Przegląd
Geologiczny, vol. 46, nr 8/2, 1998
Correlation and sedimentary history of the Badenian gypsum
in the Carpathian Foredeep (Ukraine, Poland, and Czech Republic)
Tadeusz Marek Peryt*, Marek Jasionowski*, Stanislav Karoli**, Oleg I. Petrichenko***,
Andrey V. Poberegski***, Igor I. Turchinov****
Key words: Badenian, evaporites, gypsum, sedimentary basins, correlation, Carpathian Foredeep, Ukraine, Poland, Czech Republic
In the middle Miocene Badenian evaporite
basin of the Carpathian foreland basin, broad
zones of sulphate deposits occur in the marginal
parts, and narrow zones of chloride sediments are
restricted to the basin center (Fig. 1). The origin
of these evaporites is related to the salinity crisis
at the end of Middle Badenian. The time and
facies relations of evaporites occurring in
margi-nal and central parts of the Carpathian foreland
basin are still unc1ear and different correlation
has been proposed for particular parts of the basin
(Petrichenko et al., 1997). However, it is possible
to correlate particular mar ker beds in both
do-mains over a distance of hundreds of kilometers
(e.g. Garlicki, 1994; Peryt et al., 1994, 1997)
suggesting common controls of evaporite
depo-sition regardless of the geological setting.
In the
lower
part of the gypsum section in the
peripheral part of the basin, a unit built of blocky
crystalline intergrowths occurs (see photo on the
front page of this issue). It was recorded in major
part of the Carpathian Foredeep, from Koberice
(Moravia, Czech Republic)
in
the west (see Peryt
et al., 1997) to Odayev (eastem Galicia, West
Ukraine) in the east. In some sections in eastem
Galicia, the place of blocky crystalline
inter-growths is taken by nodular, secondary gypsum
(Fig. 4; Peryt, 1996), and further toward the east
by a unit of stromatolitic gypsum. The transition
between the unit of giant gypsum intergrowths
and the unit of stromatolitic gypsum occurs in the
area located between Odayev and Zalishchyky,
and its expressed by the occurrence of
intercala-Fig.
2. Crystalline gypsum overlain by stromatolitic
gypsum, Gorodnyts'ya. All photos by T.M. Peryt
Fig.
3. Marker bed of microcrystalline ("alabastrine")
gypsum seen in the middle of the outcrop, 01eshiv
*Państwowy
Instytut Geologiczny,
ul. Rakowiecka 4,00-975 Warszawa, Poland,
e-mail:tper@pgi.waw.pl
* * Geological Survey of Slovak Republic,
Werferova 1, 040 11 Kosice, Slovakia
***Institute of Geology and Geochemistry of
Combustible Minerais, NANU, Naukova 3A,
290053 Lviv, Ukraine
****Lviv Geological Survey Expedition,
Turgeneva 33,290018 Lviv, Ukraine
100 km
5km
Verenchanka • • Tovtry
limit ol occurrence ol Bademan
evaporites north ol CarpJthian overthrust
Bademan sulfate lac/es
Fig.
1. Occurrence ofthe Badenian sulphate deposits in the Carpathian Foredeep
(Czech Republic, Poland, Ukraine, and Moldova), showing the location of
outcrops referred to in the text and shown on the cover photos
Przegląd
Geologiczn
y,
vol.
46,
nr
8/2
,
1998
---
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--Fig. 4.
Example~of gypsum
sectiom
Borków
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Fig.
5. Marker bed of microcrystalline gypsum, Tovtry
Piski
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calated
with selenitic gypsum (Fig. 6; cf.
Ka-sprzyk,
1993).
Higher
up,
a
unit of sabre gypsum
occurs (see also photos on page 795 of this
issue,
and
the lower photo on the back of this issue).
It
contains, in its upper part, a thin (usually 10 cm
thick) intercalation of c1astic gypsum (Fig. 4).
Towards
the basin margins, the stromatolitic
gypsum replaces the sabre gypsum, and a
possib-le counterpart of c1astic gypsum
intercalation
in
the latter
is
a
lenticular
layer/lamina of limestone
occurring in some sections composed of
stroma-tolitic
~ypsum
(Fig. 7). This limestone has
8
180
and 8
lC values that are characteristic for
con-temporaneous marine limestones: between 0.19
and
-4.94%0
(except of Kudryntsi where they are
-5
.
91 and
-7.93%0)
and 0.85 and
-2.55%0,
re-spectively.
tion (a
few
tens of cm thick) of crystalline gypsum within
the stromatolitic unit (Fig. 2)
.
In the area located between Seret and Zbruch
rivers in West Ukraine, vertically elongated dome
structures, 5 to 10m across, occur (Turczynow
&
Andrijczuk, 1995). The dome nuc1ei are composed of
stro-matolitic gypsum, and the dome peripheries are built of
sabre gypsum crystals that differ from those earlier
descri-bed from southem Poland (e.g.
Bąbel,1986; Kasprzyk,
1993) in that they are thinner, they are bent upward, and
consist of many subcrystals (see the lower photo on p. 795
Above, a characteristic, thin (10-40 cm) bed of
charac-teristic microcrystalline ("alabastrine") gypsum occurs (Figs
3-5); in many place s this unit is preceded by a few thinner
beds of microcrystalline and/or stromatolitic gypsum
giant gypsum intergrowths nodular gypsum stromatolitic gypsum
~ stromatolitic gypsum with
b d
com mon intercalations otalabastrine gypsum
~ clastic I.aminated and
1-
-
-I
clay ~ redeposlted gypsum - _-~ moulds ot halite
t..:....:.:...:
crystalsl •••
• • : .'
breccia gypsumD
alabastrine gypsum~
=
1
banded gypsum ~ ~ planar laminated gypsum~ srass -like gypsum ,-:,ith
r=-=l
druse aggregates ot ~ Interbeds ot alab.a.stnoe ~ gypsum crystalsand/or stromatohtlc gypsum
~
sabre gypsum 1f';'
crystalline gypsum1
~
:y4/-1
nucleation conesF===1
G;;;;J
crinkled laminated gypsumTovtry
Przegląd
Geologiczny, vol.
46,
nr
8/2, 1998
and
the
upper
photo on the back of this
issue; Turchinov, 1997)
.
The
upper part of the
gypsum
se-quence consists of
interbedded
lami-nated gypsum, gypsiferous c1aystones
and gypsum breccias (Petrichenko et al.,
1997;
Fig. 4). The redeposition
pheno-mena are common
in
that part of the
gypsum section (Peryt &
Jasionowski,
1994;
Peryt
et al.,
1997).
In the central
part of the basin, the place of gypsum
is
taken by anhydrite, and the
redepo-sition features abound
throughout
the
entire sulphate section that is built of
laminated anhydrite intercalated with
anhydrite breccia (Peryt et al.,
1998).
Odayev
Gavry/'ak
Babyn
Verenchanka
The middle Miocene Badenian
gypsum of Carpathian Foredeep was
mostly deposited, in the lower part of
the stratigraphic section,
in
a vast
bri-ne
pan. This brine pan was
charac-terised by a facies mosaic that reflects
an
interplay
of concentrated brines
from the central part of the evaporite
basin and diluted brines, possibly due
to the influx of continental meteoric
waters (Peryt, 1996).
Althoughindivi-dual depositional features and facies
types in the Badenian may be
explai-ned by comparison with modem
sali-nas (e.g. Orti Cabo et al., 1984), lateral
persistence of thin beds over large
are-as with only minor changes in
thick-ness and facies indicates that they
formed on broad, very low relief areas
which could be affected by rapid
transgressions. Asimilarity of
evapo-rite facies through the Badenian basin
seems to be related to an extrabasinal
"
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~~
"V ~ ~ -../~ "": ...,. ~ ::--~\,'AWVl~~rrł-(f:(~
-.,.... -v :v::~~"
'\ '\ '\ '\ '\\
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'\Fig. 7. Lenticular limestone bed in the upper part of the stromatolitic gypsum
section at Kudryntsi; the top of limestone bed is below the elbow of right hand
of A.V. Poberegski
Fig. 6. Intercalations of selenitic gypsum and stromatolitic/alabastrine gypsum
below the marker bed of microcrystalline gypsum, Verenchanka
Przegląd
Geologiczny, vol.
46,
nr
8/2, 1998
controi
that did not obscured important local and regional
tectonics. Intrabasinal marker beds occurring in the
evapo-rite sequences record distinct phases ofbrine body evolution
(frequent refreshing episodes) or diagenesis related to
sub-aerial exposure.
In the peripheral part of the basin, gypsum is ovedain by
marine limestone (Ratyn Limestone). The boundary
be-tween gypsum and limestone is the
sequence
boundary, and
gypsum deposits prior to
carbonate
deposition underwent an
important faulting phase
and
subsequent erosion.
References
BĄBEL M. 1986 - Growth of crystals and sedimentary structures in the sabre-like gypsum (Miocene, southern Poland). Prz. GeoI., 34: 204-208. GARLICKI A 1994 - Porównanie osadów solnych Górnego Śląska i okolic Wieliczki. Prz. GeoI., 42: 752-753.
KASPRZYK A. 1993 - Lithofacies and sedimentation of the Badenian (Middle Miocene) gypsum in the northern part of the Carpathian Fore-deep, southern Poland. Ann. Soc. Geol. Pol., 66: 33-84.
ORTI CABO F., PUEYO MUR JJ., GEISLER-CUSSEY D. & DULAU N. 1984 - Evaporitic sedimentation in the coastal salinas of Santa Pola (Alicante, Spain). Rev. Inst. Inv. Geol., 38/39: 169-220.
PERYT TM. 1996 - Sedimentology ofBadenian (middle Miocene) gy-psum in eastern Galicia, Podolia and Bukovina (West Ukraine). Sedimen-tology, 43: 571-88.
PERYT TM. & JASIONOWSKI M. 1994 - In situ formed and redepo-sited gypsum breccias in the Middle Miocene Badenian of southern Po -land. SedimenL GeoI., 94: 153-163.
PERYT TM., KAROLI S., PERYT D., PETRICHENKO 0.1., GEDL P., NARKIEWICZ W., DURKOVICOVA J. & DOBIESZYŃSKA Z.
1997 - Westernmost occurrence of the Middle Miocene Badenian gy-psum in central Paratethys (Kobefice, Moravia, Czech Republic). Slovak
GeoI. Mag., 3: 105-120.
PERYTTM., PERYT D., SZARAN J., HAŁAS S. & JASIONOWSKI M. 1998 - O poziomie anhydrytowym badenu w otworze wiertniczym Ryszkowa Wola 7 k. Jarosławia (SE Polska). BiuI. Państw. InsL GeoI., 379: 61-78.
PERYT TM., POBEREŻSKI AW., JASIONOWSKI M., PETRY-CZENKO 0.1., PERYT D. & RYKA W. 1994 - Facje gipsów badeń
skich Ponidzia i Naddniestrza. Prz. Geol., 42: 771-76.
PETRICHENKO 0.1., PERYT T.M. & POBEREGSKI AV. 1997 - Pe-cularities of gypsum sedimentation in the Middle Miocene Badenian eva-porite basin of Carpathian Foredeep. Slovak Geol. Mag., 3: 91-104. TURCHINOV 1.1. 1997 - Litologiczne uwarunkowania rozwoju proce-sów krasowych w badeńskich gipsach Przedkarpacia. Prz. Geol., 45:
803-806.
TURCZYNOW 1.1. & ANDRIJCZUK W.M. 1995 - Kopułowate stru -ktury w badeńskich gipsach Naddniestrza. Prz. Geol., 43: 403-405.
Paleoeeology and organie matter
in
the Late Badenian and Early Sarmatian
marine basin of the Polish part of the Carpathian Foredeep
Iwona Czepiec*, Maciej
J.
Kotarba**
The studies aim to determine both the eeologieal and geoehemieal eonditions oj
the Late Badenian and Early Sarmatian sedimentary
basin loeated in the outer part ojthe Carpathian Foredeep. Partieularly interesting are: depositional environment oj organie matter,
depth ojthe basin and water temperatures. The Late Badenian sea was presumably only slightly deeper than the outer shelf, i.e. about
200 meters. The warm climate resembling that oj the
warm
temperate zone resulted in
surjaee
water temperatures 17-20°C.
In
the
Sarmatian the sea depth was initially about 30-50 meters thus,
the existenee oj submarine meadows was injerred.
Then,
progressing
shallowing to
about
10 meters took place.
The
Sarmatian sea was a warm basin with temperatures roughly eorresponding to those oj
the Late Badenian ones. Organie matter
deposited during both the Badenian and the Sarmatian reveals terrestrial origin. Organie matter
in
the Late Badenian
and Early Sarmatian
strata is immature or,
at most, early matured but at depth
below
3000 meters. Very low
eorrelation ojboth the eoneentrations and the maturation degree ojthe organie matterwith its depth ojoeeurrenee suggest the similarity
oj sedimentary environments in the whole Miocene sueeession and the laek ojthermal transjormation after deposition. Almost exclusive
oeeurrenee oj
the humie organie matter points to the jast and rhythmie supply oj
terrestrial clay matter to
the deltaie environments in
the shallow Miocene basin. A rapid sedimentation oj
terrestrial, deltaic sediments took place in the Miocene basin, therejore
the humie
organie matter (typ e III kerogen) prevailed there and the marine type II kerogen was hardly deteetable.
Key
words:
areal geology, Badenian, Sarmatian, basin analysis,foraminifers, paleoeeology, organie materials, Carpathian Foredeep,
Poland
Introduction
The joint studies on microfossils and organie
geochemi-stry of the
Late
Badenian and Eady Sarmatian sediments aim
to determine both
the
ecological and organie matter
deposi-tion condideposi-tions in the sedimentary basin located in the outer
part of the Carpathian Foredeep. Special attention was paid
to depositional environment of the organie matter (OM),
depth of the basin and water temperatures.
These
data are
crucial
for
the reconstruction of generation and
accumula-tion systems of natural gases (Szafran, 1990;
Kotarba
et al.,
1998a).
Such preliminary reconstruction has been based
*University
ofMining and Metallurgy, Department of
Stratigraphy
&
Regional Geology,
al.
Mickiewicza 30,
30-059 Kraków, Poland, email: iwczep@geolog.geol.agh.edu.pl
**University of Mining and Metallurgy, Department of
Fossil Fuels,
al. Mickiewicza 30,30-059 Kraków, Poland,
email:
kotarba@uci.agh.edu.pl
732
upon
the
results of routine geochemie al analyses of
hydro-carbons (Rock
Eval
and extraction) as well as upon the
studies on
microfossil
assemblages with the
reference
to
other fossil remains (particularly to their taxons composition
and degree of preservation
in
the sediment).
The study
has been
undertaken as a part of research
projects of
the
Carpathian
Foredeep financed
by the State
Committee for Scientific Research
in
Warsaw (grant No.
992149203) and National Fund for Environmental
Protec-tion and Water Management (grant No.
2.14.0100.00.0).
Materiał
