.  Percentage  abund-
ance  of  taxa  with  different
trophic  preferences  versus
depth, from the Stobierna 2,
Stobierna 3,

Stobierna 4,

Pogwizdów 2,

Stadnicka

Brzóza 1 boreholes.

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at the interval 1161—1170 m, in samples collected from VIIIth
and Ist meter, oligotrophic species percentage is around 30 %,
whereas eutrophic ones amount respectively to 63 and 57 %.
In  S-4  at  the  depth  1116—1125 I,  at  the  Xth,  IVth  and  Ist
meter,  fluctuations  were  observed.  In  the  lower  part  the  per-
centage of both groups is the same (39 %), whereas at the IVth
meter the percentage of eutrophic species is twice as much as
the  oligotrophic  ones  (64  to  30 %  respectively).  At  the  Ist
meter  abundance  of  oligotrophic  species  is  higher  than
eutrophic  ones  (49  to  32 %).  Likewise  in  S-3  in  the  sample
from  the  depth  1113—1122 II  oligotrophic  species  prevail
over eutrophic, reaching up to 45 and 35 % respectively. In
SB-1 in the sample collected from interval 1043—1047 m at
the IInd meter, the percentage of eutrophic species amounts
to 54 % with 31 % of oligotrophic ones. In turn in S-4 at the
depth  1016—1021 II,  oligotrophic  species  (45 %)  prevail
over the eutrophic ones (35 %) (Table 2, Fig. 16).

At the last depth interval (850 and 700 m), within the

samples from S-3, distribution of examined paleoecological
groups at the beginning, in the sample 834—843 VIII, is char-
acterized by relatively higher abundance of eutrophic species
reaching up to 49 %, whereas oligotrophic species is around
42 % (Table 2, Fig. 16). At the same interval, in the sample
from IVth meter their percentage is equal, around 40 %. At
the interval 715—724 from the IXth meter, oligotrophic spe-
cies begin to prevail over eutrophic ones. The difference at
the IXth and VIIIth meters is the order of a few percent,
whereas at the IInd meter is strongly marked reaching up to
22 % and at the last first meter 14 %.

Discussion

The calcareous nannofossils assemblages from the

Stobierna 2,  Stobierna 3,  Stobierna 4,  Stadnicka  Brzóza 1
and  Pogwizdów 2  boreholes  are  characterized  by  relatively
high  percentages  of  Coccolithus  pelagicus  and  Cyclicargo-
lithus  floridanus  assigned  to  cold-water  taxa.  The  former,
which  is  a  subpolar  species  today,  evolved  in  the  tropical
area  during  the  Early  Cenozoic  and  changed  temperature
preference through geological time (Haq & Lohmann 1976;
Wei & Wise 1990). C. pelagicus is a good paleoclimatic in-
dicator  (Haq  1977),  which  prefers  cold  (7—14 °C)  nutrient
rich  surface  waters  (McIntyre  &  Bé  1976).  Its  high  abun-
dances  are  related  to  intense  upwelling  and  unstable  strati-
fied water column (Rahmann & Roth 1990), which is typical
for coastal environments (Spezzaferri & Ćorić 2001; Ćorić &
Rögl 2004). But it is also well known that this species is re-
sistant to the carbonate dissolution. This could result in im-
provement  of  its  relative  frequency  within  the  associations,
giving a “cold” aspect to the assemblages (Rahmann & Roth
1990; Vulc & Silye 2005). Additionally due to high redepo-
sition and the long-lasting range of these taxa, the real abun-
dance may differ from the estimated values.

In all profiles small reticulofenestrids were observed very

often. The size of coccoliths is associated with seasonal
fluctuations in nutrients and temperature (Gartner et al. 1983/
1984; Kameo 2002) and thus the frequent occurrence of small
reticulofenestrids could be a signal of changes in nutrient dy-

namic. Its bloom is interpreted as a result of influence of warm
waters without upwelling conditions (Ćorić & Rögl 2004).

Pontosphaera multipora occurs at a lower frequency. Oc-

currence of cribriliths secreted by Pontosphaera spp. is con-
sidered indicative of shallower marine environments (Bukry
1971; Bybell & Gartner 1972; Roth & Thierstein 1972;
Edwards 1973; Müller 1976; Aubry 1990). The Ponto-
sphaera spp. shows more variety near shore than in the open
oceanic samples (Perch-Nielsen 1972).

Braarudosphaera bigelowii was noticed sporadically. This

species  was  included  by  Andreyeva-Grigorovich  (2002)  in
the  group  preferring  warm-water  conditions.  B.  bigelowii
was found mostly in coastal waters (Gran & Braarud 1935;
Gaarder 1954; Nishida 1979; Aubry 1989). Previous studies
of Braarudosphaera spp. enrichments in the open ocean sed-
iments  (e.g.  Siesser  et  al.  1992)  show  that  this  genus  is  not
necessarily  linked  to  neritic  environments  but  rather  to
eutrophic  waters  and  reduced  competition  (see  Bartol  et  al.
2008). Its preference for shallow water has been related to wa-
ter depth (Takayama 1972) or to lower salinity and higher tur-
bulence  (Bramlette  &  Martini  1964;  Martini  1965;  Aubry
1989). B. bigelowii is an opportunistic species associated with
stress conditions (Thierstein et al. 2004; Bartol et al. 2008).

The warm-water group includes Sphenolithus moriformis

which  is  numerous  in  all  profiles  and  the  less  abundant  S.
abies. The first one is typical for marine basins with normal
salinity  (Andreyeva-Grigorovich  2002).  Its  great  concentra-
tions  were  observed  in  the  tropical  zones  whereas  S.  abies
was  more  common  in  subtropical  provinces  (Dmitrenko
1993, fide Andreyeva-Grigorovich 2002).

Nannofossil species Helicosphaera carteri, belonging to

moderate  group,  was  observed  in  relatively  high  numbers  in
both profiles. The geographical distribution of the living spe-
cies H. carteri has been interpreted as dependent upon water
temperature (McIntyre & Bé 1967; Okada & Honjo 1973; Oka-
da  &  McIntyre  1979;  Aubry  1990).  H.  carteri  is  eurythermal
and tolerates water temperature as low as 5 °C and as high as
30 °C (Okada & McIntyre 1979; Aubry 1990), but it is more
common  in  tropical  and  subtropical  nannoflora  provinces
(Schneidermann  1977).  This  taxa  is  interpreted  as  a  “near
shore” species (Perch-Nielsen 1985) related to warm shelf and
coastal  environment.  In  open  ocean  it  occurs  very  rarely.  Its
percentage is changeable along the profiles, but its gradual up-
ward trend is noticeable. Thus the presence of H. carteri could
indicate a warm, shallow coastal paleoenvironment.

The species of genus Discoaster, occurring in both pro-

files  with  scarce  frequency,  could  confirm  coastal  environ-
ment as a negative indicator, because discoasterids are more
common in open ocean assemblages (cf. Švábenická 2002).
However it is not an unambiguous marker of paleoecology.
Its  distribution  depends  on  paleogeography.  It  occurs  much
more often in the Mediterranean area than in the Paratethys
(cf.  Perch-Nielsen  1985).  In  addition  epicontinental  marine
sediments usually contain smaller in size and less numerous
specimens  in  comparison  with  sediments  deposited  under
open ocean conditions (Aubry 1984; Švábenická 2002). Pre-
viously it was believed that abundance of discoasterids was
associated  with  latitude  and  declines  with  its  increase  (Wei
S. & Wise W. 1990), but some later studies showed that per-

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Fig. 17. Geological profile, paleobathymetry and main pa-
leoecological changes, from the Stobierna 3 borehole (fa-
cies interpretation log after Krzywiec et al. 2008).

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centage of discoasterids was lower in equatorial regions than
in areas of moderate latitudes (Haq & Lohmann 1976). So it
would  seem  that  there  is  no  evident  dependence  between
abundance  of  this  group  and  water  temperature.  The  Dis-
coaster  genus  was  considered  as  a  warm-water  preferring
group  whereas  among  this  taxa  are  known  species  which
could tolerate lower temperature than those found in both pro-
files: D. variabilis and D. deflandrei. Aubry (1984) describes
them as species which either tolerate or exhibit preference for
colder waters (cf. Švábenická 2002).

The characteristic features of the observed nannoplankton

assemblages together with high number of redeposited nan-

nofossils are interpreted (Fig. 17) as possible indicators of a
shallow  near-shore  environment.  Such    interpretation  is  in
agreement  with  the  one  proposed  by  Garecka  &  Olszewska
(2011).  According  to  these  authors  (Garecka  &  Olszewska
2011), high number of damaged elements of coccoliths may
suggest a strong supply of terrigenous material and unstable
conditions in shallow-water basin.

In the early Late Badenian, as a result of the general shal-

lowing and partial isolation of the basin, on the shelf, the sul-
phate facies of evaporites developed (Krzyżanowice
Formation). This was a kind of platform shelf with a width
of about 75 km (Oszczypko et al. 2006; Oszczypko 2006),

Fig. 18. Paleogeographical map of the Early Sarmatian (based on Popov et al. 2004; Studencka & Jasionowski 2011, simplified).

290

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GEOLOGICA CARPATHICA, 2012, 63, 4, 267—294; Electronic Table Edition I—VI

located  north  of  the  actual  front  of  the  Carpathian  nappes.
After  the  evaporite  deposition  the  central  part  of  the  Polish
Carpathian Foredeep Basin (PCFB) was uplifted and eroded
(“Rzeszów Island”). The “Rzeszów Island” can be regarded
as a kind of “fore-bulge” connected with the initial period of
the  “middle-Badenian  compression”  (the  late  Styrian  com-
pression,  see  Oszczypko  &  Oszczypko-Clowes  2011).  The
formation of the “Rzeszów Island” was followed by a north-
wards shift of the Carpathian nappes, and initiation of a new
phase of subsidence in the Polish Carpathian Foredeep Basin
and  the  beginning  of  deposition  of  the  Machów  Formation
(Oszczypko  1998,  1999,  2006).  During  this  time,  the  depth
of the sea oscillated around a depth characteristic of the up-
per  bathyal—neritic  zone  (Oszczypko  1999).  In  the  eastern
part  of  the  Carpathian  Foredeep  the  subsidence  axis  coin-
cides  approximately  with  the  current  front  of  the  Car-
pathians.  In  the  Late  Badenian,  in  the  region  of  Rzeszów,
the overall rate of subsidence was 1200—1300 m/Myr, while
the  rate  of  sedimentation  fluctuated  around  1000 m/Myr
(Oszczypko  1998,  1999).  The  Late  Badenian  (Kosovian)
transgression was related to the last, but very intense phase of
PCF subsidence that commenced around 13.65 Ma and ended
ca.  10.5 Ma  during  the  Sarmatian  s.l.  During  this  transgres-
sion, the outer and inner neritic conditions were established in
the inner and outer parts of the foredeep as well as in the mar-
ginal part of the Carpathians (Fig. 18) (see Oszczypko-Clowes
et  al.  2009;  Studencka  &  Jasionowski  2011;  Oszczypko  &
Oszczypko-Clowes 2011). The southern part of the foredeep
basin  was  supplied  with  detritic  material  derived  from  ero-
sion  of  Carpathians.  This  results  clearly  from  log  measure-
ments  of  the  paleotransport  directions  in  the  Stobierna 2,
Stobierna 3  and  Pogwizdów 2  boreholes  (Krzywiec  et  al.
2008). It is also confirmed by the presence of reworked nanno-
fossil  assemblages.  The  percentage  of  reworked  species  in
most samples from the Stobierna 2, Stobierna 3, Stobierna 4,
Stadnicka  Brzóza 1  and  Pogwizdów 2  boreholes  prevails
over  autochthonous  specimens  (Peryt  in  Peryt  et  al.  1998;
Garecka & Olszewska 2011). In the Stobierna 3 borehole the
supply from the south is already apparent in the lower deltaic
complex, whereas in the other three wells, only in the higher
deltaic complex. This supply direction remained in the Sarma-
tian. Only in the highest part of the profile – the last 600—800
meters, the southern direction of supply changes to south-east-
ern.  The  distribution  of  facies  suggests  multipoint  supply
through the fan-deltas (Oszczypko et al. 1987). Badenian sub-
sidence continuously passed into the Sarmatian, although the
change  of  direction  and  position  of  depocenters  was  signifi-
cant,  moving  from  the  vicinity  of  the  Carpathians  edge  into
the  Wielkie  Oczy  trench.  The  total  subsidence  is  here  from
1500 m in the NE part of the trench to 2500—3000 m in the SE
(Oszczypko  1998,  1999).  Development  and  architecture  of
the  Upper-Sarmatian  sediments  in  the  eastern  part  of  the
foredeep is probably derived from the interaction of tectonic
processes and shallowing-upward changes in sea level. Tec-
tonic  processes,  including  thrust  movements  of  the  Outer
Carpathians, probably largely determined the size of subsid-
ence in the basin and migration of depocenters, while chang-
es  in  sea  level  determined  the  depth  of  the  reservoir  and
shoreline shifts.

Conclusion

1. Deposition of the Machów Formation, in Sokołów area,

was related to the last, but very intense phase of subsidence
in the NE part of the Polish Carpathian Foredeep.

2. This subsidence commenced with the late Styrian com-

pression (latest Badenian) and ended during the Sarmatian s.l.

3. In the studied material reworked nannofossil assem-

blages prevail over autochthonous specimens. This suggests
importance of material supply, derived from eroded Outer
Carpathians.

4. The Carpathian supply of siliciclastic material is also

documented by the lower and upper deltaic complexes.

5. The obtained quantitative ratios of calcareous nanno-

plankton taxa show a general character of assemblages indi-
cating a shallow near-shore sedimentary environment.

6. The common occurrence of long-ranging taxa and taxa

resistant to carbonate dissolution may affect their real abun-
dance in assemblages, which makes paleoecological inter-
pretation problematic.

Acknowledgments:  The  authors  wish  to  thank  Katarína
Holcová  and  Stjepan  Ćorić  for  their  detailed  review  of  the
manuscript. The work was conducted owing to financial sup-
port  from  the  Jagiellonian  University  Grant  PSP  K/ZDS/
0001679 and research Project 03764/C.T12-6/200,  financed
jointly by the Polish Ministry of Research and Higher Edu-
cation and the Polish Oil and Gas Company, and coordinated
by  dr  hab,  ing.  Piotr  Krzywiec  from  the  Polish  Geological
Institute (Warsaw), to whom we extend our thanks. Special
thanks  should  be  given  to  dr  hab.  Anna  Wysocka  (Warsaw
University) for cooperation during the field work concerning
core material description as well as for very fruitfull discus-
sion concerning the subject, over all these years.

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Appendix

Nannofossil taxa mentioned in the text, in alphabetical order of genera

Braarudosphaera bigelowii (Gran & Braarud, 1935) Deflandre (1947)
Calcidiscus leptoporus (Murray & Blackman, 1898) Loeblich &

Tappan (1978)

Calcidiscus macintyrei (Bukry & Bramlette, 1969) Loeblich & Tappan

(1978)

Calcidiscus premacintyrei Theodoridis (1984)
Chiasmolithus bidens (Bramlette & Sullivan, 1961) Hay & Mohler

(1967)

Chiasmolithus grandis (Bramlette & Riedel, 1954) Radomski (1968)
Chiasmolithus modestus Perch-Nielsen (1971)
Chiasmolithus oamaruensis (Deflandre in Deflandre & Fert, 1954)

Hay, Mohler & Wade (1966)

Chiasmolithus solitus (Bramlette & Sullivan, 1961) Hay, Mohler &

Wade (1966)

Coccolithus miopelagicus Bukry (1971)
Coccolithus pelagicus (Wallich, 1877) Schiller (1930)
Coronocyclus nitescens (Kamptner, 1963) Bramlette & Wilcoxon

(1967)

Cyclicargolithus abisectus (Muller, 1970) Wise (1973)
Cyclicargolithus floridanus (Roth & Hay in Hay et al., 1967) Bukry

(1971)

Cyclicargolithus luminis (Sullivan, 1965) Bukry (1971)
Dictyococcites bisectus (Hay, Mohler & Wade, 1966) Bukry &

Percival (1971)

Discoaster barbadiensis Tan Sin Hok (1927)
Discoaster binodosus Martini (1958)
Discoaster challengeri Bramlette & Riedel (1954)
Discoaster deflandrei Bramlette & Riedel (1954)
Discoaster distinctus Martini (1958)
Discoaster druggi Bramlette & Wilcoxon (1967)
Discoaster exilis Martini & Bramlette (1963)
Discoaster lodoensis Bramlette & Riedel (1954)
Discoaster mediosus Bramlette & Sullivan (1961)
Discoaster multiradiatus Bramlette & Riedel (1954)
Discoaster saipanensis Bramlette & Riedel (1954)
Discoaster tanii Bramlette & Riedel (1954)
Discoaster tanii nodifer Bramlette & Riedel (1954)
Discoaster variabilis Martini & Bramlette (1963)
Ellipsolithus macellus (Bramlette & Sullivan, 1961) Sullivan (1964)
Ericsonia fenestrata (Deflandre & Fert, 1954) Stradner in Stradner

& Edwards (1968)

Ericsonia formosa (Kamptner, 1963) Haq (1971)
Ericsonia subdisticha (Roth & Hay in Hay et al., 1967) Roth in

Baumann & Roth (1969)

Helicosphaera ampliaperta Bramlette & Wilcoxon (1967)
Helicosphaera bramlettei (Müller, 1970) Jafar & Martini (1975)
Helicosphaera carteri (Wallich, 1877) Kamptner (1954)
Helicosphaera compacta Bramlette & Wilcoxon (1967)
Helicosphaera euphratis Haq (1966)
Helicosphaera gartneri Theodoridis (1984)
Helicosphaera intermedia Martini (1965)
Helicosphaera lophota (Bramlette & Sullivan, 1961) Locker (1973)
Helicosphaera mediterranea Müller (1981)
Helicosphaera perch-nilseniae Haq (1971)
Helicosphaera recta (Haq, 1966) Jafar & Martini (1975)

Helicosphaera scissura Müller (1981)
Helicosphaera stalis Theodoridis (1984)
Helicosphaera walbersdorfensis Müller (1974)
Helicosphaera waltrans Theodoridis (1984)
Heliolithus kleinpelli Sullivan (1964)
Holodiscolithus macroporus (Deflandre in Deflandre & Fert, 1954)

Roth (1970)

Isthmolithus recurvus Deflandre in Deflandre & Fert (1954)
Lanternithus minutus Stradner (1962)
Neococcolithes dubius (Deflandre in Deflandre & Fert, 1954) Black

(1967)

Pontosphaera discopora Schiller (1925)
Pontosphaera enormis (Locker, 1967) Perch-Nielsen (1984)
Pontosphaera latelliptica (Báldi-Beke & Baldi, 1974) Perch-Nielsen

(1984)

Pontosphaera multipora (Kamptner ex Deflandre, 1959) Roth (1970)
Pontosphaera plana (Bramlette & Sullivan, 1961) Haq (1971)
Pontosphaera rothi Haq (1971)
Reticulofenestra daviessi (Haq, 1971) Haq (1971)
Reticulofenestra dictyoda (Deflandré in Deflandré & Fert, 1954)

Stradner in Stradner & Edwards (1968)

Reticulofenestra hillae Bukry & Percival (1971)
Reticulofenestra lockerii Müller (1970)
Reticulofenestra ornata Müller (1970)
Reticulofenestra pseudoumbilica (Gartner, 1967) Gartner (1969)
Reticulofenestra reticulata (Hay, Mohler & Wade, 1966) Roth

(1970)

Reticulofenestra umbilica (Levin, 1965) Martini & Ritzkowski

(1968)

Rhabdosphaera clavigera Murray & Blackman (1898)
Semihololithus kerabyi Perch-Nielsen (1971)
Sphenolithus abies Deflandre in Deflandre & Fert (1954)
Sphenolithus belemnos Bramlette & Wilcoxon (1967)
Sphenolithus capricornutus Bukry & Percival (1971)
Sphenolithus conicus Bukry (1971)
Sphenolithus dissimilis Bukry & Percival (1971)
Sphenolithus editus Perch-Nielsen in Perch-Nielsen et al. (1978)
Sphenolithus heteromorphus Deflandre (1953)
Sphenolithus moriformis (Brönnimann & Stradner, 1960) Bramlette

& Wilcoxon (1967)

Sphenolithus radians Deflandre in Grassé (1952)
Sphenolithus spiniger Bukry (1971)
Toweius rotundus Perch-Nielsen in Perch-Nielsen et al. (1978)
Transversopontis fibula Getha (1976)
Transversopontis obliquipons (Deflandre in Deflandre & Fert,

1954) Hay, Mohler & Wade (1966)

Transversopontis pulcher (Deflandre in Deflandre & Fert, 1954)

Perch-Nielsen (1967)

Transversopontis pulcheroides (Sullivan, 1964) Báldi-Beke (1971)
Transversopontis pygmaea Locker (1967)
Tribrachiatus orthostylus Shamrai (1963)
Triquetrorhabdulus rugosus Bramlette & Wilcoxon (1967)
Umbilicosphaera rotula (Kamptner, 1956) Varol (1982)
Zygrhablithus bijugatus (Deflandre in Deflandre & Fert, 1954)

Deflandre (1959)

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GEOLOGICA CARPATHICA, 2012, 63, 4, 267—294; Electronic Table Edition I—VI

Table 3: Nominal and percentage distribution of calcareous nannofossils in the Stobierna 2 borehole. x – species too rare to be included in count.

Stobierna 2

1190–1208 XVI

1190–1208 I

1208–1222 X

1320–1338 IV

1320–1338 XIII

Autochthonous species

Braarudosphaera bigelowii

0.67

3.10

0.68

0.58

0.63

Calcidiscus leptoporus

Calcidiscus macintyrei

0.67

0.63

Calcidiscus premacintyrei

0.68

0.58

1.25

Coccolithus miopelagicus

2.67

1.55

2.70

1.16

3.13

Coccolithus pelagicus

22.00

17.05

17.57

26.01

18.13

Coronocyclus nitescens

0.67

2.33

2.70

1.73

1.25

Cyclicargolithus floridanus

24.00

23.26

20.95

31.79

18.75

Discoaster deflandrei

0.68

0.58

1.25

Discoaster exilis

0.67

Discoaster variabilis

Helicosphaera carteri

14.67

7.43

1.16

11.88

Helicosphaera intermedia

0.78

0.68

0.58

0.63

Helicosphaera stalis

0.67

2.70

0.58

0.63

Helicosphaera walbersdorfensis

2.67

4.65

0.68

1.73

3.75

Pontosphaera discopora

2.67

0.78

2.03

0.58

1.25

Pontosphaera multipora

2.67

6.20

3.38

1.88

Reticulofenestra pseudoumbilica

6.00

6.20

15.54

15.03

13.13

Reticulofenestra spp. small

8.67

20.93

6.76

6.94

13.13

Sphenolithus abies

1.33

2.33

4.73

4.62

0.63

Sphenolithus moriformis

8.00

7.75

8.78

5.78

6.25

Umbilicosphaera rotula

1.33

3.10

1.35

0.58

1.88

Allochthonous species
Chiasmolithus bidens

Chiasmolithus grandis

Chiasmolithus modestus

Chiasmolithus oamaruensis

Chiasmolithus solitus

Cyclicargolithus abisectus

Cyclicargolithus luminis

Dictyococcites bisectus

Discoaster barbadiensis

Discoaster binodosus

Discoaster druggi

Discoaster lodoensis

Discoaster multiradiatus

Discoaster tanii

Discoaster tanii nodifer

Ericsonia fenestrata

Ericsonia formosa

Helicosphaera bramlettei

Helicosphaera compacta

Helicosphaera euphratis

Helicosphaera gartneri

Helicosphaera mediterranea

Helicosphaera recta

Helicosphaera scissura

Heliolithus kleinpelli

Isthmolithus recurvus

Lanternithus minutus

Neococcolithes dubius

Pontosphaera enormis

Pontosphaera latelliptica

Pontosphaera plana

Pontosphaera rothi

Reticulofenestra daviessi

Reticulofenestra dictyoda

Reticulofenestra hillae

Reticulofenestra lockerii

Reticulofenestra ornata

Reticulofenestra reticulata

Reticulofenestra umbilica

Sphenolithus conicus

Sphenolithus dissilimis

Sphenolithus editus

Sphenolithus heteromorphus

Sphenolithus radians

Transversopontis obliquipons

Transversopontis pulcher

Transversopontis pulcheroides

Transversopontis pygmaea

Tribrachiatus orthostylus

Zygrhablithus bijugatus

Cretaceous species undivided

SUM

300

Electronic Edition of Tables 3-7 – OSZCZYPKO-CLOWES et al.: SARMATIAN PALEOECOLOGICAL ENVIRONMENT

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2012, 63, 4, 267—294; Electronic Table Edition I—VI

Table 4: Nominal and percentage distribution of calcareous nannofossils in the Stobierna 3 borehole. x – species too rare to be included in count.

Stobierna 3

715–

724 I

715–

724 II

715–

724 VIII

715–

724 IX

834–

843 IV

834–

843 VIII

1113–

1122 II

1290–

1295 II

1660–

1669 II

1660-

1669 VI

Autochthonous species

Braarudosphaera bigelowii

3 2.19

2 1.34

1 0.74

1 0.85

Calcidiscus leptoporus

7 5.11

9 6.04

7 5.15

1 0.85

1 0.75

1 0.84

5 2.98

Calcidiscus premacintyrei

1 0.32

1 0.36

1 0.33

Coccolithus miopelagicus >10 m

10 7.30

8 5.37

6 4.41

5 4.27

9 7.63

4 2.99

Coccolithus miopelagicus

4 2.92

3 2.21

8 6.78

6 1.90

5 1.78

2 0.67

Coccolithus pelagicus

10 7.30

14 9.40

13 9.56

16 13.68 14 11.86

18 13.43

13 9.35 32 20.92 30 25.21

53 31.55

Coronocyclus nitescens

10 3.17 19 6.76

2 0.66

2 0.67

Cyclicargolithus floridanus

13 9.49

10 6.71

23 16.91

21 17.95 15 12.71

22 16.42

18 12.95 33 21.57 28 23.53

50 29.76

Discoaster deflandrei

1 0.85

3 2.24

2 1.44

Discoaster variabilis

2 1.69

1 0.75

Helicosphaera carteri

12 8.76

18 12.08

13 9.56

17 14.53

6 5.08

7 5.22

11 7.91

8 5.23

7 5.88

2 1.19

Helicosphaera intermedia

3 2.19

2 1.34

2 1.47

2 1.71

6 4.48

2 1.44

1 0.65

5 4.20

1 0.60

Helicosphaera walbersdorfensis

5 3.65

5 3.36

2 1.47

1 0.85

5 3.60

2 1.31

1 0.84

7 4.17

Pontosphaera discopora

2 1.46

4 2.68

1 0.74

2 1.71

3 2.54

1 0.75

5 3.60

3 1.96

3 2.52

3 1.79

Pontosphaera multipora

14 10.22

11 7.38

12 8.82

5 4.27

6 5.08

16 11.94

15 10.79

3 1.96

9 7.56

4 2.38

Reticulofenestra pseudoumbilica

3 2.19

3 2.01

1 0.74

3 2.56

9 7.63

8 5.97

12 8.63 10 6.54

7 4.17

Reticulofenestra spp. small

14 10.22

14 9.40

5 3.68

10 8.55

9 7.63

9 6.72

11 7.91 10 6.54

8 6.72

9 5.36

Sphenolithus abies

13 9.49

14 9.40

16 11.76

10 8.55 10 8.47

8 5.97

8 5.76

3 1.96

3 2.52

3 1.79

Sphenolithus moriformis

17 12.41

24 16.11

22 16.18

17 14.53 21 17.80

23 17.16

16 11.51 10 6.54 19 15.97

10 5.95

Umbilicosphaera rotula

7 5.11

11 7.38

9 6.62

6 5.13

4 3.39

7 5.22

4 2.88 13 8.50

3 2.52

9 5.36

Allochthonous species
Calcidiscus premacintyrei

Chiasmolithus bidens

Chiasmolithus modestus

Chiasmolithus oamaruensis

Chiasmolithus solitus

Coronocyclus nitescens

Cyclicargolithus abisectus

Cyclicargolithus luminis

Dictyococcites bisectus

Discoaster barbadiensis

Discoaster binodosus

Discoaster lodoensis

Discoaster multiradiatus

Discoaster saipanensis

Discoaster sp.

Discoaster tanii

Discoaster tanii nodifer

Ericsonia fenestrata

Ericsonia formosa

Ericsonia subdisticha

Helicosphaera bramletei

Helicosphaera euphratis

Helicosphaera gartneri

Helicosphaera mediterranea

Helicosphaera recta

Helicosphaera scissura

Helicosphaera sp.

Helicosphaera waltrans

Isthmolithus recurvus

Lanternithus minutus

Neococcolithes dubius

Pontosphaera latelliptica

Pontosphaera plana

Pontosphaera rothi

Reticulofenestra dictyoda

Reticulofenestra hillae

Reticulofenestra lockerii

Reticulofenestra ornata

Reticulofenestra reticulata

Reticulofenestra umbilica

Sphenolithus belemnos

Sphenolithus conicus

Sphenolithus dissilimis

Sphenolithus heteromorphus

Sphenolithus radians

Toweius rotundus

Transversopontis obliquipons

Transversopontis pulcher

Transversopontis pulcheroides

Zygrhablithus bijugatus

Cretaceous species undivided

SUM

300

267

289

284

III

Electronic Edition of Tables 3-7 – OSZCZYPKO-CLOWES et al.: SARMATIAN PALEOECOLOGICAL ENVIRONMENT

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2012, 63, 4, 267—294; Electronic Table Edition I—VI

Table 5: Nominal and percentage distribution of calcareous nannofossils in the Stobierna 4 borehole. x – species too rare to be included in count.

Stobierna 4

1016–

1021 II

1116–

1125 I

1116–

1125 IV

1116–

1125 IX

1229–

1238 V

1229–

1238 VII

1229–

1238 VIII

Autochthonous species
Braarudosphaera bigelowii

2.19

2.61

1.44

0.78

3.61

1.83

Calcidiscus leptoporus

2.19

1.96

1.61

0.72

0.78

1.20

0.61

Calcidiscus premacintyrei

4.58

3.60

0.60

3.05

Coccolithus miopelagicus

5.84

0.65

4.32

2.34

3.01

3.66

Coccolithus pelagicus

10.22

9.80

24.19

9.35

10.16

11.45

10.98

Coronocyclus nitescens

4.38

3.92

3.23

6.47

8.59

7.83

8.54

Cyclicargolithus floridanus

6.57

7.19

34.68

10.79

12.50

10.84

11.59

Discoaster deflandrei

2.92

0.65

0.72

1.56

0.61

Helicosphaera carteri

10.22

15.03

6.45

7.91

20.31

13.25

9.15

Helicosphaera intermedia

5.11

3.92

0.81

0.72

0.78

0.60

1.22

Helicosphaera walbersdorfensis

2.92

0.65

2.42

2.16

3.13

1.81

1.22

Pontosphaera discopora

9.49

5.88

2.42

2.88

3.61

3.66

Pontosphaera multipora

3.65

6.54

1.61

6.47

6.25

1.81

4.27

Reticulofenestra pseudoumbilica

2.92

0.81

7.91

2.34

8.43

1.22

Reticulofenestra spp. small

9.49

10.46

7.26

7.91

6.25

4.22

7.32

Rhabdosphaera clavigera

2.19

0.65

Sphenolithus abies

6.57

2.61

3.23

3.60

3.13

4.22

3.05

Sphenolithus moriformis

8.03

15.69

9.68

15.83

11.72

17.47

20.73

Umbilicosphaera rotula

5.11

7.19

1.61

7.19

9.38

6.02

7.32

Allochthonous species
Chiasmolithus bidens

Chiasmolithus modestus

Chiasmolithus oamaruensis

Chiasmolithus solitus

Cyclicargolithus abisectus

Cyclicargolithus luminis

Dictyococcites bisectus

Discoaster barbadiensis

Discoaster binodosus

Discoaster lodoensis

Discoaster multiradiatus

Discoaster saipanensis

Discoaster sp.

Discoaster tanii

Discoaster tanii nodifer

Ericsonia fenestrata

Ericsonia formosa

Ericsonia subdisticha

Helicosphaera bramlettei

Helicosphaera euphratis

Helicosphaera gartneri

Helicosphaera mediterranea

Helicosphaera perch-nilseniae

Helicosphaera recta

Helicosphaera scissura

Helicosphaera sp.

Helicosphaera waltrans

Isthmolithus recurvus

Lanternithus minutus

Neococcolithes dubius

Pontosphaera latelliptica

Pontosphaera plana

Pontosphaera rothi

Reticulofenestra dictyoda

Reticulofenestra hillae

Reticulofenestra lockerii

Reticulofenestra ornata

Reticulofenestra reticulata

Reticulofenestra umbilica

Sphenolithus dissimilis

Sphenolithus heteromorphus

Sphenolithus radians

Toweius rotundus

Transversopontis obliquipons

Transversopontis pulcher

Transversopontis pulcheroides

Tribrachiatus orthostylus

Zygrhablithus bijugatus

Cretaceous species undivided

SUM

300

246

300

287

300

Electronic Edition of Tables 3-7 – OSZCZYPKO-CLOWES et al.: SARMATIAN PALEOECOLOGICAL ENVIRONMENT

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2012, 63, 4, 267—294; Electronic Table Edition I—VI

Table 6: Nominal and percentage distribution of calcareous nannofossils in the Pogwizdów 2 borehole. x – species too rare to be included
in count.

Pogwizdów 2

1161–

1170 I

1161–

1170 VIII

1381–

1390 II

1381–

1390 IX

Autochthonous species
Braarudosphaera bigelowii

2 1.64

Calcidiscus leptoporus

1 0.82

Calcidiscus macintyrei

Calcidiscus premacintyrei

1 14

Coccolithus miopelagicus

2 1 3 2

Coccolithus pelagicus

30 24.59 33 26 40 25 56 30

Coronocyclus nitescens

12 9.84

6 5 13

8 19 10

Cyclicargolithus floridanus

28 22.95 31 24 38 23 57 31

Discoaster challengeri

Discoaster deflandrei

1 0.82

1 0.32

Discoaster variabilis

Helicosphaera carteri

5 4.10

7 5 5 3 1 1

Helicosphaera intermedia

1 0.82

Helicosphaera stalis

1 0.82

1 1 x

1 1

Helicosphaera walbersdorfensis

2 1.64

2 2 4 2 6 3

Holodiscolithus macroporus

Pontosphaera discopora

4 3.28

1 1 1 1 1 1

Pontosphaera multipora

2 1.64 14 11 6 4 1 1

Reticulofenestra pseudoumbilica

3 2.46

2 2 32 20 1 1

Reticulofenestra spp. small

10 8.20 13 10 10 6 12 6

Rhabdosphaera clavigera

1 0.82

Sphenolithus abies

1 0.82

2 2 1 1 4 2

Sphenolithus moriformis

15 12.30 11 9 6 4 8 4

Triquetrorhabdulus rugosus

Umbilicosphaera rotula

3 2.46

1 1 2 1 1 1

Allochthonous species
Chiasmolithus bidens

Chiasmolithus grandis

Chiasmolithus modestus

Chiasmolithus oamaruensis

Chiasmolithus solitus

Cyclicargolithus abisectus

Cyclicargolithus luminis

Dictyococcites bisectus

Discoaster barbadiensis

Discoaster binodosus

Discoaster distinctus

Discoaster druggi

Discoaster lodoensis

Discoaster mediosus

Discoaster multiradiatus

Discoaster saipanensis

Discoaster tanii

Discoaster tanii nodifer

Ellipsolithus macellus

Ericsonia fenestrata

Ericsonia formosa

Helicosphaera ampliaperta

Helicosphaera bramlettei

Helicosphaera compacta

Helicosphaera euphratis

Helicosphaera gartneri

Helicosphaera lophota

Helicosphaera mediterranea

Helicosphaera recta

Helicosphaera scissura

Isthmolithus recurvus

Lanternithus minutus

Neococcolithes dubius

Pontosphaera enormis

Pontosphaera latelliptica

Pontosphaera plana

Pontosphaera rothi

Reticulofenestra daviessi

Reticulofenestra dictyoda

Reticulofenestra lockerii

Reticulofenestra ornata

Reticulofenestra reticulata

Reticulofenestra umbilica

Pogwizdów 2

1161–

1170 I

1161–

1170 VIII

1381–

1390 II

1381–

1390 IX

Allochthonous species
Semihololithus kerabyi

Sphenolithus capricornutus

Sphenolithus conicus

Sphenolithus dissilimis

Sphenolithus editus

Sphenolithus heteromorphus

Sphenolithus radians

Sphenolithus spiniger

Toweius sp.

Transversopontis fibula

Transversopontis obliquipons

Transversopontis pulcher

Transversopontis pulcheroides

Transversopontis pygmaea

Tribrachiatus orthostylus

Zygrhablithus bijugatus

Cretaceous spieces undivided

SUM

300

Electronic Edition of Tables 3-7 – OSZCZYPKO-CLOWES et al.: SARMATIAN PALEOECOLOGICAL ENVIRONMENT

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2012, 63, 4, 267—294; Electronic Table Edition I—VI

Table 7: Nominal and percentage distribution of calcareous nannofossils in the Stadnicka Brzóza 1 borehole. x – species too rare to be in-
cluded in count. Continued on the next page.

Stadnicka Brzóza 1

350–356 I

1043–1047 II 1175–1179 III 1327–1331

II 1586–1590 1586–1590

1663–1667 III

Autochthonous species
Braarudosphaera bigelowii

0.83

0.79

0.80

0.72

0.83

Calcidiscus leptoporus

Calcidiscus macintyrei

Calcidiscus premacintyrei

0.80

Coccolithus miopelagicus

9.45

6.40

5.07

3.31

1.40

1.74

Coccolithus miopelagicus >10 m

3.31

Coccolithus pelagicus

27.27

22.05

32.80

27.54

23.97

32.87

21.74

Coronocyclus nitescens

2.36

3.20

0.72

7.44

3.50

2.61

Cyclicargolithus floridanus

25.62

19.69

28.00

26.09

20.66

30.77

19.13

Discoaster challengeri

Discoaster deflandrei

4.13

2.36

Discoaster exilis

0.79

Discoaster variabilis

0.83

Helicosphaera carteri

6.61

6.30

5.07

6.61

4.90

12.17

Helicosphaera intermedia

2.36

0.83

0.87

Helicosphaera stalis

0.83

1.57

5.22

Helicosphaera walbersdorfensis

1.65

2.36

1.60

5.80

3.31

5.59

2.61

Holodiscolithus macroporus

Pontosphaera discopora

4.13

0.79

2.90

3.31

0.70

1.74

Pontosphaera multipora

4.13

8.66

4.00

1.45

4.96

1.40

10.43

Reticulofenestra pseudoumbilica

1.65

1.57

2.40

11.59

9.92

6.29

9.57

Reticulofenestra spp. small

7.44

7.09

5.60

4.35

1.65

4.90

8.70

Rhabdosphaera clavigera

0.00

1.57

0.70

Sphenolithus abies

3.31

0.79

2.40

1.45

2.48

3.50

0.87

Sphenolithus moriformis

6.61

7.87

8.80

5.80

8.26

2.80

Triquetrorhabdulus rugosus

Umbilicosphaera rotula

1.65

1.57

3.20

1.45

2.48

0.70

2.61

Allochthonous species
Calcidiscus macintyrei

Calcidiscus premacintyrei

Chiasmolithus bidens

Chiasmolithus grandis

Chiasmolithus modestus

Chiasmolithus oamaruensis

Chiasmolithus solitus

Coronocyclus nitescens

Cyclicargolithus abisectus

Cyclicargolithus luminis

Dictyococcites bisectus

Discoaster barbadiensis

Discoaster binodosus

Discoaster druggi

Discoaster lodoensis

Discoaster multiradiatus

Discoaster saipanensis

Discoaster tanii

Ericsonia fenestrata

Ericsonia formosa

Helicosphaera bramlettei

Helicosphaera compacta

Helicosphaera euphratis

Helicosphaera gartneri

Helicosphaera mediterranea

Helicosphaera recta

Heliolithus kleinpelli

Isthmolithus recurvus

Lanternithus minutus

Neococcolithes dubius

Pontosphaera enormis

Pontosphaera latelliptica

Pontosphaera plana

Pontosphaera rothi

Reticulofenestra daviessi

Reticulofenestra dictyoda

Reticulofenestra hillae

Reticulofenestra lockerii

Reticulofenestra minuta

Reticulofenestra ornata

Reticulofenestra reticulata

Reticulofenestra umbilica

Electronic Edition of Tables 3-7 – OSZCZYPKO-CLOWES et al.: SARMATIAN PALEOECOLOGICAL ENVIRONMENT

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2012, 63, 4, 267—294; Electronic Table Edition I—VI

Table 7: Continued.

Stadnicka Brzóza 1

350–356 I

1043–1047 II 1175–1179 III

1327–1331 II

1586–1590

1586–1590 I

1663–1667 III

Allochthonous species
Semihololithus kerabyi

Sphenolithus conicus

Sphenolithus dissilimis

Sphenolithus editus

Sphenolithus heteromorphus

Sphenolithus radians

Toweius sp.

Transversopontis fibula

Transversopontis obliquipons

Transversopontis pulcher

Transversopontis pulcheroides

Transversopontis pygmaea

Tribrachiatus orthostylus

Zygrhablithus bijugatus

Cretaceous species undivided

SUM

300