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ABSTRACT

The facies distribution of the Late Cenomanian carbonate plat-form deposits of the Tripolitza zone, in central Peloponnesus (Vitina,Mainalon Mnt., Greece) is more or less uniform and supports a flattopography of the related platform sector during the above interval.Peritidal facies with shallow-upward cyclothems predominate, contain-ing a subaerial exposure evidence, while parts of the studied sectioncorrespond to vanished evaporites. Texturally, the Late Cenomanianlimestone in central Peloponnesus, as well as, in central eastern Crete,appear principally as wackestone, lesser as wackestone-packstone andonly randomly as packstone-floatstone. Peloidal wackestone are com-mon, as well, characterized by irregular fenestrae and/or dissolutioncavities. Grainstone (intrabiopelsparites) are minor in occurrence.

Facies associations include: fossiliferous limestone/dolostoneand microbial laminites documenting a low-energy, restricted shal-low subtidal environment to intertidal/supratidal settings in a ramp-like depositional system comparable with the Balearic ramp-likeplatforms; temporary high-energy conditions also periodicallyoccured; dolomites/dedolomites after preexistent evaporites assignedto supratidal conditions and intermittent subaerial exposure as wellas pedogenic limestone-conglomerates support a long-term, terres-trial exposure environment. The thick shale interval detected in theVitina section supports a long-lasting exposure (sedimentary hiatus)of the platform during the Late Cenomanian. Pedogenic alteration ofthe sediments is intensive along certain horizons, indicatingrepeated sea-level fall intervals, supporting regional sea-level fluctua-tions, of allogenic origin, during a general sea-level rise status, whichfor the Late Cenomanian is known to coincide with the highestglobal sea-level stand.

KEY WORDS: Facies Associations, Late Cenomanian, long-term/terrestrial subaerial exposure.

RIASSUNTO

Associazioni di facies del Cenomaniano superiore nellapiattaforma carbonatica della subzona di Tripolitza (Vitina, Pe-loponneso centrale, Grecia): evidenze di esposizione subaereaprolungata.

Nella regione studiata (Vitina, Monte Mainalon, Peloponessocentrale, Grecia) affiora una sequenza sedimentaria che rappresentaparte del Cenomaniano superiore della piattaforma carbonatica del-la subzona di Tripolitza. La distribuzione delle facies nelle aree di af-fioramento studiate, è più o meno uniforme e testimonia un bassorilievo topografico dell’ area durante il Cenomaniano superiore. Cicliperitidali tipo shallowing-upwards, modificati da processi di esposi-zione subaerea non-prolungata sono prevalenti, mentre parte dellasuccessione in esame e rappresentata da facies indicative del am-biente sopratidale-evaporitico. Dal punto di vista tessiturale, i carbo-nati investigati sono costituiti principalmente da wackestone, da mi-

nori wackestone-packestone e infine da rari packstone-floatstone. Laloro deposizione avveniva in settori interni di una piattaforma car-bonatica, comparabile a quelli della rampa Balearica.

Le associazioni delle facies indentificate, includono: calcari edolomie fossiliferi- e laminiti algali stromatolitici, depositati in unambiente caratterizzato da bassa energia e scarsa turbolenza, dasubtidale di debole profondità a situazioni deposizionali intra-sopra-tidali; dolomie/dedolomie in sostituzione di minerali evaporiticipreesistenti, riferibili ad un ambiente sopratidale e marcate da strut-ture di esposizione subaerea; calcari e conglomerati di origine pedo-genetica documentanti fasi di emersione ed evidenze di alterazionemeteorica. Il livello argilloso, di spessore notevole, ritrancciato nelaffiorammento esaminato, riflette la presenza di una grande lacunastratigrafica (hiatus sedimentare). I livelli pedogenizzati riconosciu-ti, rivelano ripetute fluttuazioni (abbassamenti) eustatiche, duranteil generale innalzamento globale del livello marino registrato nel Ce-nomaniano superiore.

TERMINI CHIAVE: Associazioni di facies, Cenomanianosuperiore, Esposizione subaerea prolungata.

INTRODUCTION

In the Cretaceous peri-Adriatic Carbonate Platforms,the Cenomanian successions were characterized by a sig-nificant turnover of facies and biota in relation with thedevelopment of complex pathworks of depositional envi-ronments. Previous investigations of Cenomanian shal-low-water limestone that crops out in central easternCrete (Greece, ZAMBETAKIS-LEKKAS et alii, 1995, ZAMBE-TAKIS-LEKKAS et alii, 2007) as well as, in the CentralPeloponnesus (Greece, ZAMBETAKIS-LEKKAS, 1988; ZAM-BETAKIS-LEKKAS et alii, 1995; ZAMBETAKIS-LEKKAS &ALEXOPOULOS, 2007) enabled to us to detect a cyclicstacking pattern was prevailing in the analyzed succes-sions. Successions are composed of shallowing-upwardscycles in which the sedimentary composition and tex-ture, sedimentary structures and fauna are consistentwith intertidal-shallow subtidal flats in inner-shelf low-energy depositional settings. Intense dolomitization, sig-nificant processes of pedogenesis and, locally, clear evi-dences of pre-existing evaporites are common features ofthese carbonates representing an interesting topic to beinvestigate in order to interprete some of the Cenoman-ian depositional settings.

The aim of the present study was the recognition offacies distribution of the Late Cenomanian carbonateplatform deposits of the Tripolitza zone, in central Pelo-ponnesus (Vitina, Mainalon Mnt, Greece), the determina-tion of the responsible environmental factors and thepalaeoenvironmental reconstruction of the platform dur-ing the Late Cenomanian.

Boll.Soc.Geol.It. (Ital.J.Geosci.), Vol. 128, No. 1 (2009), pp. 00-00, 2 figs., 3 pl.

Facies associations of the late Cenomanian carbonate platform of Tripolitza subzone (Vitina, Central Peloponnesus, Greece):

evidence of long-term/terrestrial subaerial exposure

F.A. POMONI-PAPAIOANNOU (*) & A. ZAMBETAKIS-LEKKAS (*)

(*) Department of Geology and Geoenvironment, Section ofHistorical Geology and Palaeontology, National University of Athens,Panepistimiopolis, 157 84 Athens, Greece. E-mail: [email protected]

SGI - 212_34/07

Queste bozze, corrette e accompagnate dall’al-legato preventivo firmato e dal buono d’ordine,debbono essere restituite immediatamente allaSegreteria della Società Geologica Italianac/o Dipartimento di Scienze della TerraPiazzale Aldo Moro, 5 – 00185 ROMA

GEOLOGICAL SETTING

The Mainalon mountain, situated in central Pelopon-nesus (Greece), is principally formed by thrust sheets ofTripolitza and Pindus units (LEKKAS, 1977, 1978; FLEURY,1980; CAROTSIERIS, 1981). The investigated series belongsto the Cretaceous carbonate sequence of Tripolitza unit(ZAMBETAKIS-LEKKAS, 1988; ZAMBETAKIS-LEKKAS, 2006;ZAMBETAKIS-LEKKAS & ALEXOPOULOS, 2007). The seriesis intensively faulted.

The Tripolitza zone constitutes the eastern (internal)part of the Gavrovo-Tripolitza platform, of the Hellenides.TSAILA-MONOPOLIS (1977), FLEURY (1980) and ZAMBE-TAKIS-LEKKAS (2006) present in a synthetic way thestratigraphy and the sedimentology of the Tripolitzazone. FLEURY (1980), presents a biozonation of the Creta-ceous deposits of the Gavrovo-Tripolitza platform, deter-mining 7 biozones for the Albian-Maestrichtian interval.The investigated in this paper series corresponds to theCsB2 Fleury’s biozone of upper Cenomanian age. Accord-ing to FLEURY (1980), BERNIER & FLEURY (1980), duringthis period subtidal conditions of sedimentation domi-nated in the Tripolitza zone, while intertidal/supratidalconditions of sedimentation in the Gavrovo zone. ZAMBE-TAKIS-LEKKAS (1988) and ZAMBETAKIS-LEKKAS et alii

(1988) describe in central Peloponnesus, in the Vitinaarea an emergence episode during late Cenomanian inthe Tripolitza zone. More detailed investigations in theregion provided strong evidences of a local, long-term/ter-restrial exposure environment. In this paper we docu-ment these evidences and we discuss about the durationand the responsible reasons for this emergence episode.

METHODS

The section has been lithologically, sedimentologi-cally and biostratigraphically described, the repetitivefacies patterns have been interpreted and a detailed strati-graphic log has been constructed.

STRATIGRAPHY

The outcrop investigated is located on the road Vitina-Tripolis 6 km from Vitina (fig. 1). It belongs to the Creta-ceous carbonate sequence of Mainalon (ZAMBETAKIS-LEKKAS, 1988). The outcropping limestone is intensivelyfaulted and its upper Cenomanian part, reaching up to150m in thickness, is dated by Pseudorhapydionina dubia,

2 F.A. POMONI-PAPAIOANNOU & A. ZAMBETAKIS-LEKKAS

Fig. 1 - Map showing the studied locality. Pa: Patras, P: Pyrgos, T: Tripolis, S: Sparti. 1: Alluvial, 2: Quaternary conglomerates, 3: UpperCretaceous limestones of the Pindos series, 4: radiolarites, 5: Cretaceous limestones of the Tripolitza series, 6: fault, 7: overthrust.– Carta della area studiata con ubicazione della sezione di Vitina. Pa: Patrasso, P: Pyrgos, T: Tripolis, S: Sparta. 1: Alluvioni 2: Conglomerati delQuaternario, 3: Calcari del Cretaceo superiore-serie del Pindos, 4: Radiolariti, 5: Calcari del Cretaceo-serie di Tripolitza, 6: faglie, 7: overthrust.

FACIES ASSOCIATIONS OF THE LATE CENOMANIAN CARBONATE PLATFORM OF TRIPOLITZA SUBZONE 3

Fig. 2 - Lithostratigraphic log of the Vitina section.– Colonna stratigrafica della sezione esaminata di Vitina.

Pseudorhapydionina laurinensis, Pastrikella balcanica,Pseudonummoloculina regularis, Biplanata peneropli-formis, cf. Merlingina cretacea. Nezzazatinae, discorbids,ophthalmidiids, Aeolissacus kotori, ostracods gastropodsand Thaumatoporellaceans are found associated.

We studied in detail the upper part of the upper Ceno-manian interval, more than 50m in thickness and verypoor in fossil assemblages. The microfauna componentsare rare and badly preserved, so suggesting unfavorablepaleoecological conditions.

Lithologies, textures, sedimentary structures, as wellas the fossil content have been analyzed (see the strati-graphic log in fig. 2) enabling us to recognize, from thebase to the top, the Units below:

Unit A: 10m of thick-bedded limestone and dolostone.Unit B: 10m of thick- to medium-bedded limestone

bearing Nezzazatinae and cf Merlingina cretacea.Unit C: 3m of thick to medium bedded limestone

which contain, in its upper portion, un argillaceous inter-val ranging in thickness from 20 to 50 cm. Well roundedintraclasts from the underlying strata occur in the argilla-ceous layer. Pseudonummoloculina regularis (photo PlateIII/4) marks the top of the limestone immediately under-lying the argillaceous level.

Unit D: 30m of limestone and dolostone, with aninterval consisted of dolomite breccia (schvma?). In addi-tion, two thin argillaceous intercalations occur betweenthe carbonate beds. Pseudonummoloculina regularis andBiplanata peneropliformis have been recognized.

BIOSTRATIGRAPHICAL REMARKS

The investigated carbonates overlies a sequence of darklimestone, upper Cenomanian in age on the base of thepresence of Pseudorhapydionina dubia, Pseudorhapydion-ina laurinensis, Pastrikella balcanica, Pseudonummolo-culina regularis, Biplanata peneropliformis, cf. Merlinginacretacea, Nezzazatinae. In the described units the micro-fauna is rare. Nevertheless, Pseudonummoloculina regularisoccur immediately under the argillaceous level, as well asin association with Biplanata peneropliformis, in the overly-ing the argillaceous level carbonates. This fact provides evi-dences that the whole sequence was deposited during thelate Cenomanian. It belongs to the CsB2 Fleury’s biozoneof the Gavrovo-Tripolitza upper Cretaceous sediments.

FACIES ASSOCIATION AND DEPOSITIONAL MODELS

In the studied section, the following facies associa-tions (F) have been recognized:

– F1: fossiliferous limestone/dolostone and microbiallaminites;

– F2: dolomites/dedolomites after preexistent evaporites;– F3: pedogenic limestone and conglomerates.

FACIES ASSOCIATION 1: FOSSILIFEROUS LIMESTONE/DOLO-STONE AND MICROBIAL LAMINITES

This is the principal facies association constitutingthe Units B and C. It consists of calcareous and dolomi-tized bioclastic wackestone-packstone (from fossiliferousmicrites to biomicrites and biopelmicrites), with ostra-cods, discorbids, opthalmidiids, Aeolisaccus kotori, Nezza-

zata cf. convexa and in places, Thaumatoporella (Pl. I/1).In addition, peloids are locally abundant. Bioclastic pack-stone-grainstone (packed biomicrites/biopelmicrites tobiopelsparites) with rich benthic fossil assemblages areobserved along some horizons. Fauna includes miliolids,discorbids, Aeolisaccus kotori, rudists, gastropods, Nezza-zatidae, and Pseudonummoloculina regularis (Pl. I/2).Grainstones (pelsparites-intrapelsparites) with ellipsoidalto round peloids–nodules are locally common (Pl. I/3).Selective secondary porosity, due mainly to gastropodshells dissolution, occurs as well as thin sheet cracks andirregular pore spaces (ped and fenestrae textures).

Microbial laminites occur at many levels and arecharacterized by high-organic content. In places the stro-matolitic laminae are rich in ostracods whose shells areparallel orientated (Pl. I/4).

Desiccation cracks, in-situ brecciation and irregularfenestrae, of bird’ s eyes type with geopetal filling, arevery common (Pl. II/1) witnessing to significant, althougheffemeral subaerial exposure episodes. Microepikarsticcavities, filled with speleotheme-like cement occur in places(Pl. II/2). The former presence of evaporites is impliedby anhydrite and gypsum pseudomorphs (crystals and/ornodules), authigenic idiomorphic quartz crystals anddisseminated pyrite (Pl. II/3). Replacing calcite/dolomitetextures characterized by variation in crystallinity and «pile-of bricks» texture remind preexistent anhydrite (Pl. II/4).

The above facies association is commonly interruptedby pedogenic limestone and conglomerates (see «FaciesAssociation 3»). It has to be noted, that in the upper partof Unit C a thick shale interval (20-50 cm), mineralogi-cally composed of illite, has been detected interruptingthe carbonate sequence. Upon that layer, sediments con-tain abundant intraclasts from the substrata (fig. 2).

Interpretation

On the whole, this facies association witness to very-shallow, low-energy, restricted subtidal to supratidal envi-ronmens, with salinities ranging from nearly normalmarine to hypersaline. It consists of a classical peritidalfacies association, arranged in shallowing-upward cycles.

The rich in benthic fauna assemblage wackestone-packstones witness to a protected shallow subtidal setting(e.g.: low-energy lagoonal environment. Washed pack-stones and grainstones indicate temporary high-energyconditions. Microbial-stromatolitic laminites grew in,and/or close to the shallow lagoons. Intertidal-supratidallaminites are witnessed by loferitic laminae in which theabundance of dissication features suggests significantalthough effemeral subaerial exposures. «Intermittent»subaerial exposures as well as salinity fluctuations mayalso be inferred from the former presence of evaporites.The thick shale interval of Unit C presumably reflects along-lasting exposure during the late Cenomanian. Therich in carbonate intraclasts horizon marks the starting ofsedimentation above this discontinuity (fig. 2).

FACIES ASSOCIATION 2: DOLOMITES/DEDOLOMITES AFTER

PREEXISTENT EVAPORITES

This is the principal facies association of Units A andD. It is characterized by textures assigned to preexistentevaporites, although evaporites are entirely replaced bydolomite or curved rhombic calcite crystals (dedolomite)


(Pl. III/1). Pseudomorphs after nodular and «pile-of-bricks» textures are common. The variation in crys-tallinity and the crystals habit, strongly remind preexis-tent evaporites. Along certain horizons, solution-collapsebreccias, resulting by dissolution of evaporites, occur.Disseminated pyrite, curved rhombic or radial dolomitecrystals are also indices of vanished evaporites. Due tofurther dedolomitization and recrystalization, most evap-orite-related textures have been obliterated.

Thin argillaceous intercalations are common.

Interpretation

Preexistent evaporites are assigned to supratidal con-ditions and «intermittent» subaerial exposure, which pre-vailed during certain time intervals. The argillaceousintercalations mark preexistent erosional surfaces.

FACIES ASSOCIATION 3: PEDOGENIC LIMESTONE AND CON-GLOMERATES

Pedogenic limestone intervenes very often along thestudied stratigraphic section and occur mainly above cer-tain disconformities, representing the result of pedogenicalteration of the previously described peritidal facies. Inthin sections they usually exhibit floatstone textures, withcaliche pisoids (Pl.III/2), meniscus-like cement, clottedmicrite, rhizocretions, alveolar-septal texture, soil glae-bules, black pebbles, nodules, irregular fenestrae, circum-granular cracking, ferroan dolomite/dedolomite, laminarcalcretes, black pebbles and displacive-growth brecciationfabrics. In places, ostracods are common.

Poorly-sorted pedogenic conglomerates (soil breccias)represent an in-situ type of brecciation, due to intensivebrecciation. Relics from the primary deposited carbonate


Plate I - 1) Bioclastic wackestone-packstone (from sparse biomicrites to biomicrites-biopelmicrites) with ostracods, benthic foraminifera andcalcareous algae; 2) Bioclastic packstone- grainstone (packed biomicrites-biopelmicrites to biopelsparites) with a rich fossil assemblageconsisted of benthic foraminifera, rudists and gastropods; 3) Peloidal grainstone (pelsparites-intrapelsparites) characterized by «ped andfenestrae» texture. Ellipsoidal to round peloids-nodules, separated by thin sheet cracks and irregular pore spaces are observed; 4) Stromatolitic-like, bituminous, microbial boundstone. Ostracod-rich laminae occur in-between.– 1) Wackestone-packstone bioclastici (biomicriti-biopelmicriti) con Ostracodi, Foraminiferi bentonici e Alghe calcaree; 2) Packstone-grainstone(biomicriti-biopelmicriti e biopelspariti) fossiliferi. Sono riconoscibili abbondanti resti di foraminiferi bentonici, frammenti di rudiste e gasteropodi;3) Grainstone peloidale (pelspariti-intrapelspariti). Struttura «ped and fenestrae». Si osservano peloidi arrotondati-noduli separati da sottili «sheetcracks» e cavità irregolari; 4) Laminiti stromatolitiche, boundstone di origine algale. Presenti, tra le lamine, sottili intercalazioni ricche in gusci diOstracodi.

facies are still preserved, but the surrounded soil matrixtends to assimilate them (Pl. III/3,4).

Interpretation

The conglomeratic levels, clearly have a pedogenicorigin. Features as caliche pisoids, rhizocretions, alveo-lar-septal texture and black pebbles are very strongindices of this origin.

Facies 3 consists a complex subaerial exposureassemblage of «long-term/terrestrial» type.

According to the exposure index of GINSBURG et alii(1977), the «long-term/terrestrial» exposure correspondsto an exposure index of 100%, and normally is not floodedby marine waters. The terrestrial subaerial exposure ofcarbonate platforms is indicative for relative sea level fall,and can only be produced by allocyclic processes. Duringthis extended exposure the carbonate platform is meteori-cally altered and development of variable pedogenic fea-tures, such as alveolar textures and soil glaebules, are

favoured. Instead, during the «intermittent» subaerialexposure, which characterizes the supratidal and theintertidal environment, time is too short for the develop-ment of pedogenic features and the most common fea-tures are desiccation cracks and bird’ eyes. Therefore, therecognition of intermittent and terrestrial exposure envi-ronments in carbonate platforms is very significant for thereconstruction of the global sea-level fluctuations.

DISCUSSION

The lithofacies associations of the Vitina section, sup-port a flat topography of the Tripolitza zone in Late Ceno-manian, because the depositional environments were notdeeper than the shallow subtidal zone. The studied shal-low-marine deposits probably built up at or close to sealevel, filling accommodation. This resulted in a generallyflat topography, which in turn favoured a more or lessuniform facies distribution.


Plate II - 1) Wackestones with irregular fenestrae, of bird’s eyes type. Note the geopetal internal filling; 2) Wackestones with microepikarsticcavities, filled with speleotheme-like cement; 3) Mudstone with sparse calcite replacement evaporite pseudomorphs; 4) Replacing cal-cite/dolomite textures characterized by variation in crystallinity and «pile-of bricks» texture.– 1) Wackestone. Fenestrae irregolari, di tipo bird’s eyes, con riempimento geopeto; 2) Wackestone. Presenti cavità minute di tipo carsico riempiteda speleotemi calcitici; 3) Mudstone. Cristalli di calcite in sostituzione di preesistenti minerali evaporitici; 4) Calcite/dolomite in sostituzione diminerali evaporitici preesistenti. Struttura «pile-of bricks».

During intermittent subaerial exposure episodes,supratidal conditions prevailed, giving birth to evaporitesformation. Strong evidence of vanished evaporites consistof horizons with solution-collapse breccias and pseudo-morphs after evaporite crystals/nodules and textures.

According to the most recent European sequencechronostratigraphy framework (HARDENBOL & ROBASZYN-SKI, 1998), the Late Cenomanian corresponds to the post-Ce 5-6 interval, and it is well known, that this interval coin-cides with a global sea-level rise perhaps resulted in (HAQ

et alii, 1987). However, in the Upper Cenomanian carbon-ate lithostratigraphic section of Vitina, it has been shown,that most discontinuity surfaces correspond to long-termterrestrial subaerial exposure environment and are markedby pedogenic limestones and conglomerates. On top of thesubaerial exposed facies, subtidal facies are found corre-sponding to transgressive facies. The prevailance of such acomplex subaerial attestation of terrestrial type supports

the fact that during the Late Cenomanian, which is knownto reach the highest sea-level stand of the entire Phanero-zoic, several relative sea-level lowering episodes, of allo-genic origin, took place. Local tectono-sedimentary condi-tions presumably ruled the sea-level fluctuations.

CONCLUSIONS

The sedimentological study of the Late Cenomanianplatform deposits of the Tripolitza zone (Vitina, MainalonMnt, Greece) shows a facies distribution of a classic peri-tidal environment, which undergo to effemeral subaerialexposure episodes. The depositional environment was notdeeper than the shallow subtidal zone supporting a flattopography of the Tripolitza zone in Late Cenomanian.The repeated discontinuities, which correspond to long-lasting and more complex subaerial exposure events wit-


Plate III - 1) Replacive calcite textures consisted of curved rhombic calcite crystals; 2) Pedogenic limestones, with floatstone texture, withcaliche pisoids, rhizocretions and soil glaebules. Note the circumgranular cracking and the meniscus-like cement in-between the pisoids;3) Poorly-sorted pedogenic conglomerates (soil breccias). Carbonate fragments are surrounded by a pedogenic matrix; 4) The soil matrixtends to assimilate the carbonate fragments.– 1) Mosaico calcitico in sostituzione di preesistenti minerali evaporitici. Si notino cristalli di calcite rombici ed arcuati; 2) Calcari di originepedogenetica (floatstone). Pisoliti vadose, rizocrezioni, granuli pedogenetici. Si notino le caratteristiche crepacciature circumgranulai ed il cementoa menisco presenti tra le pisoliti vadose; 3) Conglomerati pedogenetici (soil breccias). Frammenti carbonatici circondati da una matrice di originepedogenetica; 4) Matrice di origine pedogenetica che tende ad assimilare i frammenti carbonatici.

ness to long-term/terrestrial intervals. This supports inter-vening sea-level lowering intervals, of allogenic origin, inthe frame of the general global sea-level rise of the LateCenomanian.

ACKNOWLEDGEMENTS

The authors are grateful to Professor Lucia Simone for her sub-stantial comments and insightful remarks, that helped us to improveour manuscript significantly. We also wish to thank an anonymousreferee for his critical review.

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ZAMBETAKIS-LEKKAS A., POMONI-PAPAIOANNOU F. & ALEXOPOULOS

A. (2007) - New stratigraphic and palaeogeographic data from theMesozoic strata of the Tripolitza platform in central Crete. Eviden-ce of subaerial exposures during Albian-Early Cenomanian. Helle-nic Journal of Geoscienses, 42, 7-18.


Received 00 ..... 0000; revised version accepted 00 ..... 0000.

facies associations of the late cenomanian carbonate ...users.uoa.gr/~pavlakis/pomonipaper01.pdf ·...

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