GeolCarp_Vol63_No2_121

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA

, APRIL 2012, 63, 2, 121—137 doi: 10.2478/v10096-012-0010-x

The oxygen and carbon isotopic composition of Langhian

foraminiferal tests as a paleoecological proxy in a marginal

part of the Carpathian Foredeep (Czech Republic)

KATARÍNA HOLCOVÁ

and ATTILA DEMENY

Institute of Geology and Paleontology, Charles University in Prague, Albertov 6, 128 43 Praha 2, Czech Republic; holcova@natur.cuni.cz

Institute for Geochemical Research, Hungarian Academy of Sciences Budapest, Budaorsi ut 45, H-1112 Budapest, Hungary;

demeny@geochem.hu

(Manuscript received January 26, 2011; accepted in revised form September 30, 2011)

Abstract: Foraminiferal assemblages from three locations of the Moravian part of the Carpathian Foredeep (Kralice,
Přemyslovice, Židlochovice) have been studied in order to determine the paleoenvironmental conditions during the
Early Badenian (Middle Miocene). Paleobiological characteristics (plankton/benthos-ratio, relative abundances of warm-
water plankton species, five-chambered Globoturborotalita spp., Coccolithus pelagicus and high nutrient markers
[benthos], test sizes and ranges of Globigerina sp. and cibicidoids, Benthic Foraminiferal Oxygen Index) were deter-
mined along with stable C and O isotope compositions. The stable isotope compositions show large variabilities indicat-
ing sample inhomogeneity in well preserved foraminiferal samples, interpreted as a sign of primary environmental
variation and postmortem mixing of tests of different populations and sources. Based on the combined interpretation of
paleobiological indicators and isotopic compositions, two theoretical models were established to describe the observed
paleobiological and stable isotope data, that were used to categorize the locations studied. Several types of near-shore
paleoenvironment were distinguished using the theoretical models: (i) bay influenced by seasonal phytodetritus supply
from the continent (Kralice); (ii) dynamic shore characterized by variable isotopic compositions probably due to mixing
of indigenous, transported and reworked tests (Přemyslovice); (iii) shore of alternating normal marine and continentally
influenced environments (Židlochovice).

Key words: Middle Miocene, Badenian, Carpathian Foredeep, paleoecology, foraminifera, calcareous nannoplankton,
oxygen and carbon stable isotopes.

Introduction

Oxygen  and  carbon  isotopic  compositions  of  the  foramini-
feral tests represent routine geochemical proxies for paleoen-
vironmental  conditions  in  the  oceanic  realm.  In  the  epeiric
seas,  the  application  of  the  method  is  more  problematic.
Variable  paleoenvironments  with  oscillations  of  evapora-
tion/influx-ratio,  variable  input  of  organic  matter  from  the
continent  and  communication/isolation  events  influenced
the  isotopic  composition  of  sea  water  and  make  interpreta-
tion of these proxies difficult.

The study area, the Central Paratethys, represents a chain

of Oligocene and Miocene epeiric seas with marked oscilla-
tion of paleoecological parameters and episodic communica-
tion with the oceanic realm (Rögl 1998, 1999).

The study interval can be well biostratigraphically dated

and  represents  a  lower  part  of  the  local  Central  Paratethys
Badenian stage which is correlated with the Langhian (Rögl
et  al.  2008;  Hohenegger  et  al.  2009).  The  paleogeographic
and paleoclimatic situation which could have influenced the
isotopic  composition  of  the  Central  Paratethys  sea  water  is
well known. The period was characterized by a large marine
transgression affecting the entire circum-Mediterranean area.
The transgression was connected with brief reopening of the
Mediterranean—Indo-Pacific  seaway  and  invasion  of  the
tropical—subtropical water masses into the Central Paratethys

basins (Rögl & Steininger 1983; Rögl 1998, 1999; Popov et
al.  2004;  Kováč  et  al.  2007;  Piller  et  al.  2007).  The  Early
Badenian climate of the Central Paratethys realm can be as-
sumed  as  fairly  uniform  and  corresponds  with  the  Miocene
Climatic  Optimum  (Böhme  2003;  Slamková  &  Doláková
2004).  The  Mean  Annual  Temperature  (MAT)  of  the  Early
Badenian has been estimated at 13 to almost 20 °C on the ba-
sis  of  percentage  of  evergreen  taxa  with  a  seasonal  tempera-
ture  change  of  less  than  25 °C  and  with  the  temperature  of
the coldest month varying between 4 and 10 °C  (Kvaček  et
al.  2006),  although  a  minimum  Sea  Surface  Temperature
(SST) has been estimated at 16—18 °C based on stenothermic
gastropods (Harzhauser et al. 2002).

Most of the oxygen and carbon isotopic data from the Central

Paratethys  originated  from  this  interval  (Foraminifera:
Gonera et al. 2000; Bicchi et al. 2003; Báldi 2006; Báldi &
Hohenegger  2008.  Molluscs:  Latal  et  al.  2004,  2006;
Harzhauser et al. 2007. Bryozoa and bulk sediments: Hladí-
ková  &  Hamršmíd  1986;  Nehyba  et  al.  2008).  Comparison
of  paleotemperatures  estimated  for  the  terrestrial  biotopes
(Kvaček et al. 2006) with calculations of paleotemperatures
from the isotopic data suggest an

O-enriched seawater sys-

tem (due to evaporation), different from estimation for the
oceanic realm (—1 ‰; Lear et al. 2000). Latal et al. (2006)
and Nehyba et al. (2008) estimated the average

O value of

the Central Paratethys sea water at approximately + 1 ‰.

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GEOLOGICA CARPATHICA, 2012, 63, 2, 121—137

In this study, isotopic analysis was focused on the assem-

blages  from  the  marginal  shallow-water  parts  of  the
Carpathian Foredeep. The aim of the work is to analyse the
causes  of  observed  within-sample  variabilities  and  discuss
the  potential  of  the  isotopic  proxy  for  paleoenvironmental
interpretation in the marginal parts of epeiric seas.

Materials

The studied materials originated from three shallow bore-

holes  from  the  Carpathian  Foredeep:  Přemyslovice  (PY1,
PY3)  (Zágoršek  &  Holcová  2009),  Židlochovice  (ZIDL2)
and section Kralice (KRAS; Zágoršek et al. 2009). Samples
KRAS 1, 3, 4, 6, 7, 8, 11, 12;  PY1/40,  PY1/220,  PY3/230,
PY3/150;  ZIDL2/8.5m,  ZIDL2/12.2m  and  ZIDL2/16.9m
were analysed for isotopic composition of foraminiferal tests
(Fig. 1). The assemblages can be correlated with calcareous
nannoplankton  Zone  NN5  according  to  occurrence  of
Sphenolithus  heteromorphus  and  absence  of  Helicosphaera
ampliaperta (Martini  1971).  The  study  interval  can  be  well
dated using two planktonic foraminiferal events: the first oc-
currence  (FO)  of  Orbulina  suturalis  (Figs. 2,  3.1,2)  and  the
last occurrence (LO) of Praeorbulina (Figs. 2, 3.3) (Berggren
et  al.  1995;  Lourens  et  al.  2004;  Rupp  &  Hohenegger  2008;
Hohenegger  et  al.  2009).  These  biostratigraphical  events
characterize the Langhian (Gradstein et al. 2004) which can be
correlated with the lower part of the local Central Paratethys
Badenian stage (Hohenegger et al. 2009). Figure 1 shows tran-
sitional rock types including marls and sandstones (Fig. 1).

Methods

The carbon and oxygen isotope compositions of calcite

were  determined  at  the  Institute  for  Geochemical  Research
of the Hungarian Academy of Sciences (Budapest, Hungary)
following  the  method  of  acid  digestion  of  the  carbonatite
samples  (for  analytical  details  see  Spötl  &  Vennemann
2003). The isotope analyses were conducted using automat-
ed  GASBENCH  equipment  attached  to  a  Finnigan  Thermo
delta  plus  XP  mass  spectrometer.  The  compositions  are  ex-
pressed as

C and

O values relative to V-PDB, accord-

ing to the equation:

= (R

sample

/ R

standard

—1) 1000

where R is the

C or

O ratio in the sample or in

the international standard V-PDB. The analytical precision
was better than 0.15 ‰ based on multiple analyses of stan-
dards, but the standard deviation is much higher for most of
the samples (discussed below).

During a first run of analyses only two tests were analysed

from each sample that yielded a high within-sample variabil-
ity. In order to investigate this variability in detail, recrystal-
lization  of  inner  test  walls  was  re-evaluated  for  10—15
specimens  from  every  sample  (Fig. 4).  Assemblages  with
abraded and corroded tests were excluded from the isotopic
analysis,  thus,  during  a  taphonomic  analysis  only  size  sort-
ing of tests separately for benthic and planktonic assemblages
were  used  as  a  criterion  of  postmortem  test  transport.  The
greatest diameter of tests from every sample were measured
using a VIA video measuring system and data were summa-
rized in histograms. The first hundred specimens of Globige-
rina  spp.  and  the  first  hundred  specimens  of  Cibicidoides
spp. from fraction 0.063 to 2 mm were measured. As trans-
ported  tests  should  be  well-sorted,  accumulation  of  small,

Fig. 2. Biostratigraphical correlation of studied interval.

The foraminifera were separated from

washed  residues  (fraction  0.063  to
2 mm).  The  residues  were  dried  at  room
temperature.  Cooking,  freezing  or  any
chemical processes were omitted from the
disintegration  of  rock  samples.  The
washed residues were rinsed with hydro-
gen  peroxide.  Empty  tests  were  hand-
picked  from  floating  ones  for  isotopic
analyses and were cleaned in an ultrason-
ic  bath  of  distilled  water.  Foraminiferal
tests were checked for recrystallization on
the inner test walls using scanning electron
microscope  (SEM)  type  JSM  6380  LV
(Fig. 4). Groups of small-sized four-cham-
bered  Globigerina  sp.  (Fig. 3.6,7)  and
Cibicidoides spp. (Fig. 3.15,16) were cho-
sen  for  isotopic  analysis.  Planktonic  fora-
minifera for isotopic analysis were picked
from the size fraction 63—200 µm in which
no specimens with reproductive chambers
were  observed.  The  size  ranges  of  analy-
sed  tests  in  individual  samples  are  speci-
fied  in  Table 1.  Benthonic  foraminifera
were picked from the 63—300 µm fraction.

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GEOLOGICA CARPATHICA, 2012, 63, 2, 121—137

usually thin-walled tests (rounded forms  < 200  m) indicates
suspended-load  transport;  accumulation  of  large,  thick-
walled tests ( > 300  m) and missing of smaller tests charac-
terize  tests  which  were  transported  as  bed  load  (Murray
1965; Wang & Murray 1983; Holcová 1996).

Paleobiological proxies

Isotopic data were compared with foraminiferal and cal-

careous nannoplankton paleoebiological proxies. In all stud-
ied samples, foraminiferal and calcareous nannoplankton
assemblages were quantitatively evaluated from 200—500
specimens (for detailed methods see Zágoršek et al. 2009).

The upper part of the water column was characterized using

the following proxies:

(1) Relative abundances of warm-water taxa of planktonic

foraminifera  according  to  the  classifications  of  Spezzaferri
(1995), Bicchi et al. (2003) and Rupp & Hohenegger (2008).
Among  warm-water  taxa  were  classified  orbulinids,
Globigerinoides  spp.  and  Globigerinella  spp.,  cold-tempe-
rate indicators are Globorotalia spp. while Globigerina spp.
and Turborotalita spp. indicate cold water.

(2) The ratio between five- and four-chambered small

Globigerina and Globoturborotalita. Generally, in the normal
oceanic realm small Globigerina are considered to be an indi-
cator of the presence of nutrient-rich, cold water, whereas in
the marginal part of the basin they may indicate deterioration
of paleoenvironmental conditions, such as oscillation of salin-
ity. The alternation of horizons dominated by four-chambered
Globigerina or five-chambered Globoturborotalita is char-
acteristic for the early Middle Miocene of the Central Para-
tethys (Rupp & Hohenegger 2008; Zágoršek et al. 2009).
Hohenegger et al. (2008) consider “five-chambered globiger-
inids” to be indicators of cold, non-stratified water masses.

(3) Size distribution of tests of Globigerina spp. Histo-

grams of the test diameter of approximately one hundred
specimens of Globigerina spp. from every sample were con-
structed and used for estimation of postmortem transport.

(4) Relative abundances of the most common calcareous

nannoplankton species: Coccolithus pelagicus and Reticulo-
fenestra minuta. The presence of Coccolithus pelagicus is a
traditional  indicator  of  cold  and  nutrient-rich  water  (Okada
&  McInyre  1979;  Winter  et  al.  1994),  but  this  is  weakened
by  the  common  occurrence  of  the  species  in  waters  up  to
18 °C in which it can be used as a tracer of the periphery of
areas of enhanced productivity (Cachao & Moita 2000). The
species  also  may  dominate  secondarily  in  assemblages  due
to its higher resistance to dissolution (Roth & Berger 1975;
Roth 1994; Flores et al. 2003).

The most common species Reticulofenestra minuta is

generally opportunistic; its blooms are connected with envi-
ronmental stress characterized by quick changes within envi-
ronmental  conditions  (Wade  &  Brown  2006)  and  its  high
abundance distinguishes assemblages from continental mar-
gins (Haq 1980) where the species can  tolerate  the brackish
to  hypersaline,  high  productivity  environments  (Wade  &
Bown  2006).  Wells  &  Okada  (1997),  Flores  et  al.  (1997),
Bollmann  et  al.  (1998)  and  Kameo  (2002)  regard  small
Reticulofenestra  spp.  as  eutrophic  species  while  Hallock

(1987), Beaufort & Aubry (1992) and Spezzaferri et al.
(2009) suggested that blooms of small Reticulofenestra indi-
cate oligotrophic warm water.

(5) Plankton/benthos (P/B) ratio. This indicator should

change with paleodepth. The relationship between bathyme-
try  and  relative  abundance  of  planktonic  foraminifera  has
been determined by van der Zwaan et al. (1990). A discrepan-
cy between calculated paleodepth and sedimentology has been
pointed out, for example, in the Middle Miocene of the Central
Paratethys (Hohenegger 2005). Therefore, estimation of pale-
odepth  using  modified  plankton/benthos-ratio  was  compared
with  depth  ranges  of  individual  taxa  (Culver  &  Buzas  1980,
1981; Murray 1991; de Stigter et al. 1998; Hohenegger 2005;
van  der  Hinsbergen  et  al.  2005)  and  oxygenation  of  bottom
water. The high P/B-ratio in comparison with assumed paleo-
depth may be caused by postmortem transport of plankton to
the marginal part of the basin and/or by extra high production
of plankton as well as low production of benthos.

Bottom environment has been characterized by several in-

dicators:

(6) The BFOI= Benthic Foraminiferal Oxygen Index.

BFOI expresses oxygen content (Kaiho 1994, 1999):

BFOI = O/(O + D) 100

where O is the number of oxic indicators and D is the num-
ber of disoxic indicators. Oxic and disoxic indicators were
classified according to Kaiho (1994, 1999), den Dulk et al.
(1998), den Dulk et al. (2000), Spezzaferri et al. (2002) and
Báldi (2006).

(7) Relative abundances of high primary productivity indi-

cators among benthic species (Uvigerina grilli, Uvigerina
macrocarinata, Uvigerina pygmoides, Uvigerina uniseriata,
Melonis pompiloides; Spezzaferri et al. 2002).

(8) Size distribution of cibicidoid tests. It is evaluated

similarly to the size distribution of the Globigerina-plexus,
namely providing information on postmortem transport.

Statistical analysis of data was done using PAST software

(Hammer et al. 2001).

Results

Stable isotope compositions, test recrystallization and
taphonomic changes

Repeated measurements of isotopic composition of fora-

miniferal tests showed standard deviations higher than ac-
ceptable value < 0.3 for 20 samples out of the 27 analysed
(Table 1). To analyse the causes of this high variability, the
recrystallization of the inner test walls was re-evaluated and
taphonomical analysis of assemblages was done.

The recrystallization of inner test walls was re-analysed on

10—15 specimens from every sample. One to three recrystal-
lized specimens were detected per sample in 7 out of the 25
samples.  However,  the  variability  of  isotopic  composition
(expressed  by  standard  deviation)  does  not  correlate  posi-
tively with recrystallization degree, since the highest values
of  standard  deviations  were  recorded  for  samples  with  well
preserved tests (Table 1).

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GEOLOGICA CARPATHICA, 2012, 63, 2, 121—137

It is remarkable that standard deviations of

C and

values for individual samples are positively correlated for sam-
ples  with  only  well  preserved  tests  (correlation  coefficient
= 0.77), while a slightly negative trend appears for samples with
presence of recrystallized tests (correlation coefficient  = — 0.39).
As  the  standard  deviations  for

C and

O values show a

good positive correlation for well preserved samples and a
slight negative one for recrystallized tests, the isotopic scatter
seems to be related to primary characteristics rather than instru-
mental error, representing original water chemistry from the pa-
leobiotops in which the analysed specimens lived (Fig. 5).

To recognize postmortem transport and reworking of tests,

the taphonomic analysis of assemblages followed. Generally,
marked evidence of transport was not recorded: abrasion, ero-
sion and other damage to tests were not observed using SEM.
All benthic assemblages are composed of taxa with compara-
ble  environmental  requirements  (shallow  water,  normal  ma-
rine). Both planktonic and benthic species have corresponding
stratigraphic ranges. However, two indications of postmortem
changes  of  assemblages  were  recorded:  (1)  Size  sorting  of
tests  in  samples  from  the  PY-boreholes  showed  a  lack  of
small-sized tests (Figs. 6, 7) that may be caused by destruction

of  small  tests  in  high  energy  environment  and/or  dissolution
of  small  tests.  (2)  Paleodepth  calculated  from  the  P/B-ratio
(van  der  Zwaan  et  al.  1990)  showed  high  values  (excepting
samples  PY1/40,  PY3/230)  from  200  to  350 m  which  is  in
contrast with paleodepth estimated on the base of depth range
of  benthic  species  (from  20  to  100 m).  It  may  be  caused  by
postmortem transport of planktonic foraminifera and their ac-
cumulation  in  the  marginal  part  of  the  basin.    These  indica-
tions of postmortem transport of tests are taken into account in
the following interpretations.

Relations between isotopic compositions and other paleo-
environmental proxies

Correlations between the paleobiological proxies and be-

tween paleobiological proxies and isotopic values were quan-
tified using Spearman coefficients and statistically verified by
p-value (Tables 2, 3). The following correlations were consid-
ered to be statistically significant:

a) Mean test sizes of Globigerina spp. in individual sam-

ples correlate very positively with sizes of Cibicidoides spp.
(correlation coefficient = 0.85, p = 0.006);

Sample

Sta

nda

tio

asu

Sta

nda

tio

asu

umb

er of

asu

umb

ell

res

ved

tests t

umb

er of

rec

ryst

lized

tests

ge of

(

Z2/12.2/CIB 0.82

0.28 6 12 0 200–300

Z2/12.2/GL

0.13

0.17 3 13 0

80–200

Z2/16.9/CIB 0.69

0.24 3 11 0 200–300

Z2/16.9/GL

0.29

0.07 3 15 0 130–200

PY1/220CIB

0.15

0.33 4 13 0 220–300

PY1/220GL 1.42

0.70 3 11 0 180–200

PY1/40CIB

0.64

0.33 4 13 0 200–300

PY1/40GL

0.55

0.37 5 14 0 180–200

PY3/150CIB 0.69

0.43 6 12 0 250–300

PY3/150GL

0.25

0.24 5 14 0 130–200

PY3/230CIB 0.35

0.17 3 13 0 210–300

PY3/230GL 1.10

0.53 3 15 0 180–200

KRAS1CIB

0.16

0.05 4 12 0 200–300

KRAS1GL 0.80

0.03 4 14 0 100–200

KRAS4CIB 0.34

0.15 3 11 0 200–300

KRAS4GL

0.23

0.27 6 14 0 80–200

KRAS6CIB

0.10

0.14 2 13 0 200–300

KRAS6GL

0.40

0.71 6 15 0 130–200

KRAS11CIB

0.21

0.26 4 12 0

KRAS12CIB

0.16

0.36 4 13 0

KRAS3CIB 0.63

0.25 3 12 1

KRAS3GL 0.58

0.22 5 15 2

KRAS7CIB

0.14

0.73 4 15 2

Z2/8.5/CIB

0.79

0.44 5 13 1

Z2/8.5/GL 1.07

0.15 6 15 1

KRAS8/CIB 0.67

1.04 4 11 1

KRAS8/GL 0.36

0.42 3 15 3

Table 1: Standard deviations of

and

measurements, num-

bers of recrystallized tests in repeated SEM analysis of recrystalli-
zation and size ranges of isotopically analysed tests (for total ranges
see Fig. 6).

Fig. 5. Relations between standard deviations of

O and

mea-

surements for individual samples: A – samples with well-preserved
tests, B – samples with admixture of slightly recrystallized tests.

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GEOLOGICA CARPATHICA, 2012, 63, 2, 121—137

b) Planktonic foraminifera: Mean test size of Globigerina

spp.  negatively  correlates  with  relative  abundances  of  five-
chambered  Globoturborotalita  spp.  (correlation  coefficient
= — 0.80,  p = 0.007)  and  with  P/B-ratios  (correlation  coeffi-
cient = — 0.71, p = 0.031), positively with relative abundances
of  warm-water  plankton  (correlation  coefficient = 0.66,
p = 0.048). Furthermore, sizes of  Globigerina spp. negatively
correlate  with

O values (correlation coefficient = — 0.83,

p = 0.006) and with ranges of

O and

C measurements.

Relative abundances of five-chambered Globoturborotalita
spp. positively correlate with

O values (correlation coeffi-

cient = 0.70, p = 0.049) and relative abundances of warm-wa-
ter plankton with ranges of

O measurements (correlation

coefficient = 0.54, p = 0.048).

c) Benthic and benthic vs. planktonic foraminifera: Nega-

tive correlation was recorded between BFOI and size ranges
of  Globigerina  spp.  (correlation  coefficient = — 0.67,
p = 0.046)  and  between  test  sizes  and  size  ranges  of  cibici-
doids  (correlation  coefficient = 0.67,  p = 0.048).  Relative
abundances  of  high  nutrient  markers  negatively  correlate
with  differences  in  carbon  isotopic  composition  of  benthos
and  plankton  (correlation  coefficient = — 0.70,  p = 0.043),
positively  with  differences  in  oxygen  isotopic  composition
of  benthos  and  plankton  (correlation  coefficient = 0.64,
p = 0.048) and with

C values (correlation coefficient = 0.61,

p = 0.049).

According to the above mentioned correlations between

geochemical and paleobiological proxies, theoretical models
of two “boundary” foraminiferal assemblages can be defined
(Fig. 8):

Model (1). The first “boundary” assemblage is characterized

by small tests, plankton with higher abundances of five-cham-
bered Globoturborotalita spp., benthos by lower abundance of
high-nutrient markers correlative with higher BFOI index.
Higher

O values for plankton, lower differences between

oxygen isotope composition of benthos and plankton and larg-
er differences between carbon isotope composition of benthos
and plankton characterize isotopic values in this assemblage.

Model (2). The second “boundary” assemblage is com-

posed  of  larger  tests  with  higher  abundance  of  warm-water
taxa  in  plankton  and  higher  abundance  of  high-nutrient
markers  at  the  bottom.  The  isotopic  composition  of  tests  is
variable,  which  agrees  with  higher  size  variability  of  the
analysed taxa. The isotopic values are characterized by larger
differences between oxygen isotope composition of benthos
and  plankton  and  lower

O values, while the

C values

for plankton and benthos are similar.

Types of marginal foraminiferal assemblages

On the basis of quantitative isotopic (Fig. 9) and paleobio-

logical data, the studied samples were classified using Non-

Table 2: Values of Spearman coefficient (upper numeral) for paleobiological proxies based on species composition of assemblages and size
variability. Only coefficients with p-values (measure of significance; lower numeral) under 0.05 are recorded.

P/B-

-w

lan

Tes

t s

ize

(

lob

ange

(

Glo

big

Fiv

amb

ered

lita

spp

. (%)

ith

)

Tes

t s

ize

(

cib

)

ge (

cib

)

igh

rien

t m

ark

(be

ntho

BFO

P/B-ratio

–0.71
0.031

–0.68
0.049

Warm-water plankton

0.66
0.048

0.81

0.008

Test size (Globigerina)

–0.80
0.007

0.85
0.006

0.67
0.047

Size range (Globigerina)

–0.67
0.046

Five-chambered Globoturborotalita spp. (%)

–0.69
0.047

Coccolithus pelagicus (%)

Test size (cibicidoids)

0.67
0.048

Size range (cibicidoids)

High nutrient markers (benthos)

–0.81
0.01

BFOI

Spearman coefficients

p-value

Spearman coefficients

p-value

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GEOLOGICA CARPATHICA, 2012, 63, 2, 121—137

Geochemical proxies

Paleobiological proxies

(Glo

big

oid

Ran

easu

(Glob

Ran

easu

oid

cib

oid

lobi

(Glob

)

Ran

asu

rem

(Glob

Ran

asu

rem

oid

C c

ibic

ds-

lob

P/B-ratio

Warm-water plankton

0.54
0.048

Test size (Globigerina)

–0.83
0.006

0.65
0.043

0.72
0.031

Size range (Globigerina)

Five-chambered Globoturborotalita spp.

0.70
0.049

Coccolithus pelagicus (%)

Test size (cibicidoids)

Size range (cibicidoids)

0.69
0.042

High nutrient markers (benthos)

0.64

0.048

0.61

0.049

–0.70

0.043

BFOI

Spearman coefficients

p-value

metrical Multidimensional Scaling (Euclidean distance),
Principal Component Analysis and Cluster Analysis (Ward
method) (PAST-software). The following types of foramini-
feral assemblages can be distinguished (Fig. 10):

1. The “Přemyslovice” area is characterized by varying

isotopic compositions of tests (Fig. 9) and markedly differs
from the other sections (Fig. 9). Geochemical and paleobio-
logical markers showed that assemblages from this area are
near to the Model (2). Some isotopic values of planktonic
tests are comparable to values from the central part of the ba-
sin, mainly from the Gliwice boreholes due to higher

values (Fig. 11).

2. Foraminiferal assemblages in the “Kralice bay” (sam-

ples KRAS 1, 4, 6) and in the “Židlochovice” area are simi-
lar and agree with the Model (1) assemblage. However, some
differences can be observed. In the “Kralice bay”, the seawa-
ter system differs from the other part of the Central Para-
tethys by low

C values especially for the planktonic

foraminifera, though the

O values are comparable

(Fig. 11). A significant discrepancy between paleodepth esti-
mated from the P/B-ratio (300—350 m) and depth range of

Table 3: Values of Spearman coefficient (upper numeral) for relations between geochemical and other paleobiological proxies. Only coef-
ficients with p-values (measure of significance; lower numeral) under 0.05 are recorded.

Spearman coefficients

p-value

taxa (20—100 m) were recorded (Zágoršek et al. 2009). In the
“Židlochovice” area, two different assemblages were record-
ed. The assemblage from sample ZIDL2/16.9 is similar to
those from the “Kralice bay” with respect to species compo-
sition and size distribution of tests but isotopic composition
is specific with high

C values similar for benthos and

plankton (Fig. 10). Isotopic values are near to those from the
area of Gliwice (Fig. 11).

Discussion

Taking the high standard deviations obtained for many of

the analysed samples into account, reliability of the isotopic
data is a major issue. The isotopic scatter seems to be related
to primary characteristics rather than instrumental error, rep-
resenting original water chemistry from paleobiotopes in
which the analysed specimens lived. In order to display the
internal variability, not only average values but also whole
ranges of measured isotopic values were taken into consider-
ation in the paleoenvironmental interpretations.

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Fig. 6. Size sorting of planktonic tests; line indicates maximal diameter of suspension-transported tests.

Factors influencing the oxygen and carbon isotopic
variability in the marginal part of epicontinental seas

In the shallow-water marine facies, indigenous, transported

and/or reworked foraminiferal tests may be mixed. The fol-
lowing factors could have influenced the isotopic variabili-
ties in the studied samples:

1. Intraspecific variability. The correlation between the

size  of  planktonic  foraminifera  and  their  isotopic  composi-
tion is documented but studies have given contradictory evi-
dence.  The  factor  was  comprehensively  described  by
Waelbroecket  et  al.  (2005).  Within-test  variations  of

values may exceed 2 ‰ depending on the actual species. The

C values may be influenced by the presence of symbiotic

algae around the shell (Pearson & Wade 2009). They form a
local microenvironment with relatively heavy

C value

(Spero  &  Williams  1988;  Pearson  et  al.  1993;  Wade  et  al.
2008).  On  the  other  hand,  incorporation  of  metabolic  light
carbon  into  the  shells  can  cause  an  anomalously  light

ratio (e.g. Douglas & Savin 1978). This effect seems the

most  common  in  small  species  and  juveniles,  while  larger
species  and  larger  size  fractions  generally  give  isotopic  ra-
tios  closer  to  equilibrium  with  the

C value of the sur-

rounding water (Berger et al. 1978). However, laboratory
experiments conducted on the planktonic foraminifera
Globigerinoides sacculifer under controlled temperature and
light levels show that chamber

C values increase with in-

creasing light levels; the effect of ontogeny on chamber

is minimal. Chamber

O values are also not affected by on-

togeny, but decrease with increasing light levels (Spero &
Lea 1993). Within size differences in our planktonic fora-
minifera (80—200 µm; Table 1), the test sizes of Globigerina
spp. correlate negatively with

O values (correlation coef-

ficient = — 0.76;  Table 2)  in  agreement  with  observation  of
Waelbroecket  et  al.  (2005)  for  comparable  size  fractions
200—250 µm  vs.  250—315 µm.  Spero  et  al.  (2003)  recorded
opposite correlation but they compared the isotopic compo-
sition  of  size  fractions  250—350 µm  vs.  > 650 µm.  Signifi-
cant correlation between test size of benthic foraminifera and
isotopic values has not been observed (Table 2).

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Fig. 7. Size sorting of benthic tests; line
indicates maximal diameter of suspen-
sion-transported tests.

2. Seasonal variability: foraminifera

which  grew  during  the  warmer  and
colder  seasons  (e.g.  spring  and  sum-
mer population) may be mixed in one
sample and increase variability of iso-
topic composition in this sample. The
seasonality was detected for the Early
Badenian  of  the  Central  Paratethys
using  stable  isotope  profiles  of  Turi-
tella  that  showed  seasonal  differenc-
es  in  oxygen  isotopic  composition
from —0.5 to 1.5 ‰ (Latal et al. 2006).
Seasonality during the Early Badenian
is also expected from the paleobotanic
studies (Kvaček et al. 2006). Howev-
er, the question arises whether the sea-
sonal  differences  can  be  recorded  in
isotopic  composition  of  foraminiferal
tests. The life cycles of planktonic for-
aminifera are 2—4 weeks (Bijma et al.
1990);  for  individual  species  it  is  re-
stricted  to  a  specific  period  of  the
year.  Blooms  of  the  analysed  genus
Globigerina  are  reported  from  the
early  spring  (Kleijne  et  al.  1989;
Thunell  &  Reynolds  Sautter  1992;
Oda  &  Yamasaki  2005).  Then,  mea-
sured  isotopic  values  of  Globigerina
plexus  record  water  chemistry  during
early  spring  flourishing  of  Globigeri-
na and their high variability cannot be
caused  by  seasonal  differences  in  the
isotopic composition of sea water.

The situation is different for benthic

foraminifera. The majority of Cibici-
doides sp. tests is larger than 150 µm
(Fig. 7). For this size fraction Fontani-
er et al. (2006) supposed rather long-
term calcification processes (several
weeks or months), which limit the im-
pact of ephemeral

C enrichment dur-

ing eutrophic periods. However,
Mackensen et al. (1993) showed that
Cibicidoides wuellerstorfi

C values

may be influenced by seasonally high
organic  matter  fluxes.  Therefore,
these  inconsistent  actuoecological
data cannot explain whether the isoto-
pic  composition  of  Cibicidoides  sp.
reflects  the  “mean”  annual  isotopic
value  of  the  sea  water  or  the  value
during  a  seasonal  influx  of  organic
matter.  The

C and

O ranges at

normal marine isotopic compositions
around 0 ‰ (Fig. 10) support the as-
sumption of long growth over the year
averaging the carbon input from vari-
ous sources such as continental influx
or planktonic organic matter.

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3. Interannual climatic variability. Populations of decades

to  some  hundred  years  (depending  on  sedimentation  rate)
may  be  mixed  in  one  sample  (due  to  bioturbation).  During
this time, wet and dry and/or colder and warmer years can al-
ternate  which  may  cause  short-time  oscillations  of  salinity,
temperature and influx of organic matter from the continent.
Such disturbances could be expected particularly in the upper
part of the water column that can be interpreted from the sig-
nificant dominance of stress-tolerant small-sized Globigerina-
plexus (foraminifera) and Reticulofenestra minuta (calcareous
nannoplankton; Wade & Bown 2006). However, the ranges of
these  oscillations  and  their  influence  on  the  isotopic  values
cannot be quantified.

4. Postmortem transport. Lateral transport of the sinking

tests of planktonic foraminifera leads to differences between
living  and  sedimented  assemblages.  A  site  of  deposition,
therefore,  collects  faunas  from  a  certain  area  depending  on
combined  effect  of  current  directions  and  current  speeds
(Takahashi & Bé 1984). The source areas of planktonic fora-
minifera  may  be  characterized  by  paleoenvironments  and
water chemistries different from the area of their deposition.
Specimens from different areas may mix in one fossil assem-
blage  and  increase  its  variability.  Transport  of  planktonic
tests may be promoted by downwelling antiestuarine circula-
tion  assumed  for  the  Early  Badenian  by  Brzobohatý  (1987)
and Báldi (2006), although a complex model of water mass
circulation  has  not  been  established  yet.  Though  direction
and distance of the test transport cannot be determined from
the paleoceanographical model, a lateral transport of tests is
probable.

5. Reworking of foraminiferal tests. Reworking may be

expected in the study area because abundant intraclasts indi-

Fig. 8. Models of two “boundary” marginal-sea environments based on paleontological and geochemical proxies and their correlations.

cating  cannibalization  of  older  sediments  characterize  the
marginal Early Badenian lithofacies in the Carpathian Fore-
deep (Nehyba & Šikula 2007). Reworked tests may isotopi-
cally  differ  due  to  different  paleoenvironments  or  a  more
complex sedimentary history including secondary diagenetic
effects.  Besides  the  slightly  recrystallized  tests  recorded  in
some  assemblages  (Table 1),  reworked  tests  can  also  be  ex-
pected in samples with no indications of postmortem changes.

Marginal marine environments in the Carpathian Foredeep

To summarize isotopic and paleontological data (Figs. 8,

11, Tables 2, 3), the following types of marginal environ-
ments in the Carpathian Foredeep can be suggested:

1. Paleoenvironment in the “Kralice bay”. The Middle

Miocene sediments in this area represent a denudation relict
(situated about 30 km from the continuous extent of the Early
Badenian deposits; Nehyba & Šikula 2007), which were de-
posited during the second Langhian transgression (Hohenegger
et al. 2007) on the Variscan basement. Significant distur-
bances from the continent are expected. This hypothesis can
be supported by different carbon isotope values of planktonic
foraminiferal tests in comparison with similar foraminifera
from the central part of the Paratethys (Fig. 11).

The interpretation of the paleoenvironment in the “Kralice

bay” is based mainly on dominance of opportunistic taxa
(small Globigerina, Reticulofenetra minuta, small Cibici-
doides sp.), low

C values and larger differences between

carbon isotopic composition of benthos and plankton and no
indication of postmortem tests transport. Though

values may depend on many factors, the

C values for

plankton are near to areas with phytodetritus supply where

135

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2. The “Přemyslovice” area is characterized by peculiar

isotopic compositions of planktonic foraminiferal tests and
absence of small-sized tests. Samples PY1/220 and PY3/230
show high

C and

O variations. Higher abundance of

warm-water planktonic taxons indicating warmer rather oligo-
trophic conditions does not agree with higher abundance of
high-nutrient markers at the bottom. Increased isotopic vari-
ability  may  be  generally  explained  by  several  taphonomic
disturbances in assemblages: (i) mixing of indigenous, trans-
ported  and/or  reworked  tests  with  different  isotopic  ranges
in a dynamic environment in which small tests could be me-
chanically destroyed, (ii) missing of small-sized foraminifera
and higher abundance of resistant calcareous nannoplankton
species  Coccolithus  pelagicus  (Roth  &  Berger  1975;  Roth
1994; Flores et al. 2003) due to dissolution that may remove
a component with specific isotopic values or affect the isoto-
pic compositions via dissolution/reprecipitation. It is impor-
tant to note that dissolution was observed in sample PY1/200
with rare foraminifera (Fig. 4.10,11,17), although their isoto-
pic compositions were not determined concerning preserva-
tion stage. The low

O end of the field of samples PY1/220

and PY3/230 (Fig. 10) may indicate input of meteoric water
from the continent to the sea water, as diagenetic changes
can be excluded due to the lack of recrystallization signs.

3. The “Židlochovice” area is represented by two samples.

The assemblages are similar to those from “Kralice bay” and
a similar environment influenced by phytodetritus supply
can be expected. Sample ZIDL2/16.6 has high

C values

comparable for benthos and plankton suggesting a non-
stratified, well-mixed water column. The normal marine

C and

O values indicate the lack of riverine water influx

from the continent at this particular site.

Conclusions

Foraminiferal assemblages from three localities on the

marginal parts of the Moravian part of the Carpathian Foredeep
have been studied by means of paleobiological and stable C
and O isotope analyses. The complex interpretation of paleo-
biological characteristics and isotope compositions has led
us to the following conclusions:

1. For reliable interpretation of isotopic data in a marginal

nearshore environment, detailed taphonomical analysis of as-
semblages is necessary. Recrystallized tests may represent
only a small part of fossil assemblages. The influence of mix-
ing of indigenous, postmortem transported and reworked tests
should be expected even if no indicators of postmortem trans-
port and resedimentation of tests are observed. The postmor-
tem transport and resedimentation of tests is a considerable
cause of large variability of the isotopic composition of tests.

2. Even in indigenous assemblages, the isotopic composi-

tion of foraminiferal tests in marginal marine environment is
influenced  by  many  factors  including  strong  continental
influx  of  meteoric  water,  detrital  organic  matter  and  nutri-
ents.  Due  to  the  spatially  varying  influences,  the  isotopic
compositions  show  distinctions  between  different  parts  of
epeiric  basin  and  groups  of  taxa  with  different  life  strategy
(plankton, benthos).

3. In the studied parts of the Carpathian Foredeep, compari-

son of geochemical and paleobiological proxies enables us to
distinguish two types of shallow marine environments: (i) bay
influenced by seasonal phytodetritus supply connected with
bloom of opportunistic taxa and carbon isotopic values dif-
ferent from other parts of the Central Paratethys; (ii) dynamic
shore characterized by variable isotopic compositions proba-
bly due to mixing of indigenous, transported and reworked
tests.

Acknowledgments:  This  research  was  supported  by  Grant
Projects GAČR 205/09/0103 and MSM0021620855. The sta-
ble isotope facility of the Institute for Geochemical Research,
Budapest was financially supported by the National Office for
Research  and  Technology  (GVOP-3.2.1-2004-04-0235/3.0).
I  thank  Silvia  Spezzaferri  (University  of  Fribourg,  Switzer-
land) and  Johann Hohenegger (Vienna University, Austria)
for  their  comments  and  corrections  which  substantially  im-
proved the quality of this manuscript.

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