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 100 km 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 limit ol occurrence ol Bademan 5km evaporites north ol CarpJthian to correlate particular marker beds in both do­ overthrust mains over a distance of hundreds of kilometers Verenchanka • • Tovtry Bademan sulfate lac/es (e.g. Garlicki, 1994; Peryt et al., 1994, 1997) suggesting common controls of evaporite depo­ Fig. 1. Occurrence ofthe Badenian sulphate deposits in the Carpathian Foredeep sition regardless of the geological setting. (Czech Republic, Poland, Ukraine, and Moldova), showing the location of outcrops referred to in the text and shown on the cover photos 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:[email protected] * * 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

729 Przegląd Geologiczny, vol. 46, nr 8/2, 1998 ------

Kobe'fice Borków Piski Pidkamin' Podil/'a O/eshiv

~. .~"---.t.- - .~ ' . . . - .....•. . . ~ ;l~-;--- . . . '\ '\ '\ Fig. 4. Example~ of gypsum sectiom "I '\ "\ '\ "\ "\ '\ . '\ '\ " '\ "I "\ "\ "\ "I "I "\ "\ '\ "\ '\ "\ '\ "I "I "I "\ "\ " '\ '\ "\ '\ "I "\ "I "I "- '\ '\ '\ '\ "I " "I " "\ "\ '\ '\ '\ '\ '\ "\ "\ "I "'\ '\ '\ "I "'\ "\" "\" "\ " " " " " "\ '\ "\ '\ "I "\ "\ "\ "\ "\ "\ '\ '\ " '\ " " '\ '\ '\

~~~ ~~ Ij ~~~

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 8180 and 8 l C 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. In the area located between Seret and Zbruch Fig. 5. Marker bed of microcrystalline gypsum, Tovtry rivers in West Ukraine, vertically elongated dome structures, 5 to 10m across, occur (Turczynow & tion (a few tens of cm thick) of crystalline gypsum within Andrijczuk, 1995). The dome nuc1ei are composed of stro­ the stromatolitic unit (Fig. 2). matolitic gypsum, and the dome peripheries are built of Above, a characteristic, thin (10-40 cm) bed of charac­ sabre gypsum crystals that differ from those earlier descri­ teristic microcrystalline ("alabastrine") gypsum occurs (Figs bed from southem Poland (e.g. Bąbel, 1986; Kasprzyk, 3-5); in many place s this unit is preceded by a few thinner 1993) in that they are thinner, they are bent upward, and beds of microcrystalline and/or stromatolitic gypsum inter- consist of many subcrystals (see the lower photo on p. 795

730 Przegląd Geologiczny, vol. 46, nr 8/2, 1998

giant gypsum ~ stromatolitic gypsum with and the upper photo on the back of this bd com mon intercalations ot intergrowths alabastrine gypsum issue; Turchinov, 1997). The upper part of the gypsum se­ nodular gypsum ~ clastic I.aminated and 1---I clay ~ redeposlted gypsum - _ - quence consists of interbedded lami­ ~ moulds ot halite nated gypsum, gypsiferous c1aystones stromatolitic gypsum l••• ' gypsum t..:....:.:...: crystals ••:. breccia and gypsum breccias (Petrichenko et al., ~ planar 1997; Fig. 4). The redeposition pheno­ D alabastrine gypsum ~ =1banded gypsum ~ laminated gypsum mena are common in that part of the ~ srass -like gypsum ,-:,ith r=-=l druse aggregates ot gypsum section (Peryt & Jasionowski, ~ Interbeds ot alab.a.stnoe ~ gypsum crystals and/or stromatohtlc gypsum 1994; Peryt et al., 1997). In the central ~ sabre gypsum 1 f';' crystalline gypsum part of the basin, the place of gypsum is taken by anhydrite, and the redepo­ F===1 crinkled laminated Tovtry 1~ :y4/-1 nucleation cones G;;;;J gypsum sition features abound throughout the entire sulphate section that is built of laminated anhydrite intercalated with anhydrite breccia (Peryt et al., 1998). The middle Miocene Badenian Odayev Gavry/'ak Babyn Verenchanka 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 "V ned by comparison with modem sali­ ~

~ "": nas (e.g. Orti Cabo et al., 1984), lateral -../~...,. ~ ::-- persistence of thin beds over large are­ ~\,'AWVl~~ as with only minor changes in thick­ -.,.... -v :v::~~ rrł-(f:(~ 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

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

731 Przegląd Geologiczny, vol. 46, nr 8/2, 1998

controi that did not obscured important local and regional PERYT TM. 1996 - Sedimentology ofBadenian (middle Miocene) gy­ tectonics. Intrabasinal marker beds occurring in the evapo­ psum in eastern Galicia, Podolia and Bukovina (West Ukraine). Sedimen­ tology, 43: 571-88. rite sequences record distinct phases ofbrine body evolution PERYT TM. & JASIONOWSKI M. 1994 - In situ formed and redepo­ (frequent refreshing episodes) or diagenesis related to sub­ sited gypsum breccias in the Middle Miocene Badenian of southern Po­ aerial exposure. land. SedimenL GeoI., 94: 153-163. In the peripheral part of the basin, gypsum is ovedain by PERYT TM., KAROLI S., PERYT D., PETRICHENKO 0.1., GEDL P., NARKIEWICZ W., DURKOVICOVA J. & DOBIESZYŃSKA Z. marine limestone (Ratyn Limestone). The boundary be­ 1997 - Westernmost occurrence of the Middle Miocene Badenian gy­ tween gypsum and limestone is the sequence boundary, and psum in central Paratethys (Kobefice, Moravia, Czech Republic). Slovak gypsum deposits prior to carbonate deposition underwent an GeoI. Mag., 3: 105-120. important faulting phase and subsequent erosion. 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., References 379: 61-78. PERYT TM., POBEREŻSKI AW., JASIONOWSKI M., PETRY­ BĄBEL M. 1986 - Growth of crystals and sedimentary structures in the CZENKO 0.1., PERYT D. & RYKA W. 1994 - Facje gipsów badeń­ sabre-like gypsum (Miocene, southern Poland). Prz. GeoI., 34: 204-208. skich Ponidzia i Naddniestrza. Prz. Geol., 42: 771-76. GARLICKI A 1994 - Porównanie osadów solnych Górnego Śląska i PETRICHENKO 0.1., PERYT T.M. & POBEREGSKI AV. 1997 - Pe­ okolic Wieliczki. Prz. GeoI., 42: 752-753. cularities of gypsum sedimentation in the Middle Miocene Badenian eva­ KASPRZYK A. 1993 - Lithofacies and sedimentation of the Badenian porite basin of Carpathian Foredeep. Slovak Geol. Mag., 3: 91-104. (Middle Miocene) gypsum in the northern part of the Carpathian Fore­ TURCHINOV 1.1. 1997 - Litologiczne uwarunkowania rozwoju proce­ deep, southern Poland. Ann. Soc. Geol. Pol., 66: 33-84. sów krasowych w badeńskich gipsach Przedkarpacia. Prz. Geol., 45: ORTI CABO F., PUEYO MUR JJ., GEISLER-CUSSEY D. & DULAU 803- 806. N. 1984 - Evaporitic sedimentation in the coastal salinas of Santa Pola TURCZYNOW 1.1. & ANDRIJCZUK W.M. 1995 - Kopułowate stru­ (Alicante, Spain). Rev. Inst. Inv. Geol. , 38/39: 169-220. 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 upon the results of routine geochemie al analyses of hydro­ carbons (Rock Eval and extraction) as well as upon the The joint studies on microfossils and organie geochemi­ studies on microfossil assemblages with the reference to stry of the Late Badenian and Eady Sarmatian sediments aim other fossil remains (particularly to their taxons composition to determine both the ecological and organie matter deposi­ and degree of preservation in the sediment). tion conditions in the sedimentary basin located in the outer The study has been undertaken as a part of research part of the Carpathian Foredeep. Special attention was paid projects of the Carpathian Foredeep financed by the State to depositional environment of the organie matter (OM), Committee for Scientific Research in Warsaw (grant No. depth of the basin and water temperatures. These data are 992149203) and National Fund for Environmental Protec­ crucial for the reconstruction of generation and accumula­ tion and Water Management (grant No. 2.14.0100.00.0). tion systems of natural gases (Szafran, 1990; Kotarba et al., 1998a). Such preliminary reconstruction has been based Materiał and methods

The source materials were 85 core c1aystone/mudstone *University ofMining and Metallurgy, Department of Stratigraphy & Regional Geology, al. Mickiewicza 30, sampies of autochthonous Late Badenian and Early Sarma­ 30-059 Kraków, Poland, email: [email protected] tian sediments of the Carpathian Foredeep collected from **University of Mining and Metallurgy, Department of the following 11 wells (Fig. 1): Brzóza Stadnicka 1 (BS 1), Fossil Fuels, al. Mickiewicza 30,30-059 Kraków, Poland, Czarny Las 3 (CL-3), Dobra 4 (Do-4), Jaksmanice 257 email: [email protected] (1-257), Jodłówka 4 (10-4), Komorów 2 (Km-2), Łazy 9

732