Introduction

After a period of no deposition during the Aptian andthe Albian, with a new transgressive cycle, land mass-es of Jurassic ophiolites (nowadays in western Serbia)were flooded with a shallow to moderately shallow sea.Although extensively eroded since, Cretaceous depo-sits that were formed during this transgressive cyclecould be found on numerous outcrops in western Ser-bia. The most extensive exposure among these outcropsis located in the vicinity of Mokra Gora and occupiesthe Beli Rzav and Kamešina Valleys with their tributar-

ies. The lower portion of these deposits near MokraGora Village was previously studied and described asthe Kotroman Formation (BANJAC et al. 2008 and ref-erences therein).

Previous Studies

The general consensus among the stratigraphiccommunity was that the Mokra Gora deposits are Up-per Cretaceous in age. However, much debate wasinvolved to the question of the age of specific strati-

Paraseqences in the Kotroman Formation, western Serbia

NENAD BANJAC1 & DIVNA JOVANOVIĆ2

Abstract. An attempt was made to describe two parasequences separated within the sediments of theKotroman Formation at the Mokra Gora Village in western Serbia. The whole formation, of Albian–Ceno-manian age, in some general characteristics corresponds to tidal flats, some of which were described in theliterature (LARSONNEUR 1975), and the sediments were compared with ones from recent tidal flat environ-ments. The heterogeneous composition of the Kotroman Formation influenced different authors to describeseveral non-synchronous and incomparable superpositioned packages. The parasequences were investigatedin the attempt to correlate them with the stratigraphic age of the members. The parasequences were formedduring the Albian transgression and represent a gradual deepening of the wider area. Well-developed floodingsurfaces with significant deepening indicated retrogradational stacking of certain transgressive system tractsand reflect landward movement of the shoreline, indicating a gradual sea level rise.

Key words: Parasequences, Kotroman Formation, palaeontology, sedimentology, Albian–Cenomanian,Mokra Gora, western Serbia.

Апстракт. У раду су описане две парасеквенце уочене у седиментима формације Котроман код Мо-кре горе у западној Србији. Цела формација, албско-ценоманске старости, у неким својим општимкарактеритикама, одговара тајдалној равни, какве су већ описане у литератури (LARSONNEUR 1975), ањени седименти су упоредиви са творевинама рецентних тајдалних равни. Хетерогена грађа форма-ције Котроман условила је да више аутора описује неколико различитих суперпозиционих пакета којисе међусобно не могу поредити. У раду су описане парасеквенце и представљена је њихова страти-графска припадност. Парасеквенце су формиране током албске трансгресије и настале су услед по-степеног продубљавања на ширем простору. Површине плављења са маркатним продубљавањемуказују на ретроградациони трансгресивни тракт и представљају последицу сталног издизања нивоамора уз постепено померања обалске линије ка копну.

Кључне речи: Парасеквенце, Формација Котроман, палеонтологија, седиментологија, алб–цено-ман, Мокра Гора, западна Србија.

GEOLO[KI ANALI BALKANSKOGA POLUOSTRVA

ANNALES GÉOLOGIQUES DE LA PÉNINSULE BALKANIQUE72 63–69 BEOGRAD, decembar 2011

BELGRADE, December 2011

1 Department of Geology, Faculty of Mining and Geology, University of Belgrade, Kamenička 6, P. O. Box 162, 11000Belgrade, Serbia. E-mail: banjac@afrodita.rcub.bg.ac.rs

2 Geological Institute of Serbia, Rovinjska 12, 11000 Belgrade, Serbia. E-mail: djdivna@gmail.com

DOI: 10.2298/GABP1172063B

graphic sections. The Mokra Gora deposits were firstdescribed by ŽUJOVIĆ (1893), as carbonates of Seno-nian age. The author sporadically mentioned numer-ous hippuritids and abundant fossil gastropod associ-ations. The following works (ŽIVKOVIĆ 1905, 1907;PETKOVIĆ 1925; AMPFERER1928; MILOVANOVIĆ 1933)confirmed Mokra Gora deposits as Senonian in age,locating the whole sequence as analogues to the Go-sau Beds in Austria. The determination was based onmacrofossil fauna assemblages with: Pyrgulifera pi-chleri, P. accinosa, P. lyra, P. striata, Glauconia ke-fersteini, G. renauxi, G. coquandi, Natica bulbiformis,N. lyrata, Hippurites gosaviensis, Radiolites lusitani-cus, etc. However, LÓCZY (1924) indicated that the sed-iments are Upper Cretaceous in age, more specificallyCenomanian, Turonian and Senonian, based on themacrofossil fauna: Acanthoceras mantelli, Puzosia aff.gaudama, Biradiolites affilaensis, etc. MILOVANOVIĆ

(1935) just mentioned deposits from the UpperCenomanian to the Upper Campanian age. MITROVIĆ

(1966), MITROVIĆ et al. (1989), confirmed this agebased on abundant echinid assemblages with numerousrepresentatives of the Epiaster and Hemiaster genera.

PEJOVIĆ & RADOIČIĆ (1971, 1973, 1974) and RADO-IČIĆ (1984), placed the whole Mokra Gora series as theCenomanian, Turonian and older Senonian. Accordingto these authors, the sandy and marly carbonate por-tion of the local stratigraphic column, “tens of metersabove the weathering crust” RADOIČIĆ (1984, p. 136.),is characterized by mid-Cenomanian microfauna:Aeolisacus inconstans, Ovalveolina maccagnae andRhapidionina laurinensis. Therefore, the authors con-cluded that the lower-most, palaeontologically sterilebasal section can be recognized as the Albian stage.The upper portion of the local stratigraphic column isrepresented by marly limestone with abundant ostrei-ds, grypheas and inoceramids, as well as pelagic mi-crofossils of the Pithonella ovalis, Hedbergella-Tici-nella group, which indicate the lower Turonian stage.However, upper Cenomanian age was accepted afterlater revision of the beds with Cisalveolina fraasi,(RADOIČIĆ 1984, 1995).

The uppermost member of the stratigraphic columnis represented with massive limestone bearing hippu-rites and gastropods of Turonian age.

The Albian–Cenomanian age of the Mokra GoraSeries was confirmed in the works of BANJAC (1994,1994a, 2000). The author reported mollusc fauna ofAlbian–Cenomanian and Turonian age, although someof the specimens, e.g., Paraglauconia lujani, is knownfrom Aptian deposits. DULIĆ (2003), described it as theAlbian–Cenomanian palynomorph association fromthe Mokra Gora Series. The same age was confirmedby JOVANOVIĆ et al. (2004) based on the microfaunaassemblage, as well as BANJAC et al. (2007) based onthe gastropod assemblage. RADOIČIĆ & SCHLAGINTWEIT

(2007) at the Mokra Gora Series established a newspecies Neomeris mokragorensis of Albian age. It must

be noted that lower portion of the stratigraphic columnis described as deposits of Barremian age (NIRTA et al.2008; MENA et al. 2008).

Lithostratigraphic members

Due to heterogeneous composition of the MokraGora Series, authors described several non synchro-nous and incomparable superpositioned packages.LÓCZY (1924) differentiated five packages. (1) Thefirst one consists of conglomerates and sandy hori-zons with oolith iron nodules, (2) the second withmarly to sandy limestone, (3) the third with shaly andsandy limestone. The fourth package (4) is represent-ed by greyish to yellowish fragile marl with largemolluscs and bivalve fossil specimens, whereas thefifth package (5) is represented by massive reef lime-stone. MILOVANOVIĆ (1933) also differentiated 5 pack-ages: (1) basal, represented by conglomerate, reddishquartzite and iron rich bearing schist; (2) tabular marland limestone, which gradually become sandy lime-stone and sandstone; (3) lower package of sandstone,sandy limestone and marls with abundant associationsof gastropods and most commonly the genus Pyrgu-lifera and (4) upper package of sandy limestone andmarl with associations of gastropods, bivalves andechinoids. The uppermost package (5) is representedwith massive reef limestone with abundant rudistfauna. This subdivision was generally accepted in theworks of DRAKULIĆ & DEDIĆ (1963) and FOTIĆ (1965).

PEJOVIĆ & RADOIČIĆ (1971, 1973, 1974), RADOIČIĆ

(1984) described the biostratigraphic characteristics ofthe Mokra Gora Series, with three main levels: (1) thebasal clastites, (2) carbonates with marls and (3) shal-low water reef limestone. The lowermost level (1),transgressively overlying serpentine or a weatheringcrust, is represented by conglomerate, conglomeraticsandstone and sandstone lacking any fauna. The over-all height is around 50 m. The authors emphasized theextremely heterogeneous composition and thickness ofthis level. The following level (2) was named by theauthors as Carbonaceous or Pelagic beds, and bears twomembers of lower rank, i.e., (2a) sandstone, marl andcarbonaceous deposits (150–200 m thick) and (2b)marly-carbonaceous deposits (150–200 m. thick). Theuppermost level (3) consists of massive limestonewith hippurits of Turonian age. A similar partitionwith three principal units was presented by MOJSI-LOVIĆ et al. (1978) and OLUJIĆ et al. (1986). NIRTA etal. (2008) and MENA et al (2008) explained the litho-logic characteristics of the Mokra Gora Series,describing two units (named A and B), which reflecttwo main deepening-shallowing cycles. These unitscorrespond to the levels 1 and 2, respectively, suggest-ed by PEJOVIĆ & RADOIČIĆ (1971, 1973, 1974) andRADOIČIĆ (1984). The authors also mentioned, but didnot study, the third unit (named C), which corresponds

NENAD BANJAC & DIVNA JOVANOVIĆ64

to level 3 of massive limestone with hippurites sug-gested by PEJOVIĆ & RADOIČIĆ (1971, 1973, 1974).

Within an analysis of the Cretaceous deposits ofwestern Serbia, JOVANOVIĆ et al. (2004) separatedthree levels.

The first is basal terrigenous sandy series with no-dular biomicrite. The biocomponent is representedwith rare fragments of microflora and microfauna inaddition to mollusc detritus. The frequent charophytsand ostracods of the same age indicate the presence ofan intermittent freshwater environment at the sameperiod. Rich fossil assemblages can be found in theuppermost section of the Kotroman Formation.

The next level is the Pelagic Series, composed ofthin-bedded marly limestone. These are fine laminat-ed biomicrite with an abundant alevritic fraction andcentimetre thick beds of bioclastic marl, bioclasticpackstone, sometimes with accumulations of thinshell fragments. They are commonly alternating withthin marly layers.

The third level, uppermost portion of the MokraGora Series, consists of massive carbonates with hip-purits and gastropods of Turonian age.

The first of the aforementioned, the so-called Basalterrigenous sandy series, was described by Banjac et al.(2008), and proposed as the Kotroman Formation. TheFormation consists of clastic deposits in the lower partand limestone beds in the upper part of the stratigraph-ic column. The lower limit is a sharp transgressiveboundary with serpentinite or a few meters thick weath-ering crust, while the upper limit is a blunt transition tothe so-called Hemipelagic Series. Three separate mem-bers were distinguished in the Kotroman Fm.: theKamišna Mb, the Uroševići Mb and the Jatare Mb.

Parasequences

An attempt was made to describe the two parase-quences separated within the Uroševići Member ofthe Kotroman Fm. Their base is the upper portion ofthe Kamišna Mb. while they are overlain by the Jatare

Mb. The whole Kotroman Fm. in some general waycorresponds to a tidal flat, some of which weredescribed in literature (LARSONNEUR 1975), and thesediments were compared with those from the envi-ronment of recent tidal flats. It must be noted that thelow latitude (less than 30° N) position of the area dur-ing the Upper Cretaceous influenced not only thepresence of siliciclasite, but also of carbonates withcharacteristics of the carbonate shelf system of thewhole formation. The section with the described para-sequences is shown in Fig. 1.

Kamišna Member

At the investigated locality, the Kamišna Memberis not exposed at its whole thickness. In its lower seg-ment, transgressive extra-formational oligomict con-glomerate can be observed. Fragments of serpentiniteand chert are deposited within a sandy or silty matrix.

Iron-rich, dark green chamosite ooides and serpen-tinite particles can be frequently found in the con-glomerate fragments. The grains are cemented withcalcareous or clay-ironstone cement. The describedsediments correspond to the gravel initially depositedbelow the low-water tide level (LARSONNEUR 1975).

In the upper parts of the stratigraphic column, thesesediments increasingly interchange with iron-rich sand-stone characterized by well-rounded pyritised grainsand fragments of serpentine, without any fossils. Thedeposits gradually transform to sandstone containingmore than 25 % fine-grained rock fragments, predomi-nantly pyroxene and spinel clasts. This coarse- to fine-grained loose dark grey sandstone is present in the main

portion of the Basal Member. Small cherty fragmentsas well as sand particles of different sizes are bound byclayey or limonitic red or brown cement.

The described sediments correspond to gravellysand which was deposited on about the low-water tidelevel (LARSONNEUR 1975).

Paraseqences in the Kotroman Formation, western Serbia 65

Fig. 1. Parasequences at the Kotroman locality. Legend: FS1 - Flooding surface 1, FS2 - Flooding surface 2.

The iron-rich sandstone dominates in the upperportion of the Kamišna Mb. However nodular clasticlimestone interbedded with yellowish thin marl occursin this portion. The nodular limestone is representedby biomicrite, floatstone and wackestone, enclosed inan intimate mixture of clay and carbonate. Clasts ofserpentine, pyroxene and quartz mixed with scarcemollusc shell fragments are found in a fine grainmicrosparite and clayey matrix. Extremely small crys-tals of quartz, pyrite and hematite can frequently befound in these deposits.

The quantity of the bioclastic fragments increasesin the upper horizons, and rock gradually changes tobioclastic wackestone, packestone and floatstone,with sometimes large clasts. The characteristics of therock resemble storm beds. The bioclasts are represent-ed with numerous fragments of gastropods, bivalvs,and ostracods. Floral remnants, such as fine dispersedplant particles and fragments of branches and treetrunks, are common. In addition, bisect particles ofconifers, dominated by Pinus and rarely Podocarpusand Cedrus can be found.

The iron-rich sandstone of the upper portion of theKamišna Mb. represents shallow water facies. It cor-responds to biogenic sand and biogenic fine sandwhich was deposited about the high-water tide level(LARSONNEUR 1975).

Uroševići Member – Parasequence 1

Within the Uroševići Mb., two parasequences havebeen described, with an attempt to correlate them withstratigraphic age of the member (BANJAC et al. 2008).

The lowermost sediment of the Uroševići Mb. (with-in Kotroman Fm.) is represented with an almost onemeter thick bed of sandy reddish nodular limestonewith bivalve and gastropod shell fragments. Its lowerboundary represents the flooding surface (FS1) thatmarks the base of a parasequence with abrupt contact.Sandy reddish nodular limestone lying directly on topof relatively shallow iron-rich sandstone located belowthe surface. The frequent appearance of small-scaleerosion can be observed at this surface (Fig. 2).

In the following portion of the stratigraphic col-umn, nodular limestone is frequently interbedded withthin layers of marl and siltstone.

The thin section of the reddish nodular limestoneindicated bioclastic wackestone with frequent fossilshell fragments. Samples from the upper portion ofthese deposits revealed packestone, floatstone, rud-stone and rarely fine-grained sandstone. The fossilcontent is represented with mollusc fragments, insome places with abundant gastropod and bivalveaccumulations found in the cm-scale lenses of calciru-dite and calcarenite. The mollusc shells frequentlycontain geopetal fillings. These beds also contain rareostracode remnants, as well as gyrogonyts and cha-

ropohyte remnants, which indicate intermittent freshwater influxes. In addition, the algae Radiocicelapsessp. and Hemicyclamina sigali MAYNC can be found.

The microfauna assemblage consists of codiaceangrains and Radoicicelapses sterni RADOIČIĆ, Nezzaza-tinella cf. picardi (HENSON), Hemicyclamina sigaliMAYNC, Salpingoporella urladanasi CONRAD, PEY-BERNES & RADOIČIĆ, Aeolisacus sp. and Glomospirasp. The macrofauna is represented by gastropod frag-ments (Cassiope sp.).

Samples from the upper portion of the parase-quence revealed an increase of fine-grained sandsto-ne, gradually transforming to lithic sandstone. Clastsare represented with quartz, chert, pyroxene, serpen-tine, peridotite and siliceous rocks in spary cement ora microsparitic matrix. Birds-eye structures as well asfenestrated fabrics, which can be observed in the thinsection, indicate a shallow environment with spo-radic exposure to open air, i.e., deposition at the highwater tide level. The general characteristics of thefine-grained sandstone shows a gradual shallowingwhich is terminated with a sudden contact. Relativelydeeper nodular limestone is situated on top of theshallow fine-grained sandstone located below thesurface. Small scale erosion can be observed at thissurface (FS2), similar to one at the previous floodingsurface (FS1).

Uroševići Member – Parasequence 2

The lower portion of the second parasequence isrepresented with an approximately 20 cm thick bed ofnodular limestone with mollusc shell fragments. Itslower boundary is designated as a second floodingsurface (FS2) that marks the base of the second para-sequence. The nodular limestone of this parasequenceis fossiliferous packestone and wackestone withpeloidal and biogenic intraclasts in a micritic and mi-crosparitic matrix.

NENAD BANJAC & DIVNA JOVANOVIĆ66

Fig. 2. Flooding surface at the top of the Kamišna Mb.

In the upper portion of the parasequence, the nodu-lar limestone alternates with ophiolithic coarse-grained reddish sandstone.

Marly bioclastic packestone creates the next level inthe parasequence. Gastropod or bivalve shells can fre-quently be found, especially in the marly beds betweenthe thicker limestone beds. At some levels, there is atransition to wackestone, i.e., biomicrite with unsortedangular shell fragments deposited within a microcrys-

talline calcite matrix. Besides shell fragments, charo-phyte girogonits and ostracods can be found, indicat-ing intermittent fresh water influx. It is followed by

decayed, lumpy limestone thatis characterized by the pres-ence of thin mollusc shellfragments. It is predominantlybiomicrite with sporadic fora-minifera and abundant ironmatter. At some places withinthese limestone beds, the shellaccumulations indicate stormbeds. Bioclastic wackestone,as well as bioclastic rudstonecan also be found at this por-tion of the parasequence. Inthe upper portion, a blunt tran-sition to marly mudstone canbe observed.

Fine-grained sandstone re-presents the uppermost por-tion of this parasequence. Thedescribed sediments corre-spond to biogenic gravellysand to biogenic sand whichwas deposited between lowand high water tide levels.(LARSONNEUR 1975).

Jatare Member

The fine-grained sandstoneof the Uroševići Mb. is over-lain by thin-bedded nodularbioclastic limestone belongingto the third member, the JatareMb. Calcareous and silty marl-stones in some places containabundant microfauna associa-tions, which are representedby: Aeolisacus inconstans RA-DOIČIĆ, Ovalveolina macca-gnae DE CASTRO and Rhapidi-onina laurinensis DE CASTRO.Macrofauna was discovered atnumerous localities, someti-mes forming coquina beds. It isrepresented by mollusc frag-ments: bivalvs Amphidonte co-nicum (SOWERBY), Ostrea cal-limorphe COQUAND and O. cu-

nabula SEELEY, and the gastropods Pseudomesaliateniucostata (HACOBJAN), P. multicostata (HACOBJAN),Pirenella cf. levadhiae KOLLMANN, Paraglauconialujani (DE VERNEUIL & COLOMB), Bicarinella bicarina-ta (PČELINCEV) and Cassiope kotromanensis BANJAC.Thin-bedded nodular bioclastic limestone with the

Paraseqences in the Kotroman Formation, western Serbia 67

Fig. 3. Stratigraphic column with the described Parasequences.

aforementioned association of fauna corresponds tosediments deposited at a subtidal shelf or outer shelfwith increased carbonate production. In the upper por-tion, they gradually transfer to the thin-bedded, marlylimestone of the so-called hemipelagic series.

Conclusions

An attempt was made to investigate the presence ofparasequences in the Cretaceous deposits known asthe Kotroman Formation according to type localityand type section at the Kotroman Village in westernSerbia.

The investigations of the sediments at the Kotromanlocality imply two parasequences within the UroševićiMb.: Parasequence 1 and Parasequence 2. The parase-quences were formed during the Albian transgressionand represent a gradual deepening of the wider area.Well-developed flooding surfaces with prominentdeepening, indicated to retrogradational stacking ofcertain transgressive system tract and reflect the land-ward movement of a shoreline. The beds overlying theUroševići Mb. indicate a new rise in the relative sealevel. They are represented by thin-bedded nodular bio-clastic limestone belonging to the Jatare Mb.

The insufficient data does not allow the results tobe compared with the eustatic sea level curve (HAQ etal. 1987). It can only be approximately estimated(based on fossil age) that the described parasequencesbelong to the earliest Supercycle of the Upper Zuni Aset (UZA 1).

Acknowledgments

We are very thankful to PLATON TCHOUMATCHENCO

(Geological Institute, BAS, Sofia), as well as an anonymuscritic who reviewed the paper. The work was supported bythe Ministry of Education and Science of the Republic ofSerbia (Project No. 176015).

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Резиме

Парасеквенце формације Котроман,западна Србија

У седиментима формације Котроман код Мокрегоре у западној Србији истражене су и описане двепарасеквенце, формиране током албске трансгре-сије и настале услед постепеног продубљавања на

ширем простору. Цела формација, албско цено-манске старости, по својим општим карактеристи-кама, одговара тајдалној равни, какве су већописане у литератури (LARSONNEUR 1975), а њениседименти могу да се упореде са творевинамарецентних тајдалних равни.

Хетерогена грађа формације Котроман усло-вила је да више аутора описује неколико различи-тих суперпозиционих пакета. У већем броју стари-јих радова (ŽIVKOVIĆ 1905, 1907; PETKOVIĆ 1925;AMPFERER 1928; MILOVANOVIĆ 1933) наводи сестратиграфска припадност сенону, док се каснијејавља мишљење о припадности албу, ценоману итурону (MILOVANOVIĆ 1935; MITROVIĆ 1966; MITRO-VIĆ et al. 1989; PEJOVIĆ & RADOIČIĆ 1971, 1973,1974; RADOIČIĆ 1984). У већини савремених радованаводи се припадност алб-ценоману (BANJAC 1994,1994a, 2000; DULIĆ 2003; JOVANOVIĆ et al. 2004;BANJAC et al. 2007; RADOIČIĆ & SCHLAGINTWEIT

2007), а само изузетно и припадност старијим ка-товима (NIRTA et al. 2008; MENA et al. 2008).

У оквиру члана Урошевићи формације Котро-ман, издвојене су две парасеквенце формиранетоком албске трансгресије на ширем простору. Ос-нову им чине пешчари и конгломерати члана Ка-мешина, таложени у условима плитке воде. Изнадњих се запажа јасна површина плављења (FS1)која означава драстичан прекид у седиментацији ипочетак прве парасеквенце.

Прва парасеквенца обележена је квргавимкречњацима, са честим фрагментима фосила, којисе местимично смењују са финозрним пешчарима.Фрагменти љуштура мекушаца који се налазе у се-дименту често садрже геопеталне испуне. Поне-кад се у седименту налазе и фрагменти остракодакао и гирогонити и остаци харофита.

Друга парасеквенца обележена је као и прет-ходна, јасном површином плављења (FS2), изнадкоје се налазе квргави кречњаци, пакстон и вак-стон са фрагментима фосилне фауне у микритскојоснови. У вишим деловима јавља се грубозрницрвенкасти пешчар. Парасеквенца се завршава ја-сном површином плављења којом је одвојена одтанкослојевитих квргавих кречњака члана Јатаре.

Јасно дефинисане површине плављења на гор-њој и доњој граници сваке парасеквнце са мар-катним продубљавањем током развоја парсеквенцеуказују на ретроградациони трансгресивни тракти постепено померање обалске линије у правцукопна. Танкослојевити квргави кречњаци који ле-же преко горње границе члана Урошевићи, указујуна ново издизање нивоа мора.

Скроман обим података није нам дозволио по-ређење резултата са кривом промене нивоа мора(HAQ et al. 1987). Могуће је само приближно пред-поставити на основу старости детерминисане па-леофауне да описане парасеквенце припадају нај-старијем суперциклусу сета Upper Zuni A 1 (UZA 1).

Paraseqences in the Kotroman Formation, western Serbia 69