P53_ copertina_R_OK C August 20-28,2004 Florence -Italy

Field Trip Guide Book - P53 J. Tišljar, I.Vlahovi S. Šoštari D. Mati V. Jurak,I.Guši Z. Barjaktarevi Associate leaders: Post-Congress M. Jura Leaders: RECENT TIME AND FACIES FROMPERMIAN TO PLATFORM, ENVIRONMENTS MESOZOIC CARBONATE ADRIATIC-DINARIDIC 32 Volume n°5-fromP37toP54 GEOLOGICAL CONGRESS nd INTERNATIONAL č č i ec, A.Mezga,T. Paviša,S.Šestanovi ć ć , LadislavPalinkaš -Borojevi ć ć , R.Buljan,S.Bergant, , L.Marjanac,T. Marjanac, ć ć , S.Strmi ć , J.Sremac, P53 3-06-2004, 11:34:18 ć , The scientific content of this guide is under the total responsibility of the Authors

Published by: APAT – Italian Agency for the Environmental Protection and Technical Services - Via Vitaliano Brancati, 48 - 00144 Roma - Italy

Series Editors: Luca Guerrieri, Irene Rischia and Leonello Serva (APAT, Roma)

English Desk-copy Editors: Paul Mazza (Università di Firenze), Jessica Ann Thonn (Università di Firenze), Nathalie Marléne Adams (Università di Firenze), Miriam Friedman (Università di Firenze), Kate Eadie (Freelance indipendent professional)

Field Trip Committee: Leonello Serva (APAT, Roma), Alessandro Michetti (Università dell’Insubria, Como), Giulio Pavia (Università di Torino), Raffaele Pignone (Servizio Geologico Regione Emilia-Romagna, Bologna) and Riccardo Polino (CNR, Torino)

Acknowledgments: The 32nd IGC Organizing Committee is grateful to Roberto Pompili and Elisa Brustia (APAT, Roma) for their collaboration in editing.

Graphic project: Full snc - Firenze

Layout and press: Lito Terrazzi srl - Firenze

P53_ copertina_R_OK D 3-06-2004, 9:50:12 Volume n° 5 - from P37 to P54

32nd INTERNATIONAL GEOLOGICAL CONGRESS

ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME

AUTHORS: M. Juračić 1, Ladislav Palinkaš 1, Z. Barjaktarević 1, R. Buljan 3, S. Bergant 3, V. Jurak 2, I. Gušić 1, L. Marjanac 4, T. Marjanac 1, D. Matičec 3, A. Mezga 1, T. Paviša 3, S. Šestanović 5, S. Šoštarić-Borojević 1, S. Strmić 1, J. Sremac 1, J. Tišljar 2, I. Vlahović 3

1 Faculty of Natural Sciences, University of Zagreb - Croatia 2 Mining-Geology-Petroleum Engineering, University of Zagreb - Croatia 3 Institute of Geology, Zagreb - Croatia 4 Croatian Academy of Sciences and Arts - Croatia 5 Faculty of Civil Engineering, University of Split - Croatia

Florence - Italy August 20-28, 2004

Post-Congress P53

P53_R_OK A 3-06-2004, 10:01:24 Front Cover: Cliffs on DugiotokIisland (Central Dalmatia), made up of Senonian dolomitic limestones.

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Leaders: M. Juračić, Ladislav Palinkaš Associate Leaders: Z. Barjaktarević, R. Buljan, S. Bergant, V. Jurak, I. Gušić, L. Marjanac, T. Marjanac, D. Matičec, A. Mezga, T. Paviša, S. Šestanović, S. Šoštarić-Borojević , S. Strmić, J. Sremac, J. Tišljar, I. Vlahović

Marco Polo from Istria to Dubrovnik, primarily with short excursions on the mainland by bus. Mladen Juračić and Ladislav Palinkaš

I have not told a half of what I Introduction to the Adriatic saw since nobody would have Carbonate Platform believed me. Ivo Velić, Josip Tišljar, Igor Vlahović, Marco Polo, world traveler, born Dubravko Matičec and Stanislav Bergant on the island of Korčula The ancient Adriatic Carbonate Platform, which represented a part of the so-called Mediterranean Introduction Seuill (Dercourt et al., 1993), was formed during The Mesozoic Adriati-Dinaridic carbonate the Mesozoic Tethyan realm. platform, a unique geological formation Due to the complex geological history of the developed along the passive continental margin platform area, especially the signifi cant post- of Gondwana, stands among other similar depositional tectonics, there are different units in the world as a very representative opinions among Croatian geologists concerning example, owing to the size and diversity of two important issues: its name and its its sedimentary facies. It stretches along the stratigraphic range. present Adriatic coast as the External Dinarides, It is very important to discuss these questions known also as the High Karst Zone. It is a sepa≠rately to avoid the confusion of hitherto part of the Alpine-Himalayan orogenic belt, discussions, i.e.: whose existence started in Permian times and (1) to try to fi nd the best designation for the terminated in the Paleogene, and then uplifted platform, and in Neogene times. Interesting phenomena (2) to determine its most appropriate related to karst geomorphology owe their stratigraphic range. names, used in international karst terminology, to local toponyms, such as “doline’ and “polje”. Name of the platform Even the term “karst” came after kras or krš. A The most important issue for the designation of great number of points of interest are situated the platform is enabling a clear differentiation on the pearl of the Adriatic islands, inhabited between palaeogeographic relationships during since prehistoric time by fi shermen, peasants, the platform’s existence in the Mesozoic, and and sailors, who dwelt in small villages with the present structural pattern of the Dinarides picturesque architecture. Fascinating scenery of mountain belt formed during the Tertiary the white rocky coast, with garlands of olives, tectonic cycle. The Dinarides, which link the vineyards, and a drapery of conifers around Southern Alps with the Albanides, Hellenides, old stony villages, embraced by the emerald and Taurides, are composed of two genetically green-blue water of the Adriatic, gives a visual different parts: the Outer (External) Dinarides joy to the geological and cultural program. The along the Adriatic Sea, composed mostly of relics trip is not focused on sedimentology exclusively. of the carbonate platform and its foundation, and It will show some very special sites, including the Inner (Internal) Dinarides, situated between dinosaur tracks; carbonate platform foundations the Outer Dinarides and the Pannonian Basin, Volume n° 5 - from P37 to P54 n° 5 - from Volume or distractions; recent carbonate deposition composed of passive and active continental under temporal climate conditions; one of the margin rocks, including ophiolites. huge karst springs feeding the sunlight green Among numerous designations used for the river, river delta, and marsh-lands in a young carbonate platform deposits outcropping in the immature karst topography; civil engineering area of the Outer Dinarides studied over the achievements; and national parks with unique last few decades, the most frequent in the recent variety of fl ora and fauna. The trip will involve geological literature are the Dinaric Carbonate travelling by boat along the coast and islands Platform, Adriatic–Dinaric Carbonate Platform

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura Platform (notshown).AfterVeli (AdCP), theApulianCarbonatePlatform(ApCP),andApenninic Carbonate and the formation oftheAdriaticBasin(AB),andMolise–Lagonero Basin(notshown), (2), whichwaspartlydisintegratedduringtheLateLias,resulting inthe Apulian Promontory wasseparated,andahugeisolatedplatformformed the northernGondwanamargin; duringthisevent,theAdriaMicroplate or rifting, thestudyarea represented apartoftheepeiric platformlocatedalong separation oftheAdriaticCarbonatePlatform:(1)untilMiddleTriassic Figure 1.1-Schematicillustrationshowingthemaineventsbefore the fi nal separationandisolation(3)oftheAdriaticCarbonatePlatform č i ć , LadislavPalinkaš ć etal.(2003). fl (Tertiary limestones, overlying deposits magmatic rocks), and small occurrences of sedimentary rocks and and earliestJurassic (Palaeozoic, Triassic, stricto carbonate platform belong tothestudied of rocks whichdonot a signi Dinarides, there are area. EvenintheOuter the InnerDinarides which are locatedwithin of thehighestpeaks, including almostall with theplatform, genetically connected deposits whichare not a large proportion of mountain beltcomprises the Dinaridesasa – asalready mentioned, future. disintegration farinthe would beformedbyits mountain belt,which be namedafterthe way, theplatformwould on theplatform.Inthis carbonate deposition tens ofMaafterthelast that tookplaceseveral uplifted intheevents – theDinarideswere issues: several problematic unavoidably incorporates disintegration, but formed bytheplatform’s the mountainbelt geographically depicts the nameofplatform The term“Dinaric”in Platform. Carbonate the Adriatic Carbonate Platform)and (or Adriatic–Dinaridic ysch deposits,coarse- .: underlyingrocks fi cn amount cant 3-06-2004, 10:01:58 sensu ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

grained carbonate clastics – Jelar breccia and The stratigraphic range of the Promina deposits, isolated Neogene fresh- the platform water basins, and Quaternary cover). Concerning the second issue – that is, the – the term “Dinaric” primarily represents a stratigraphic range of the Adriatic Carbonate structural and/or geomorphological term, and Platform as an autonomous entity – the most its usage for a palaeogeographical unit might important point is to defi ne this huge carbonate cause confusion in communication. body and make it palaeogeographically A combined term Adriatic–Dinaric Carbonate recognizable. Although the Outer Dinarides Platform (or Adriatic–Dinaridic Carbonate comprise carbonate deposits of a wider Platform) introduces, in our opinion, besides stratigraphic range (from the Carboniferous the previously mentioned shortcomings of the to the Eocene), only a part of this succession term “Dinaric”, an additional problem, since this belongs to the Adriatic Carbonate Platform name might be confused with a concept of Herak sensu stricto, i.e. to the spatially-defi ned isolated (1986), who proposed a hypothesis where two shallow water platform. different platforms existed, separated by a deep- In the wider sense, the entire sequence of Upper marine area from the Late Triassic to the Eocene Palaeozoic, Mesozoic, and Palaeogene carbonates (named the Adriatic and Dinaric Carbonate of the Karst Dinarides has been included into the Platform). Adriatic Carbonate Platform sensu lato (Tišljar Therefore, we consider that the best term is the et al., 1991; Velić, 2000) or Adriatic–Dinaric Adriatic Carbonate Platform, since the term Carbonate Platform sensu lato (Pamić et al., 1998), “Adriatic”: since the entire sequence was deposited on – fi ts well geographically; since the remains of carbonate platforms of different types (an epeiric the platform are situated in the belt stretching carbonate platform during the Palaeozoic and along the NE Adriatic coast, and a signifi cant Lower to Middle Triassic, an isolated carbonate part of the former platform is covered by the platform during the Late Triassic to the end of the present Adriatic Sea. The name “Adriatic” is Cretaceous, and on carbonate ramps during the “free” for use, because the platforms located Palaeogene). However, if we defi ne this platform along the SW Adriatic coast have their own sensu stricto (as a specifi c palaeogeographical names – the Apulian and Apenninic Carbonate entity, representing a completely isolated, Platforms. intra-oceanic, carbonate platform, surrounded – its temporal dimension fi ts perfectly; the by other separated carbonate platforms formed disintegration of the Adria Microplate on the same foundation), its stratigraphic range (Apulian Promontory) in the Late Lias caused should be signifi cantly reduced to include the formation of the precursor of the present only a part of the Mesozoic deposits. In this Adriatic Sea, the Adriatic Basin, and in this way, the defi ned platform sensu stricto would, way, the separation of the newly formed nevertheless, include the major part of the carbonate platforms: Adriatic, Apulian, and carbonate succession of the Outer Dinarides. Apenninic. Until the Middle Triassic, the area of the future – it cannot cause confusion between the Adriatic Carbonate Platform represented carbonate platform, and the result of its a part of the northern Gondwana margin, disintegration; the Mesozoic Adriatic which was characterized by the deposition of Carbonate Platform fi nally disintegrated in the siliciclastics and carbonates on the carbonate Tertiary, and incorporated as the SW part of platform of the epeiric type. During the Middle P37 to P54 n° 5 - from Volume the Dinarides mountain belt. Triassic, disintegration of the foundation and Considering the abbreviation of the platform eventual separation of the Adria Microplate name, the “AdCP” is proposed instead of the (or Apulian Promontory) took place, resulting usually used “ACP”, to avoid confusion with in the formation of a huge shallow water body the same abbreviation commonly used for the within the Tethyan realm. However, although Apenninic Carbonate Platform (Fig. 1.1). the thick Upper Triassic alter≠nation of early- and late-diagenetic dolomites (regionally known as the Main Dolomite – Hauptdolomit

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura general maybede Carbonate Platform. Although thissuccessionin pure shallow-waterdepositsonthe Adriatic of aseveralkm-thicksequencealmost in agradualsubduction,enablingdeposition the Adria Microplate towards Laurasia,resulting were characterizedbythegradualmovementof The MiddleandLateJurassicCretaceous reduction oftheformerplatformarea. margin were alsodrowned, resulting inafurther the sameperiod,someareas alongtheNE of the Adriatic CarbonatePlatforms.s..During this eventshouldde fi deep-marine deposition,wasformedasthe way, the Adriatic Basin,chara existed tothenorthofplatform.Inthis the IonianBasinwithBellunowhich through theformationofatrough connecting place inLateLias(itstartedMiddleLias), from the Apenninic and Apulian platforms,took separation ofthe Adriatic CarbonatePlatform Disintegration ofthehugeplatform,i.e. Adria Microplate wasstillunited(Fig.1.1). Namely, duringthatperiodtheentire area ofthe to the Adriatic CarbonatePlatform carbonate platform,itshouldnotbeascribed and represent typicaldepositsoftheiso localities throughout thearea oftheDinarides, or DolomiaPrincipale),are present atseveral Cretaceous andPalaeogenewiththeformation environments, culminatinginthelatest signi as aresult ofcollisionalprocesses, causing was characterizedbygradualdisintegration arguable. IntheLateCretaceous, theplatform of the Adriatic Carbonate Platformisquite The positionoftheupperstratigraphicboundary 1998; Korbaretal.,2001). were formed(e.g.inCenomanian,Tišljar etal., Guši (e.g. nearCenomanian–Turonian boundary, environments ofthedrowned platformexisted or theupliftedblocksinLateCretaceous); around emerged areas intheKimmeridgian, depositional area wassigni established (around emerged partswhenthe events, smallplatformsofarimmedtypewere platforms existedinthisarea: duringsome during someperiods,othertypesofcarbonate carbonate platform,itshouldbementionedthat rst precursor ofthepresent Adriatic Sea,and ć fi cant differentiation ofthesedimentary andJelaska,1993);orcarbonateramps č i ć , LadislavPalinkaš fi ned asdeposits oftheisolated fi ne thelowerboundary fi cantly reduced, e.g. ≠ cterized by sensu stricto ≠ lated . represented merely theintroduction of type, mostlyonlyseveralto200mthick, Resulting carbonatesuccessionsofaforamol contemporaneously withtectonicdeformation. ramps, characterizedbynarrow belts,retreating environments represented irregular carbonate carbonate platform.Carbonatedepositional of theforeland basin(s)withintheformer in Limestones inthePalaeogenewasprimarily so-called LiburniandepositsandForaminiferal was theshortest).However, depositionofthe restricted areas ofSDalmatia,where thehiatus places, e.g.inthearea ofWSlovenia,andin rocks havebeendocumentedonlyinsome took place,mostlyintheEocene(Palaeocene transgression overanexpressive palaeorelief general emersiontookplace,andthePalaeogene smaller. At theveryendofCretaceous, a of theplatformgraduallybecamesmallerand platform emerged, andthedepositionalarea By theendofCretaceous, large areas ofthe troughs (Tišljar etal.,1998;Korbar2001). carbonate ramps,anddeeperintraplatform emerged areas, shallowwaterenvironments, complex palaeogeo blocks, i.e.asubsequentlymore andmore was characterizedbytheexistenceofdifferent area. SincetheEarlyCenomanian,platform (AdCP) andofitsneighbouringareas, which disintegration ofthe Adriatic CarbonatePlatform the product ofitsdisintegration.Therefore, distinction betweenthecarbonateplatformand importance ofmakingaclearterminological In conclusion,wewouldliketoemphasizethe Platform. be considered aspartofthe Adriatic Carbonate mostly byarelatively longhiatus,shouldnot are separatedfrom theCretaceous succession vast area. Consequently, thesedeposits,which shallow watercarbonatefactorycoveringa Palaeogene depositsdidnotrepresent amassive fairly smallsequenceofcarbonatedeposits,the carbonate production, and(3),theresulting tectonics, andthesubordinate role ofprimary area, (2)theprincipalrole ofsynsedimentary con deposits andtheJelarbreccia). Therefore, basins withclastic–carbonatedeposits(Promina deposition, andthesubsequentin of fl uenced byintensetectonics,i.e.theformation fl ≠ ysch troughs withintheformerplatform sidering the(1)restricted depositional ≠ graphical pattern,including fi lig f the of lling 3-06-2004, 10:02:01 fl ysch ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

culminated in the Oligocene–Miocene, resulted Geological Society and in the formation of the Dinarides mountain belt. -the 6th International Congress on Rudists. The stratigraphic range of the AdCP sensu stricto, Recent investigations for the new Geological i.e. a completely isolated carbonate platform, Map of the Republic of Croatia (lithostratigraphic might be defi ned as being from the Late Liassic map, scale 1:50,000), started in Istria in the to the end of the Cretaceous. mid-eighties. New data were obtained also by several specialised investigations. This review DAY 1 is predominantly based on the paper “A Review Introduction to the geology of the Geology of Istria” from the Excursion of Istria Guidebook of the First Croatian Geological Ivo Velić, Josip Tišljar, Igor Vlahović, Dubravko Congress (Velić et al., 1995a). One can also fi nd Matičec and Stanislav Bergant an extensive reference list of published works in the review of the geology of Istria in the paper of The geological literature on Istria is very Velić et al. (2003). abundant and heterogeneous, and extends over more than two centuries. Consequently, there is The stratigraphic insuffi cient space here for a full account. We will and palaeogeographic therefore restrict ourselves to discussions on the evolution of Istria geology of Istria, even omitting papers such as Although intense post-sedimentary, Tertiary G. Stache’s famous “Die Liburnische Stufe und tectonics have signifi cantly affected the entire deren Grenz-Horizonte” (Stache, 1889). area of the former Adriatic Carbonate Platform, Most general data on the geology of Istria can be resulting in the very complex tectonic pattern found in the sheets and explanatory notes to the of the area, there are localities with quite 1:100,000 scale Basic Geological Maps, although well-preserved stratigraphic records, enabling they were published twenty-fi ve to thirty years recognition of important events in the geological ago. The stratigraphy, tectonics, raw materials history of the Adriatic Carbonate Platform. One and geological history of Istria are described of them is Istria, a peninsula located on the NW in six explanatory notes to the Basic Geological part of the Croatian coast, with an area of some Map Sheets: Pula, Cres, Rovinj, Labin, Trieste, 3,000 square km. and Ilirska Bistrica. Here, one can also fi nd From a geological point of view, Istria can be detailed reviews of previous investigations and divided into three regions: lists of references. -the Jurassic–Cretaceous–Eocene carbonate plain From the mid-1960s to the mid-eighties, there of southern and western Istria, were no systematic geological investigations of -the Cretaceous–Eocene carbonate–clastic zone, regional signifi cance in Istria. However, it should characterized by overthrust structures in eastern be noted that, in the seventies, detailed lithofacies and northeastern Istria (from Plomin and Učka and biofacies investigations of shallow water to Ćićarija), and carbonates in Istria began. In addition, several -the Eocene fl ysch basin in central Istria. important international and national geological The geological peculiarities of these regions had meetings were held, presenting new knowledge been noticed historically by the inhabitants of on the geology of Istria: Istria, who coined specifi c names for them: Red -the 16th European Micropalaeontological Istria – the southern and western Istrian plain

Colloquium, named after the terra rossa covering a large part P37 to P54 n° 5 - from Volume -the 4th Regional Meeting of IAS, of the younger Mesozoic and Eocene carbonates; -the 5th Meeting of Sedimentologists of White Istria – in eastern and northeastern Istria, Yugoslavia, -International Symposium on the characterised by karstifi ed outcrops of “white” Evolution of the Karstic Carbonate Platform: Cretaceous–Eocene limestones; and Gray or Relations with other Periadriatic Carbonate Green Istria – in central Istria, characterized by Platforms, Eocene fl ysch. -the 1st Croatian Geological Congress, The Istrian succession suffers from the same -the 80th Summer Meeting of the Italian problem as the rest of the carbonate platform

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura Istria, atleast20–30kmfurtheraway. Thestudied offshore wellsandgeophysicalresearch, are in platform deposits,sincethemargins, de Adriatic Sea.Therefore, weare dealingwithinner are missing,sincetheywere drowned bythe area inCroatia: marginal areas oftheplatform (5 Istrian carbonatesand the Western Istriananticline(partlymodi Figure 1.2-Mapshowingtheschematicdistributionoflarge-scale sequencesinIstria,andthelocationof th large-scale sequence). č i ć , LadislavPalinkaš fl ysch are forthemostpartirregularly covered byrelatively thinQuaternarydeposits fi ed afterVeli fi ned by ć etal.,1995a).Depositsofalllargescale sequencesof of Istriaasan African promontory, i.e.itsspeci a consequenceofthepalaeogeographicposition deposits inotherpartsofthe AdCP, probably as thinner unitsthaninpenecontemporaneous deposits are alsocharacterisedbygenerally position alongthemargin ofthe Adria Microplate 3-06-2004, 10:02:04 fi c ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

(or Apulian Promontory). sedimentation was not interrupted until the The Istrian succession consists predominantly beginning of the Kimmeridgian, when the area of carbonate rocks, ranging in age from Late of Istria was infl uenced by a regional emersion Dogger to Eocene, with subordinate Eocene that lasted through the major part of the siliciclastic rocks, fl ysch and calcareous breccia, Kimmeridgian and Early Tithonian. and Quaternary terra rossa and loess. According Tectonic activity during the Cretaceous (D2 to the results of investigations, the Istrian Late deformation) can be traced as periodic syn- Dogger to Eocene succession can be divided sedimentary movements occurring throughout into four sedimentary units, or large-scale the period. Namely, the West Istrian anticline sequences of carbonate deposits, bounded by (anticlinorium) had already been formed in important discontinuities / emersion surfaces the Early Cretaceous. The oldest evidence of representing different durations, covered by its existence is from the Hauterivian. The hinge Quaternary deposits. The following largescale of this macrostructure remained emergent sequences have been distinguished (Fig. 1.2): throughout the rest of the Cretaceous, i.e. 1) Bathonian–lowermost Kimmeridgian; until the Eocene transgression. There is a lot of 2) Upper Tithonian–Lower/Upper Aptian; evidence to support this theory, in principal: 3) Upper Albian–Upper Santonian; –The exposed succession northeastward from the 4) Eocene; core of the anticlinorium to the Pazin fl ysch basin 5) Quaternary. is more or less continuous from the Bathonian to various levels of the Upper Cretaceous. Tectonics –Eocene foraminiferal limestone has been The tectonic pattern of the Croatian part of Istria found overlying the peneplained relief of is composed of three structural units (Fig. 1.2). Valanginian, Hauterivian, Barremian, Albian, -The Western Istrian Anticlinorium comprises and Cenomanian ages. the largest part of western and southern Istria, –Bauxites from the footwall of the Eocene being composed of carbonate deposits of the limestones were deposited in the palaeorelief Middle and Upper Jurassic in its oldest part, of the Cenomanian and Albian limestones. This and surrounded by Cretaceous and Eocene fact, together with the transgressive nature of carbonates. the Eocene foraminiferal limestones on deposits -The second unit, the Pazin Flysch Basin, is of different ages, excludes the possibility of composed of relatively thin Eocene limestones continuous deposition of a complete Lower and and thick fl ysch deposits, cropping out in the Upper Cretaceous sequence, and its subsequent central and NW parts of the peninsula. erosion prior to deposition of the foraminiferal -The third unit is composed of stacked thrusted limestones. structures of Ćićarija Mt. in the northern part; –The emerged area was inhabited by dinosaurs and of eastern Istria, as well as the Učka Nappe, during the interval from (at least) the Hauterivian which are composed of Upper Cretaceous and to the Late Cenomanian, as indicated by their Eocene carbonates and Eocene fl ysch. footprints and bones. A large quantity of fresh The oldest record of tectonic activity in Istria potable water and terrestrial vegetation would has been found in the Late Bathonian. The have been necessary for their survival. movements represent the oldest deformation – An older succession than that exposed on in Istria, referred to as the D1 deformation. The the coast of Istria can be traced under the sea effects of these movements were local emersion towards the SW, along the extension of the core Volume n° 5 - from P37 to P54 n° 5 - from Volume and a more intensifi ed relief of the subtidal of the Istrian Anticlinorium. area. It has to be mentioned that we are dealing Deep wells in the sea-fl oor confi rm this idea, with recent orientations of structures, and that and provide evidence for the dimensions of the possible subsequent rotations of the area have macrostructure. not been taken into consideration. By the end of the Cretaceous, almost the entire After a brief emersion, subtidal sedimentation Adriatic Carbonate Platform, including the area was reestablished, resulting in fi lling and of Istria, was affected by regional emersion of leveling of the former relief. The continuity of a very variable duration. Emersion was the

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura are partlyMioceneinage. sediments. Anyway, thesemovementsprobably determination inpoorly-developedterrestrial because oftheproblem withstratigraphic of itsupperboundaryisnotde question The durationoftheD3deformation,i.e. (approximately 315–135degrees). of theso-calledDinaricstrikestructures throughout the Adriatic coastlineintheform The result ofthistectonicactivityisobvious factor inthetectogenesisofDinarides. Hence D3deformationbecamethedecisive resulted inaregional compression ofthearea. of movements waswitnessedbytheformation a new, D3deformation.Theintensityofthese The Eocenetransgression wasaconsequenceof different characteristics. renewed marineconditionsintheEocenehad platform carbonatesedimentation,since and markedtheendoftypicalproductive disintegration oftheformercarbonateplatform, The LateCretaceous tectoniceventsinitiatedthe consequence ofthe fl ysch basins,whiletheirfurtherincrease č Figure 1.4-LocationofthePogledalo/Barbanpromontory andFenoligaislet. i ć , LadislavPalinkaš fi nalCretaceous compression. fi nitely denoted, towards thenewstress orientation. or rotation ofalready existingstructures structures intotheregional transcurrent faults, structures, reactivation ofoldinheritedbrittle neotectonic of new, formation either the comprised activity Neotectonic stress. regional the greatest activity of N–S oriented of the consequence is a Dinarides the entire (D4) in deformation Neotectonic Figure 1.3-TheBrijuniIslands archipelago. 3-06-2004, 10:02:11 ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

The Brijuni Islands National Park Ladislav Palinkaš and Sibila Borojević-Šoštarić The Brijuni Islands National Park has been compared to heaven on earth. According to legend, angels collected the remains of Eden and created a lasting symbol for mankind – an oasis of peace, and a wondrous gift of nature, protected by the waves. The Brijuni National Park and Memorial Park is one of the brightest pearls of natural beauty in the Adriatic (Fig. 1.3, 1.4). It can be compared only with the well-known Kornati Archipelago Island group. What makes the Brijuni Islands so attractive, is the abundance and variety of fl ora and fauna in a splendid landscape of the indented island coastline in the emerald blue-green sea. The Brijuni Islands were proclaimed a national park on 27th October 1983. The park covers an area of 3,635 hectars. It consists of 14 islands: Veliki Brijun, Mali Brijun, Sv.Marko, Gaz, Obljak, Supin, Supinić, Galija, Grunj, Vanga, Madona (Pusti), Vrsar, Jerolim, and Kotež, which together Figure 1.5 - Lithostratigraphical column of Istria, make up 734.6 hectares. The with dinosaur fi nds. surrounding sea makes up for a larger portion of the park - 2,900 hectares. bays have shingle and sand. According to geological and geomorphologic Climatically, the Brijuni Islands belong to make-up, the Brijuni Islands are a continuation the northern Mediterranean, and have all of the Istrian mainland, and are made up of the features of the western Istrian coast. The horizontal layers of Cretaceous limestone, mean temperature of the coldest month is covered by thick layers of brownish-red soil. The 5.9 degrees Celsius, and 23.3 degrees for the

rise in sea level during the past tens of millennia, warmest. Average annual precipitation is 817 P37 to P54 n° 5 - from Volume as a result of melting ice, gave the islands their mm. Low summer rainfall, and a relatively high fi nal appearance and a highly indented coastline. humidity play a signifi cant role in shaping the The total length of the coastline of all the islands vegetation of the islands. The islands also have put together is 46.4 kilometres. The most a rich cultural heritage dating from Roman and indented islands are Veliki Brijun (26.6 km), Mali Byzantine times. Brijun (8.2 km) and Vanga (3 km). The shores are Amidst century-old olive trees and vegetation, mostly low and rocky; however, their horizontal originating from various climates, cultural and stratifi cation makes them easily accessible. Some historic monuments emerge like pearls. Some

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura remains oftheSt.Marybasilica(5 which bearswitnesstothebeautyofthisedi whose messageandbeautysupportman’s make theBrijuniIslandsanaturalresource, fl A zoo,asafaripark,museum,sculptures, a erected in1481dedicatedtoSt.Germain. Not farfrom thehotels,onecanvisitchurch which wasrazedtotheground, andthenrebuilt. from the1 The remains ofRomancountrymanorsdating the spiritandtasteofanancientculture. Roman architecture, whichoffer aninsightinto of themostattractiveare uniqueexamplesof promontory. allosaurid dinosaurfrom theProgledalo/Barban Figure 1.6-Large theropod footprintleftby castrum (fort)datingfrom the6 west coastofVeliki Brijun,onecanseeaByzantine Roman thermalbaths,Venus’s temple.Onthe Veliki Brijunare amust,asare theremains ofthe ower garden andnumerous otherattractions st - 2 č nd i ć centuryB.C.inVeriga Bayon , LadislavPalinkaš th century, andthe th -6 th century), fi ce, with nature. lasting efforts through thecenturiestoco-exist on thetrackbearingsurface,and16ofthem Sixty-one dinosaurfootprintswere discovered intertidal environment. mm. Ripplemarksindicateashallowwaterto peletal limestone,withathicknessof100-200 overlying bedisathinly-bedded,stromatolitic- of 43x5.5m,andathickness130mm.The The layerissub-horizontal,withanexposedarea plane ofalayercomposedfenestralmicrite. Dinosaur footprintsoccurontheupperbedding gastropods, andcorals.(DallaVecchia, 2002). benthic foraminifers,green algae,ostracods, packstone-grainstone. Thesedimentcontains deposits, represented bythin-beddedpeloid characterized byintertidal/shallowsubtidal The Pogledalo/Barbansite(Fig.1.5)is by DallaVecchia (2002). Veli were discovered duringlaterinvestigationsby Footprints onthePogledalo/Barbanpromontory has describedtwodifferent typesoffootprints. of the Austrian industrialistBachofen-Echt,who Brijuni Archipelago beganin1925,withthework Research onthedinosaurfootprintsof fi - Cenomanian)sediments(Figs.1.4).Theoldest the LateJurassicandCretaceous (Valanginian eastern coastofthe Adriatic Sea)camefrom platform (whichisnowoutcropping alongthe dinosaurs onthe Adriatic-Dinaric carbonate All fossilremains (mostlyfootprints)of Mezga AleksandarandBajraktarevi Fenoliga islet promontory, BrijuniIslandsandthe Dinosaur tracksonthePogledalo/Barban Stop 1.1: nd isofLateTithonian age. ć Figure 1.7-Fenoligaislet,withthelocationofa andTišljar (1987),anddescribedrecently trackbearing layer. ć Zlatan 3-06-2004, 10:02:18 ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

of the biostrome, suggesting that the biostrome was dead, and at least temporarily emergent during trackway formation. The foraminifer Broeckina (Pastrikella) cf. balcanica Cherchi, Radoičić and Schroeder was determined, and indicates a Middle to Late Cenomanian age (Mezga and Bajraktarević, 1999). On the explored outcrop, 146 dinosaur footprints arranged in six trackways, and six footprint groups have been recorded. Two basic types of footprints were differentiated: large (23- 40 cm) circular–elliptical footprints, assigned to the sauropods (Fig. 1.8), and smaller (15-20 cm), slender tridactyl footprints that were assigned to the theropods (Fig. 1.9). The footprints from Fenoliga serve as a basis for determining the size and speed of these dinosaurs. The length of sauropods was estimated to be between 8,5 - 11 m. The length of theropods range from 3 - 3,5 m. Their speeds were about 1 - 3 km/h for the sauropods, and 4 - 7 km/h for the theropods (Mezga and Bajraktarević, 1999). Footprints of three theropod and at least six

Figure 1.8 - Circular footprints, assigned to the sauropods/

form four trackways. Other footprints do not make trackways, but occur individually. Among these, two types can be distinguished. The fi rst type is a robust, stout, tridactyl form (Fig. 1.6), arranged in four trackways and with 34 isolated sauropod footprints. The second type is a gracile, slender, individuals tridactyl form. These footprints belong to large are present theropod dinosaurs, similar to allosaurids (Fig. at the site. The 1.6). The reconstructed lengths of these large taxonomic position theropods, ranges between 7.5 - 8 m, and average of the footprints was velocities were around 5 km/h. not determined, owing Dinosaur tracks on the islet of Fenoliga (Fig. 1.5) to the inadequate record were discovered by Gogala (1975). The islet is of dinosaur body fossils in comprised of concordant, well-bedded, white- Istria. The footprints indicate grey limestone layers, with bed-thicknesses the existence of extensive varying between 0.1 and 1.5 m. The track-bearing Cenomanian terrestrial habitats. outcrop comprises the upper bedding plane P37 to P54 n° 5 - from Volume Favourable palaeoecological of a 12-cm thick limestone layer, exposed over conditions during this period an area of 45 x 16.5 m (Fig. 1.7) Two carbonate facilitated survival of the large lithofacies can be discerned on the outcrop: sauropod and theropod populations. white massive micritic limestones predominate on the western side, while the eastern side is characterized by a grey Rudist biostrome, between 2 - 2.5 m wide, and oriented N-S. The Figure 1.9 - Theropod footprints from dinosaur footprints occur on the upper surface the Fenoliga islet.

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura products depositedinthebasin,shelf,coastal mostly intheEocene,obliterateddiversi depositional sites.ThePaleogenetransgression, emerged, withthereduction ofthecarbonate former platformregion. Large areas ofthe AdCP in deposits andJelarbreccia, clasticcarbonate beginning ofthe AdCP disintegration. Promina palaeorelief morphologyandmarkedthe carbonate platform Disintegration oftheAdriatic intensi incipient collisionalprocesses, progressively intra-platform troughs, wasinterrupted by the creation ofcarbonaterampsanddeeper of peripheralparts,and by theepeiricdrowning quiescence, disturbedonly Cretaceous. Thistectonic deposition uptotheLate long-lasting shallowwater the AdCP becameasiteof sensu stricto. carbonate platform(AdCP) boundary ofthe Adriatic event represents thelower This Basin. the Adriatic of thepresent Adriatic sea, Basin, andtheprecursor Ionian BasinandtheBelluno a trough connectingthe Late Lias.Separationoftheplatformswasalong as anisolatedcarbonateplatformfarintothe Apenninic and Apulian platforms,whichexisted a hugecarbonateplatform,comprising Adriatic, the Tethyan realm. Itenabledthefoundationof promontory, asavastshallowwaterbodyinside of anensialicblock, Adria Microplate or Apulian Middle Triassic timegaverisetotheformation Velebit Mt..FragmentationofPangeainthe already intheMiddlePermiantime,ason traced inplacesbythedepositionofcarbonates future northernGondwanamargin, canbe autonomous entityoftheepeirictypeon Foundation ofthecarbonateplatformasan Ladislav Palinkaš led totheformationof paroxysm inthelatestCretaceous andPaleogene of sedimentaryenvironments. Thetectonic fi llings ofthe fi ed, whichgaverisetothediversi č i ć Afterwards, , LadislavPalinkaš fl ysch basin,are tectogenic DAY 2 fl yschtrough withinthe

Figure 2.1-Atthesouthendisa13th-centuryRomanesquecathedral,whose campanile (belltower)isconsidered tobethe architecture ontheAdriaticlittoral.Itis fi cation fi ed to theDinaricmountainbelt. systems. TheOligocene-Miocenetimegavebirth environments, alluvialfans,andbraided-river the greenest islandinthe Adriatic. these numerous springs,Rabisconsidered tobe communications withthemainland.Becauseof islands, isincreasing, inpartbecauseofgood island –which,incontrasttomostofthe Adriatic valuable watersupplyforthepopulationof Its more than300freshwater springsprovide a hundred-year-old agave,isnowtheprideofRab. cypress, Indian island. TheKomrcar Park,withitslaurel, poplar, botanical exhibition,withplantsnotnativetothe islands inthe Adriatic, andisaveritable Rab Islandisoneofthemostdensely-wooded Greece. stretch from theeastern Adriatic anddownto to thatfoundinthecraggyDinaric Alps, which from theirkarsttopography, whichisidentical chain. Theoriginoftheislandscanbegleaned into thebasins,resulted inthecurrent island the land,andpenetrationofseawater 30.000 yearsago,theloweringandelevatingof connected withthemainland;about20.000- Rab andalltheDalmatianislandswere originally of limestone. m atMt.Kamenjak,andcomprisesthree ridges 103.2 km,itreaches amaximumaltitudeof408 length of22km,anditstotalcoastal m. With anarea of91sq.km,agreatest transverse the shortestdistancefrom thelandbeing1,800 Podvelebitski Kanal(theVelebit Channel)with Rab isseparatedfrom themainlandby The IslandofRab towers onaridgedominatingtheoldtown. fi g-tree, rosemary, pine,and fi nest exampleofRomanesque fi rst inalineoffourbell 3-06-2004, 10:02:24 ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

Figure 2.2 - Geological map of the Rab island. After Mamužić at al. (1969)

The ancient name Arba, Arva, Arbia (mentioned document on the establishment of the Franciscan Volume n° 5 - from P37 to P54 n° 5 - from Volume by Ptolemy and Pliny the Elder, and in Tabula monastery of St. Euphemia in Kampor. Under Peutingeriana), derives probably from the the rule of Emperor August, Rab became a Illyrian Arb, meaning dark, green, forested, Roman municipality. Already in the 5th century, which is a chief feature of the island even today. Rab was the seat of the diocese. Croats inhabited In the 10th century, the emperor Constantine Rab some time later than the other islands, Porphyrogenitus calls it Arbe, the form later because they had to conquer a well-organised taken over by the Italian language. The Croatian local Roman community. At the beginning of the name Rab was fi rst mentioned in 1446, in a 11th century, Rab fell under the rule of Venice for

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura doorways, etc. Loggia, Venetian patricianpalaceswithbeautiful monuments ofart:medievalchurches, the narrow Mediterraneanstreets, preserves many town. Thetownwithitstypical,twisting,and bell towers,onaridgedominatingtheold coastal region. Itisthe of Romanesquearchitecture inthe Adriatic tower) isconsidered tobethe Romanesque cathedral,whosecampanile(bell 2.1). At thesouthendpresides a13th-century steep promontory alongthewestcoast(Fig. with three parallelmainstreets builtona The principaltown,Rab,isawalled and summerresort. of the20thcentury, whenitbecameaclimatic Tihomir MarjanacandLjerka Island ofRab recover economicallynotbefore the The diocesewasabolishedin1828.Rabstartedto political, communal,andeconomicregulations. statutes from the14thcenturycontaininteresting of Venice followed.FragmentsoftheVenetian 1409, afterwhichthealmost400-yearlongrule island toenjoypeaceandeconomicboomtill political formwhichenabledthetownand time, afree urbancommunewasestablished,a a shortperiod,andthenjoinedCroatia. At the The shoreface sandstonesdocumentfacies was truncated bythebaseofsandstonebodies. interpreted intermsofashoreface deposit,that composed ofnumerous stormbeds,are Sandstones thatoccurassheet-likebodies, in the Alps. was outsidethepresent Dinaricrange,probably incised valleysetting.Theprovenance ofsand have beendepositedinanouterestuaryor them assandwavesorcomplexduneswhich deposited bytractioncurrents, andweinterpret Sandstones whichbuildsandstonebodieswere transgressive andregressive intervals. sea levelriseandfall,sowecandistinguish succession documentsseveralepisodesof and shallow-marineorigin.Thesediment Adriatic realm owingtotheirsiliciccomposition The LoparSandstonesare uniqueintheEastern Introduction Eocene incisedvalley Stop 2.1: č i ć , LadislavPalinkaš fi ll clasticsofthe fi rst in alineoffour fi ns example nest fi rst decades relative sea-levelfalls. paralic seaandincisedvalley(s),formedduring can interpret thedepositionalenvironments asa basinward andlandward shiftsoffacies,sowe Frequent oscillationsinsealevelforced parts ofcompletedepositionalsequence(s). interpreted asatransgressive interval.Bothare estuarine sandstonesandoffshore sedimentsis regressive interval,whereas successionof shoreface sediments,isinterpreted asa Succession ofoffshore- andtheoverlying pervasive bioturbation. or offshore, where thesandwasadmixedbya where relicts ofstormsandstonesare preserved, Sandy marlswere depositedinalowershoreface, forced regression. thick tempestites,wehaveinterpreted thisasa offshore marls,andthecontactismarkedby sharp-based shoreface sandstonesoverlie in thenumberofmarlinterbeds.Where thick thickness ofindividualbeds,andareduction progradation byshowingagradualincrease of Geology oftheIslandRab of Transitional Bedsisquitepoor, sodirect reaches onlyca.10m.Thequalityofexposures 2.3). Theirthicknessisveryvariable,andhere it usually referred toasTransitional Beds(Fig. are overlainbyglauconiticmarlylimestones, and Milan1973).ForaminiferalLimestones (Mamuži Turonian -SenonianRudist-bearinglimestones represented byCenomanian-Turonian and 2.2). Theoldestrocks are Cretaceous carbonates, consists oftwoanticlinesandsynclines(Fig. The structural frameworkoftheIslandRab (Mamuži gastropods), whichindicateLowertoMiddle accompanying taxa(bivalves,echinoderms, contain abundantforaminiferalfaunaand Limestones, andNummuliteLimestones.They base upward: MiliolidaLimestones, Alveolina Limestones are composedofthree units,from the and rare bauxiteoccurrences. TheForaminiferal is characterizedbygentleangularunconformity, between Cretaceous andPaleogenelimestones Mamuži “marls andsandstones”(Mamuži of ForaminiferalLimestones(below),and deposits ontheIslandofRabare composed overlain byPaleogenecarbonates. ć ć ć andMilan1973)(above).Thecontact , 1962)orLateEoceneage(Mamuži etal.,1969),whichare disconformably ć etal.,1969; 3-06-2004, 10:02:32 ć

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Figure 2.3 - Schematic stratigraphic column of the 2.3): a) Mamužić (1962) divided the Eocene Rab island Paleogene sequence, and age attribution clastics into two units: “Lower” and “Upper by various authors. Flysch”, respectively (the “Lower Flysch” are marls with sandstone interlayers, while contact with overlying clastics is not visible. the “Upper Flysch” is an alternation of marls The Rab Island Eocene clastics were previously and sandstones); b) Muldini-Mamužić (1962) recognized as fl ysch (Marinčić, 1981), but their interpreted the “Lower Flysch” as deep-marine, origin was reinterpreted in terms of tidal shallow based on microfossils, and the “Upper Flysch” as marine deposits (Marjanac and Marjanac, 1991, of a shallow-marine, even coastal environment; Zupanič and Babić, 1991). The youngest are c) Marinčić (1981) held that the Eocene clastics of Quaternary deposits, which are partly of Eolian the Island of Rab are proximal facies of the fl ysch origin, and partly fl uvial, and alluvial. basin, which he reconstructed as extending from Volume n° 5 - from P37 to P54 n° 5 - from Volume Italy to Albania; d) Marjanac and Marjanac Eocene Clastics (1991) reinterpreted the “Upper Flysch” In spite of the folded structure of the island, sandstones as tidal sand waves that migrated the Eocene clastics on the Lopar peninsula are towards the southwest; e) Zupanič and Babić tectonically almost undisturbed, and the quality (1991) interpreted the cross-bedded sandstones of their exposures is excellent, because it allows as complex dunes built under the infl uence of the almost 3-D study of sedimentary bodies. tidal fl ows, and concluded that the major part of The Eocene clastics of the Island of Rab have the outer Dinaric clastic area was covered with a been, until present, variously interpreted (Fig.

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura (1962) SanMarinoMarlsare about150mthick. Flysch”). deepwater environment. According toMamuži stems, butveryrichmicrofauna, indicativeofa composed ofrare echinodermsandcrinoid (1962) reported poorly-preserved macrofauna the large contentofmarl.Muldini-Mamuži San MarinoMarlsare poorlyexposeddueto San MarinoMarls speci San MarinoMarls notations, wepropose tocalltheolderunit bene one, whichispredominantly sandy. Forthe with onlythinsandinterbeds,andtheyounger sedimentary units;theolderunit,whichismarly that theLoparclasticscomprisetwodistinct Previous researchers havealready recognized shallow tidalseainEocenetimes. bioturbated sandymarls.Thesandstonesare sandstone packages,whichare dividedby Lopar Sandstonesconsistofafewmetersthick Lopar Sandstones unit the Figure 2.4-Tidal bundles. fi fi t ofsimplicity, andtoavoidgeneticco- c name“LowerFlysch”),andtheyounger Lopar Sandstones č i ć , LadislavPalinkaš (insteadofaninformal,but (insteadof“Upper ć ć

forams andfrequent small foraminifers,more frequent agglutinated sandy marls,withrare andpoorly-preserved lower part,there occurbrownish calcareous- indicates ashallow-marineenvironment. Inthe large nummulitesstarttopredominate, which that smallforamsdisappeartopwards and poorly preserved) andpoormicrofauna, and deposits containabundantmacrofauna (although nannofossils ofthe part oftheUpperEocene.Beni uppermost MiddleEocene,andpossiblytoa (1962) attributedtheRabclasticsto these large foraminifers,Muldini-Mamuži contain basicallylarge foraminifers.Basedon compared totheLoparSandstones,which The SanMarinoMarlsare more fossiliferous Age ofRabclastics were found. According to superposition, more resedimented thanautochtonousspecies However, insamplesofthe LoparSandstones, no resedimented formsinthestudiedsamples. Bartonian) intheSanMarinoMarls,andfound nanno-zone (NP16,UpperLutetian-Lowermost Muldini-Mamuži stand outinrelief. more resistant toweathering,sotheyusually ć (1962)statedthatthese Nummulites Discoaster taninodifer . ć (1983)found 3-06-2004, 10:02:38 ć

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he assumed that the Lopar Sandstones can environment was probably deeper lower belong to the same or a younger biozone. The shore-face, as indicated by the intensity of resedimented nannofossils are key-fossils of bioturbation, the large size of boring organisms, the zones NP 6-7, NP 7-9, NP 9-10, and NP and the episodic input of sand, probably during 10-12. The last two allochthonous assemblages storms (indicated by gutter-cast textures). have also been determined in Istria, on the Pag Relict bedding suggests that the sediment was Island, and in Ravni Kotari. Benić believed that originally an alternation of cm-thick sand beds these resedimented nannofossils originate from and marls, which was subsequently completely fl ysch which was contemporaneous with the destroyed by intensive bioturbation. Thus, the Foraminiferal Limestones. sand grains originated from sand beds, although some may be Aeolian in origin. The Lopar sandstones A poorly bioturbated sandy marl, with smaller The Lopar Sandstones comprise the following ichnofossils, and no sand interbeds was facies (members): a) sandy marls, b) heterolithic deposited during periods of poor aeration packages (sandstone - marl alternation), c) of the bottom water, as indicated by a lower sandstones, d) biocalcarenites, e) conglomerates, bioturbation rate and the smaller size of and f) slumps. ichnofossils. The depositional environment was probably an open shelf (offshore). Sandy marls Bioturbated sandy marls were deposited on Heterolithic packages a relatively shallow shelf, which is indicated (Sandstone-marl alternation) by macro- and microfossil assemblages with Heterolithic sediments were deposited above associated Skolithos and Cruziana ichnofacies. the storm wave base, as indicated by HCS and Intensive bioturbation indicates a good aeration SCS structures in sandstones. Storms alternated of the environment, a slow deposition rate, and with relatively long fair-weather periods with a minor terrigenous input. The depositional only suspension sedimentation, when benthic

Figure 2.5 - Double mud drapes are locally well-developed, also note rippled bottomset which pinches out downdip. Volume n° 5 - from P37 to P54 n° 5 - from Volume

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura storm-beds. large numberandtheoverallthicknessof part ofthelowershoreface, asindicatedbya proximal partoftheopenshelf,namelyanupper depositional environment wasprobably a organisms recolonised theseabottom.The that are dividedwith Tidal bundles(grouping oflaminaeinpackages or complexdunesof Ashley (1990). recognized as Allen’s (1984)type2and3bodies, are usuallyreferred toassandwaves,andcanbe formed large complexsedimentarybodiesthat in migrationintensityandperiodicalerosions cross-bedded sandstones,whereas variation Migration ofdunesproduced large-scale Sandstones the lowtidescanre tides. Erosion canstartduringlowtides,thus the thinsandstonelaminaedevelopduringneap interpreted astheproduct ofspringtides,while structures. Thickerpackagesofcross-laminae are as doublemuddrapes(Fig.2.5)andherring-bone tidal processes (Visser, 1980;Roep,1991),aswell sandstone, Fig.2.4)are considered diagnosticfor the hightide,still-standmudfrom suspensionis reactivation surfaces(Collinson,1970).During Figure 2.6-Slumpingaffected offshore sandymarlsandtheoverlyingshoreface sandstones. č i ć , LadislavPalinkaš fl ect insedimentsonlyas fi nergrained orthinner formed bylocalvorticesinastormsurge. Itis origin isindicatedbygutter-casts, whichwere also occurinestuaries.Becausethetideshadto admitted thatanalogousdepositionalbodies they referred toasa“tidalsea”,althoughthey (1991) interpreted ashallowmarinerealm, which valley. have beenwithinafunnel-shapedbayorincised be ampli affected theunderlyinglithi a consequenceofravinementerosion, which storms. However, theymayalso havebeen which occurred duringexceptionallystrong tempestites (MarjanacandMarjanac1991), Biocalcarenites were interpreted asskeletal Biocalcarenites like, wedonotknowyet.Zupani Kvarner BayEocenepalaeo-topographylooked realm controls thetideamplitudes.What However, thetopographyofdepositional bodies suchasdunes,sandwaves,andbars. prerequisite forthegenerationoftidalsandstone bays andestuaries.Hightideamplitudesare a they increase infunnel-shapedstraits,large Tide amplitudesare lowontheopensea,but deposited, formingamudlamina. fi ed, thedepositionalenvironment must fi ed sands.Storm č andBabi 3-06-2004, 10:02:51 ć

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unlikely that the storm will create erosional relief lithologies indicate that they represent the most deeper than a few decimetres to a metre or two. resistant lithology in the hinterland. Since the Even then, the deepest erosion will occur in less cross-bedded sandstones are interpreted in protected areas. terms of tidal sand bodies (sand waves), it is Ravinement is created by impinging waves possible that this coarse sediment was deposited which eroded the bottom, and the depth of in low topography, eg. tidal channels. erosion is known to reach several meters, and Because of signifi cant grain size difference, the up to tens of meter,s. Lithoclasts, which are coarse debris could not be transported, and identical to the underlying sandstones document deposited simultaneously with medium sand relatively deep erosion, down to the level where by normal traction fl ow, which created the the sand was already cemented, and support dunes and sand waves. Thus, gravel-size debris interpreted ravinement origin. was probably reworked from hypothetical Abundant foraminifers and larger skeletal debris underlying coarse lag, which was most likely a (oysters and corals) were probably introduced fl uvial deposit. from lateral sources, and partly remained as a coarse lag after the erosion of poorly lithifi ed Slumps sediments. However, it seems that skeletal debris Slumps frequently occur within Lopar did not originate from the underlying sediments, Sandstones, and are characterized by lensoid because there we do not see identical fossils in geometry and slump folds (Fig 2.6). Their living positions, nor do the fossil assemblages thickness reaches up to 6 m, and they occur look natural, because abundant Nummulites tests within marly intervals, as well as within occur together with big broken (!) oysters. It may sandstones. Slump folds are commonly made be assumed that this skeletal debris originated up of sandstones and sandy marls, and occur from lateral environments, as mentioned in a sandy marl “matrix”. The slumped sandy above. Wave (symmetrical) ripples, on top marls contain scattered Nummulites, oyster of biocalcarenites, document a very shallow fragments and gastropods, and small scattered depositional setting in any case. chert gravel. Some slumps have started within the marly Conglomerates interval and got incised down to the underlying Conglomerates occur only at the bases of the sandstones, so they may be overlying sandstones units A, B and C1, in the lower part of the Lopar locally. The slump base is clearly erosional, section. Gravel does not form individual beds, whereas its upper surface is generally fl at. The but occurs within cross-bedded sandstones in the sediments overlying the slump are found to form of thin lenses and interbeds, and sometimes onlap its top surface. they line the foresets. Gravel interbeds are Slumps indicate slope instabilities, regardless sometimes 10 cm thick, with erosional bases, of its gentle dip. Marls must have facilitated and they sometimes fi ll gutter casts and even slumping and got remoulded in the “matrix” some ichnofossil shafts. Gravel locally occurs which surrounds the slump folds. Slump scattered in sandstones, and locally occurs in failures may have been initiated by slope some biocalcarenite beds, along with skeletal oversteepening, slope overloading, liquefaction, debris. Clast diameter reaches up to 10 cm, and hydraulic shocks, or earthquakes. It seems that rounding as well as sphericity are generally overloading due to a high deposition rate may good. Clast lithologies are odd with regards have initiated slumps within some sandstone Volume n° 5 - from P37 to P54 n° 5 - from Volume to the External Dinarides setting, because they bodies, whereas slumps related to marly are mostly represented by various cherts and intervals may have been initiated by liquefaction silicifi ed arenites, and no carbonates (!), so their or high-amplitude seismic shocks. provenance is still unknown. The grain size of gravel indicates considerably high fl uid velocity, and good rounding (despite resistant lithologies) document their long tractional transport. Predominating silicifi ed

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura truly aphenomenon,duetotheirgeological Paklenica (SmallandLarge Paklenica),are The entrytothecanyonsofMalaandVelika this mountainmassive. Park “Paklenica”,thesecondnationalparkof of thesouthernPangea?Diversi Was itaninstantaneouseventalongthemargins death ofthe AdCP raisesaquestionofitsbirth. created themountainchainofDinarides.The predominantly andorogenic uplift, environments, producer ofclasticsediments carbonate deposition.Diversi process ofdisintegrationgraduallystopped Triassic totheLateCretaceous, whenthe as auniqueentity, existedfrom theMiddle The Adriatic carbonateplatform(AdCP), Ladislav Palinkaš the MiddlePermiantime Foundation ofthecarbonateplatformin mountain withanarea ofnearly2000km and Biosphere), andin1981almostthewhole of thebiosphere reservations (MAB–Man of UNESCO”asaparttheinternationalnet tradition. In1978,Velebit received “TheCharter as wellitsmajorandminorparts,hasalong The protection ofthewideterritoryVelebit, Velebit-Paklenica The NationalPark and theestablishmentof while ontheVelebit Mt.,carbonatedeposition are succeededbytheLowerTriassic dolomites, marine sandstonesofthelatestPermianage sandstones, inGorskiKotar(NWCroatia), the latestPermianover (NW Slovenia),carbonatedepositionstartedin of thepresent Dinarides.InŽirovski Vrh area extension ofthesouthernPangaeainregion not aconcurrent process experiencedatthefull carbonate platformonthePermianclastics,was Carbonate deposition,asthefoundationof Dinarides, doesnotoffer theonlyanswer. the NWDinaridesinSloveniatoCentral sedimentary environments inPermiantimefrom Mesozoic megacycle. and continuedwithoutbreak asapartofthe ramp evidentlystartedinMiddlePermiantime total area of109km became anature park.TheNorthpart,witha č i ć , LadislavPalinkaš DAY 3 2 , is,alongwiththeNational fl uvial Val Gardena fi e sedimentary ed fi rt carbonate rst fi cto of cation fi nally 2

Vrilo, Velika Mo quality, are Stražbenica,KontinovoVrilo, Crno drinking water, renowned fortheirexcellent and manyconstantwatersources. Sources of temporary riversinthePaklenicaNationalPark, As such,there are severalconstantand Orlja Paklenica, andinthetemporary Brezimenja in theextendedregions ofVelika Paklenica, under theporous, andlayersofcarbonaterocks, The waterimpermeablesedimentsare located is openforviewing. karst, andthewealthof and hydrological particularities,theabundant and mostcompletelydevelopedPalaeozoicarea Velebit andLikaregion represents thebestknown The UpperPalaeozoictectonicbeltoftheMt. Introduction Jasenka SremacandTihomir Marjanac sediments ofthecentralVelebit Mt. Middle toLatePermiantime:Palaeozoic Carbonate platformenvironmentfromthe Stop 3.1: and theVodarica pit.OnlytheManitaPe the mostspectacularare theManitaPe The parkboastssome70caves,amongwhich evident inthenumerous morainedeposits. karst formationswere created duringglaciations, well-developed intheBojinacregion, where the Basins withcracksandchannelsare particularly differences duringindividualseasons. fl caves, whicharose from theintensiveactivityof in thelimestone,channels,basins, varying karstformationsare visible,from cracks the plateaubetweenbothcanyons.Here, many the regions ofBojinac,Vidakov Kuk,andon Park are seeninthesharpkarstformations The geologicalparticularitiesoftheNational Velebit mountains. deeply cutintothemassivesouthfaceof the MalaPaklenicaCanyon,12kmlong,are the Velika PaklenicaCanyon,14kmlong,and thus deepeningthemfurthereveryyear. Both creeks erodes thelimestonewallsofcanyons, the springandautumn,sheerpowerof value totheentire region, enrichingit,andin creeks MalaandVelika Paklenicagivegreat owing water, andfrom thelarge temperature č a River. č a andthesource regions ofMala č ila andPe fl ć ora andfauna.The ica. fi fl ssures, and ssures, ow ofthe 3-06-2004, 10:02:58 ć ć cave, cave ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

Figure 3.1 - Geological column of the Velebit Mt. Permian deposits (after Ramovš et al., 1990).

in Croatia. Sediments exposed here range from that existed until the end of the Permian. Rapid the Pennsylvanian (Moscovian) to the Late production of carbonate material resulted Permian in age. Carbonate sedimentation took in more than 900 m of carbonate sediments, part sporadically during the Carboniferous dolomites, and limestones, rich in diverse and P37 to P54 n° 5 - from Volume and Early Permian. Intensive tectonic uplift at numerous fossils from Middle to Late Permian the beginning of the Middle Permian caused age (Salopek, 1942; Kochansky-Devidé, 1965; the formation of prominent relief and its Ramovš et al., 1989) rapid erosion, followed by sedimentation of Lengthy carbonate sedimentation began after terrigenous molasse sediments. the deposition of the red sandstones, with the After the phase of instability, the lowering of the black limestone of the Eoverbeekina salopeki relief enabled the stabilization of the area, and the zone, which can be observed west of Brušane formation of a carbonate platform environment village (near Gospić, central Croatia - Fig. 3.1.

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura Bellerophon Limestones containlarge gastropods ( Small patch-reefs produced bycalcisponges, many othertaxa),are extremely abundant. Vermiporella, Gymnocodium,Permocalculus, The secondlimestonebelt,the Pleurotomaria, Orthoceras, Neoschwagerina, Waagenophyllum, Bellerophon, Globivalvulina Dunbarula, Nankinella,Schubertella,Glomospira, Baške Oštarije.Foraminifera:( been collectedfrom thearea ofBrušane and calcisponges, bryozoans,andgastropods, have species, theaberrantbivalve and oldhaminoids,includingseveralendemic predominantly spiriferids,enteletids,productids, macrofossils. Numerous brachiopods(45taxa), craticulifera Mizzia skeletons, predominantly ofdasycladacean recrystallized algal,foraminiferalandmicrofossil “spotted” dolomites.Whitespotsrepresent approximately 300mthicksequenceofgrey Staffella typical microfauna ( Karlobag road (afterSremac, 1991). Figure 3.2-Patchreef intheParipovjarak,nearBaškeOštarijevillage,alongGospi , accompaniedby ). Limestonesare overlainbyan ), cephalopods( zone,isextremely richin ,

etc.), andcalcareous algae:( č i ć , LadislavPalinkaš Eovrebeekina, Sphaerulina, and Eovebeekina, Staffella, Orthoceras Edmondia. Neoschwagerina, Neoschwagerina Tanchintongia Platystoma, ), anda Mizzia, and , dolomite light grey crystallinedolomite(“Schwagerina”- are separated,orinsomeplaces,replaced, with The middleanduppermostlimestonezones have beenfoundinthishorizon(Sremac, 1991). bryozoans, cyanobacteria,and/or sporadically ( from thelowermostlimestonezonealsooccurs Kahlerina, Dunbarula, Likanella, Salopekiella,Goniolinopsis,Neschwagerina, ( Streptorhynchus, Orthotetes the Yabeina-zone, suchasbrachiopods( middle zone,butsomenewmacrofossils occurin assemblages are notverydistinctfrom the limestone horizon.Differences inmicrofossil specimens of fusulinid species- Yabeina syrtalis,although syrtalis Zone,wasnamedafterthedominant The uppermostlimestonezone,the Yabeina begun inthisperiod. et al.,1991),withscarce fossils,hadalready “early diageneticsupratidaldolomites”(Tišljar “transitional dolomites”( parts ofthebasin,sedimentationso-called Temnocheilus sensu ). Dense“transitional”dolomites Yabeina Stafella, Eoverbeekina Salopek,1942),with alsooccurinthemiddle and gastropods. Fauna sensu ), andgastropods Salopek,1942),or ć - ). Insome Tubiphytes, 3-06-2004, 10:03:02 Derbya, Mizzia,

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Figure 3.3 - Vertical section through the patch- reef complex in the Paripov , near the Baške Oštarije village, along the Gospić-Karlobag road (after Sremac, 1991). Bold letters indicate individual reef units, as referred to in the text.

Observation stop: Paripov Jarak near Baške Oštarije village (central Velebit Mt.) In the area of the Brušane and Baške Oštarije villages, in the central part of the Velebit Mt., dolomite-limestone sediments of the Middle and Upper Permian are well developed. Three zones of black limestones can be clearly distinguished, containing numerous well-preserved micro- and macrofossils. The observation point is located near Baške Oštarije on Velebit Mt., also known as “Salopek’s second zone of black limestones, pv2”. These black limestones have attracted researchers due to their rich fossil content, and interesting sedimentological features (Kochansky- Devidé, 1965; Sremac, 1991; Marjanac and Sremac, 2000). During sedimentation of these limestones (Neoschwagerina craticulifera zone), the dominant environments were algal meadows of dasycladaceans and gymnocodiaceans. At several places on the platform mound, structures were formed. Among them, (sensu Salopek), or “early diagenetic supratidal there is an interesting patch-reef which is dolomites” (Tišljar et al., 1991), are well-bedded today well-exposed along the Gospić-Karlobag and rather poor in microfossils. In the lower road. portion of this sequence, Permian microfossils, Three phases of reef formation can be predominantly gymnocodiaceans, have been distinguished (A-C), and lentoid carbonate found. The uppermost portion contains small bodies were divided by clastic sediments- foraminifera typical for stressed environments. calcarenites (reef debris) and shales (Figs. 3.2 A continuous transition from the Upper Permian and 3.3). to the Lower Triassic, followed by an increase in the clastic component in dolomites, has Description of the reef complex P37 to P54 n° 5 - from Volume been indicated by previous authors (Salopek, The bluish-black limestones are bituminous 1942; Ramovš and Kochansky-Devidé, 1981). biomicrites (framestones), which overlie some Nevertheless, a lack of index species in the 10 m thick black shales with thin calcarenite uppermost dolomite beds leaves the question interbeds. The dolomitized parts are light grey in of the position of the Permian-Triassic boundary colour (Figs. 3.2 and 3.3). open. The sub-stratum, composed of skeletal debris and a muddy matrix, was fi rst colonized by tabular calcisponges, fenestellid bryozoans, and

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura (after Sremac, 1991). calcareous algae,gastropods, andbrachiopods hosted numerous reef-dwellers, suchasforaminifera, The reef frameworkmadeofencrustedframe-builders Figure 3.4-Martiniavelebiticainthespongecavity. The (cyanobacterial) crusts coattheorganisms. and crinoidsare alsopresent. Thickoncoidal as algae. Debriscomposedofcalcareous algaesuch The remaining inter-space is primary porosity wasreduced bythisprocess. gastropods, andbrachiopods(Fig.3.4).The such asforaminifera,calcareous algae, frame-builders hostednumerous reef-dwellers, The reef frameworkcomposedofincrusted later overgrown bycyanobacteria. organisms colonizedoncoidcrusts, butwere are crusts withwell-developedchamberlets,which micrite crusts withpoorlyvisiblelaminae,and Two typesofoncoidalcrusts canberecognised: calcisponges, fenestellidbryozoans,andalgae. and The reef limestoneslocallycontainlarge solution fi internal sediment,composedofcarbonatesilt, the reef frameworkare geopetally ne-grained calcarenite, andsparrycalcite. Mizzia fi fi ne-grained skeletaldebris.Somevoidsin lled withdolomite.Sometimessessile fi rst reef framebuilderswere tabular and č i ć Permocalculus, , LadislavPalinkaš fi lled withmicrite, rare gastropods fi le with lled The reef growth was shales, interpreted asstorm-beds(tempestites). The calcarenites are interbeddedwiththinblack sometimes cross-laminated, andsharptops. more-or-less well-developednormalgrading, by calcarenites ( their encrustants. Thereef bodiesare onlapped colonization bypioneeringorganisms, and to thebody breccia formschannelizedbeds(eg.laterally lithoclasts andincrusted organisms. Locally, the bounded byshale,richinscattered cobble-sized (Fig. 3.3).Thebody C fi Laterally, therole oftheskeletaldebrisin with siltandmud. places, ofprotruding incrusted organisms, are alsopresent. Thereef toprelief consists,in debris. Large bivalves clasts ofearlylithi bodies ischaracterizedbybreccias, composedof The reef topsurfaceofindividualsedimentary fl episodic exposures, andatmosphericwater developed withinthevadosezoneduring framework porosity, and“solutioncavities” “growth cavities”are remnants ofprimaryreef The genesisofthereef cavitiesistwofold;the debris andlithoclasts. (carbonate siltandcalcarenite), scattered skeletal fi cavities (somemore than30cmindiameter), probably aresult ofrapidrelative sea-levelrise. reefs buriedbeneaththickblackshales.Thiswas ne-grained matrixincreases, andthebody lled withlaminated ushing. laterallyturnsintoathincalcarenite bed Figure 3.5-Floatstonewithunsortedreef debris B ) asasubstrateforsubsequent fl oatstones, Fig.3.5),with fi ed limestonesandskeletal A, fi nally aborted,andthe however, endslaterally, Tanchintongia ogulineci fi n-rie debris ne-grained (after Sremac, 1991). 3-06-2004, 10:03:06 fi lled

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Milojević (1922) described what he interpreted as glacial deposits in the Paklenica canyon on the Velebit Mountain, and so also did Bauer (1934/35), and Degen (1936). Malez (1968) made a general statement that the mountain tops of the coastal Dinarides, including the Velebit Mountain, were glaciated during Pleistocene, Figure 3.6 - Rujno medial moraine ridge in the but provided no documentation. It is interesting seaward direction. to mention that J. Cvijić (1917) already described the glaciation of the southern Dinarides at the Short Scenario of reef-building beginning of the 20th century, but only in areas events over 1000 m a.s.l.. Poljak (1947), Leon Nikler The reef evolution can be summarized in 7 (1973), Belij (1985), and Bognar et al. (1999) phases: contributed greatly to the understanding of the 1) substrate colonization; phenomena. Recently, studied deposits along the 2) the formation of primary reef framework with Adriatic coast, interpreted as of glacial origin, dwellers; yielded evidence in favour of the glacial origin of 3) reef framework encrustation; these Quaternary deposits (Marjanac et al. 1990, 4) early lithifi cation; Marjanac and Marjanac, 1991). 5) shallowing (relative sea-level fall), followed by weathering and erosion; Geology of the area 6) infi lling of secondary reef porosity; The study area is part of an extensive karst 7) deepening (relative sea-level rise), followed region of the Velebit Mountain. Rather poor by recolonization (or fi nal burial as after reef vegetation cover allows a fairly good insight body C).

The Palaeozoic sediments of the Velebit Mt. can be considered as a foundation of the later carbonate platform environment, subsequently developed, here and elsewhere in the External Dinarides in the course of Mesozoic time. Quaternary glacial and associated deposits of Velika Paklenica and Rujno Ljerka Marjanac and Tihomir Marjanac Case history The earliest idea about the Mediterranean being infl uenced by glaciations, and so the Adriatic as being the northeast epicontinental sea, was introduced just as a hypothesis by Luis Agassiz (1840) in his discussion about glaciations. The idea that at least the highest peaks of the P37 to P54 n° 5 - from Volume Croatian External Dinarides were glaciated, dates back to 1899, and Albrecht Penck’s journey to the Dinarides. Hranilović (1901), Gavazzi (1903a,b), and Schubert (1909) also promoted the idea of glaciation on the Velebit Mountain, but it was not accepted by other researchers (i.e. Figure 3.7 - The Velika Paklenica Canyon (looking in a downstream-seaward direction). Gorjanović, 1902). Later on, geomorphologist

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura Triassic andJurassicwell-beddeddolomites valley developedwithinacomplexofUpper various olderdeposits.TheRujnoarea isalarge Paleogene age.Theytransgresively overlay massive topoorlybedded,ofsupposed carbonate Jelarbreccias andconglomerates, dolomites, andpyroclastics. Theyoungestare Triassic complexoftransgressive conglomerates, occurrence ofvolcanoclastics,andtheUpper Triassic limestonesandsandstones,withthe calcarenites; commonlyred coloured), Middle sandstones, siltstones,andshales,sandyoolithic by LowerTriassic clastics(micaceous tectonical structures. Triassic ishere represented to themainNW-SE strikeofthebeddingand Jurassic, andTertiary ages,nearlyperpendicular predominantly carbonaterocks oftheTriassic, Velika Paklenicahasbeendeeplyincisedinto into thegeologicalframework.Thecanyonof glacial striaewere foundthere. unsorted debris-Rujnomedialmoraine.Clastswith Figure 3.8-Trench showingglacially-derived, č i ć , LadislavPalinkaš basic geologicalmapofthearea (SheetGospi glacigenic originwhichare stated lithologiesinQuaternaryclasticsof V. PaklenicaandRujno,werecognized allthe our recent studiesofQuaternarydepositsin Upper Permiandolomites,are present. During clastics (conglomeratesandsandstones), In thevicinityofRujnoalsoLowerPermian such inthefollowingtext. with moraine ridge.Thewholevalleyiscovered parts, MaloRujnoandVeliko Rujno,byaglacial and limestones.Thevalleyisdividedintotwo Belij 1985). adopted alsobysubsequentresearchers (e.g., glacial byNikler(1973),andthatattributionwas The RujnomorainewasattributedtotheWürm meltwaters. which waslaterresedimented andsortedby leaving behindanextensivelagofcoarsedebris further downslopetowards loweraltitudes, the corresponding glacialtongueproceeded considered assuchinthispaper. Consequently, the characteristicsofamedialmoraine,andis (1973) andBelij(1985).However, itshowsall a.s.l., wasinterpreted asterminalbyNikler canyon), whichliesbetween830and950m The Rujnomoraine(NWfrom Velika Paklenica range is60to250cmindiameter. - erraticsare visibleonthesurface.Theirsize and shrub vegetation.Scattered large boulders (Lower Triassic). Theridgeiscovered withgrass Jurassic), andsmallred-coloured particles a predominantly darkgrey limestone(probably maximum diameterof25cm,isrepresented by of unsortedrounded debris,withanaverage conglomerate (ca.30%clay-siltmatrix).70% is anunconsolidated,matrix-supported phase ofglacialadvance.Thesediment accumulation), eachrepresenting adifferent of three “amalgamated”smallerbodies(debris glacially-derived material(Fig.3.8).Itconsists sedimentary body(ridge)composedof Rujno moraine and theV. Paklenicacanyon(Fig.3.7). we willrefer strictlytoRujnovalley(Fig.3.6), but regarding thepresent stateofexploration, broader surroundings ofRujnoandV. Paklenica, Quaternary depositscanbefoundwithinthe Sediments andtheirorigin fl uvioglacial sediment,according tothe is anelongatedcomposite fi rst describedas 3-06-2004, 10:03:18 ć ). ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

Velika Paklenica moraines occur almost along fi lled with such large boulders and cobbles. the whole length of the canyon. They change in Washed-out fi nes and gravels were transported composition from the proximal to distal part of by streams, and accumulated in alluvial fans in the canyon, depending on the source area from front of the Paklenica Canyon, today the area of which the ice was coming from. This regards Starigrad. the various lithologies of Permian, Triassic, or Jurassic eroded by ice advance and meltwaters DAY 4 during the ice retreat. Thus the moraine in the Geography and hydrogeography proximal canyon is a typical diamictite, and of the Neretva Delta matrix-supported, with a high clay content, and Gordana Pavlović and Esad Prohić derived from Lower Triassic clastics. Towards the distal canyon part (seawards), diamicts This delta borders the Adriatic sea (taking up become 90% carbonate in composition, with little about 25 km of coast), south-eastwards from matrix, or they turn to openwork conglomerates the town of Ploce at the southern extremity of (matrix washed out). Clasts of Lower Triassic the Dalmatian region. It extends inland for 20 rocks become very rare, because they are softer km, before reaching the boundary of Bosnia and easily weathered during transport. Jurassic Hercegovina and the lower end of the Neretva limestones and dolomites predominate, and valley. clasts are much larger, commonly rounded The area is characterized by coastal salt marshes, boulders over 1 m in diameter. Sediments are saline lagoons, sandbanks, and wet meadows. It more or less cemented. Distally downstream, is surrounded by Karstic hills, overgrown with moraine is commonly reworked, redeposited and degraded forest. The mean annual temperature sorted, so it becomes clearly bedded. In several is 16° C (winter 8°C, summer 24°C), with an places, an alternation of diamicts with boulders annual precipitation of 1312 mm (winter 160 and intervals of reworked moraine are visible, mm, summer 45 mm). Winds are generally from which probably represents several phases of ice the east, occasionally from the west. Winters are advance and retreat. An excellent section of the moist and mild with hot, dry summers. There is road cut shows two such intervals, a glaciofl uvial in the valley a network of small karstic lakes, conglomerate beneath an unsorted diamict with some permanent, others only temporary. The large rounded boulders, here interpreted as basal whole delta area (500,000 ha) has a very complex moraine. A sediment wedge in the glaciofl uvial hydrographic system with some waters being conglomerate was recognized and interpreted oligotrophic, and others brackish. as a possible ice wedge fi lled with coarse debris The Neretva River has its source beneath the during ice advance. Zelengora Mountain in the east of Bosnia and The most impressive remnant of an end moraine Herzegovina (Fig. 4.1). Whereas its upper and in the V. Paklenica canyon (Marjanac and middle courses are characterized by canyons and Marjanac, 1999), is visible below Anića Kuk (a cliffs, its lower course is a vast wetland valley. The well-known rock-climbers’ wall) at the forehead river fl ows further downstream through its large of Anića Luka. It is about 250 m a.s.l., and delta into the Adriatic Sea. It is the largest river probably represents Early or Middle Würmian of the eastern part of the Adriatic basin. Along glaciation. This one is composed of cobbles and its course there are several HE power-plants, boulders 1 to 10 m in diameter (the largest one and their storage lakes. Downstream from the being 22 m) “fl oating” in a gravel/arenite size infl ows of its tributaries Trebižat and Bregava, P37 to P54 n° 5 - from Volume “matrix”, which is well-cemented. Boulders and the Neretva valley extends into an alluvial fan, cobbles are subrounded to rounded, commonly “Neretvanske blatije”, with the area of 20.000 ha. spherical to oval, and poorly-sorted. At the back Its northern part, called Hutovo Blato, belongs to of the moraine (upstream), there are remnants of Bosnia and Herzegovina, whereas in its southern glaciofl uvial/fl uvial terraces. The moraine itself part, which is situated in Croatia, the Neretva has been partly destroyed. Running waters have River forms a large delta (Fig. 4.2). washed out the fi nes, and collapse of large clasts The last deglaciation caused a sea level rise, has occurred. Thus, today we can see the canyon whereby sea water covered the karst relief as

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura species. delta, someofthembeingEuropean endangered 310 birdspecieshavebeenregistered intheNeretva feeding ofmanysorts high biologicalproduction oftheriverresults inthe spreads overanarea ofapproximately 12.000ha. The Figure 4.2-ThedeltaoftheriverNeretva inCroatia biggest andmostpicturesque ontheMediteranean. River, withitsemerald green, wildwater, cutsDinarideswithadeepgorg,e andentersawidedelta,oneofthe Figure 4.1-Mostar, historictown,owesitsnametothefamousbridgeover theNeretva valley. TheNeretva č i ć , LadislavPalinkaš fi sh attheNeretva mouth. delta, where brackishwaterisauniquehabitat have disappeared. Thesealargely in earlier twelve,whereas manylagoonsandlakes only three brancheshaveremained outofan over anarea ofapproximately 12,000ha.Today, The deltaoftheRiverNeretva inCroatia spreads natural processes havebeenupset. many animalspeciesare vanishingandmany and itdoesn’tfunctionasusedtodo,namely this ecologicalsystemintomostlyarableland All sortsofanthropogenic activiteshavechanged these wetlandsare threatened withdestruction. stress ofintensivecultivationandurbanization, the eastern Adriatic coast.Beingunderthehuge the mostspectacularMediterraneanwetlandson of theNeretva valleyconsistofthelargest and the valleybyNeretva River. Thelowerparts fi far astothepresent HutovoBlato.Gravelsand ne-grained sedimentshadbeendepositedin fl uences the 3-06-2004, 10:03:29 ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

which contributes to the biological diversity of the area. The high biological production of the river provides for the feeding of many sorts of fi sh at the Neretva mouth. 310 bird species have been registered in the Neretva delta, some of them being European endangered species. In spite of its deteriorating condition, this area still represents an exceptional example of the biological and landscape diversity for which it is internationally renowned. The lower Neretva valley was included in the Ramsar List of the Ramsar Convention on Wetlands, as well as in the Programme “Important Bird Areas’, Figure 4.3 - The town of Korčula, birth place of Marco conducted by the “Bird Life International” Polo, founded in Neolitic times, with its cultural and organization. historical heritage, under Greek, Roman, Byzantine, Croatian, Hungarian, Bosnian, Venician, French, Stop 4.1: British, Austrian, Italian and fi nally again Croatian Delta of the Neretva River rule, ranks among the favourite tourist destinations The Neretva River emerges from beneath the in southern Croatia. Zelengora Mountain in eastern Bosnia and Herzegovina. Through canyons, cliffs, and meadows, beaches, sand-banks, and saltmarshes, hollows in its upper and middle courses, it as well as the adjacent karst overground and forces its way through the Dinaric Alps to spread underground, present a wide variety of habitats, downstream from the village of Pocitelj in that is the basis for an adequately wide variety of Herzegovina, over a vast wetland valley, and to plant and animal life. fl ow through its large delta into the Adriatic Sea. Neretva is the largest river of the eastern part of Stop 4.2: the Adriatic basin. The Ploče region The Neretva Delta in the Republic of Croatia Stratigraphically and structurally, this study covers about 12,000 ha. Today, in this cultivated area belongs to the geotectonic unit of the Outer area, only fragments of the earlier large Dinarides. The recent tectonic setting is highly Mediterranean wetland are preserved. Five sites complicated, as numerous tectonic phases have with a total area of 1,620 ha, are protected in the left traces in this area. There are four tectonic categories of ornithological reserve. units on the sheet Ploče: Biokovo, Biokovska Here, the natural values, and the diversity of Zagora, the Makarska littoral, and the central habitats, depend in the fi rst place upon the water Dalmatian islands. regime affected by the Neretva River. Owing to The fl anks of the Neretva valley are made up of many underground karst streams of the basin, in Mesozoic karst limestone, while the bed itself is the part adjacent with the surrounding limestone covered by younger alluvial deposits. terrain, there are a large number of springs The Quaternary is represented by lacustrine, carrying large amounts of water, especially in alluvial, and deltaic sediments. Alluvial deposits winter. The ground water coming from this consist of the lithologically-heterogenous adjacent area supplies numerous streams, lakes, complex, dominantly composed of clayey sands P37 to P54 n° 5 - from Volume and cavities. Many caves and other underground and silts. A thick and complicated, lithologically habitats in the surrounding karst are home for heterogenous delta complex has been deposited rich fauna with many endemic species. at the mouth of the River Neretva. This is where An important factor affecting the delta is the sea, the sediments of saline, potable, brackish, and the bodies of brackish water represent special and lagunar waters mix with corresponding habitats which contribute additionally to the organisms. The material, carried by the river, biological diversity of this whole area. Aquatic is being deposited towards the west, i.e. habitats, together with large reed-patches, wet towards the direction of its course. The territory,

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura Greek habitationsinLumbarda, inthevicinity island wascalled the 6thand5thcenturiesBC;atthattime the Bronze Age. A Greek colonyexistedhere in Špilja abovethecoveofRasohatica,Žrnovo)and (cave Vela ŠpiljanearVela Luka,caveJakasova The islandwasinhabitedasearlytheNeolithic the islandofKor major placesontheisland.Ferrylinesconnect and Pupnat(Fig4.3).Theregional road connects and intheinteriorBlato,Žrnovo,Smokvica,Cara fruit growing, The economyisbasedonfarming,viticulture, fl island islargely covered withMediterranean of sunshinereach 2,671hours(Vela Luka).The annual rainfallis1,100mm;thehours coast are Kor has beenrecently developed.Majorplacesonthe long traditionontheisland;nauticaltourism materials, andtourism.Summertourismhasa shipbuilding, theprocessing ofsynthetic of Kor temperature inJanuaryis9.8°C(inthetown (510 m).Theclimateismild;anaverageair highest peaksare Klupca(568m),andKom of 17,038;andthecoastisratherindented.The (length 46.8km,width5.3-7.8km);apopulation archipelago; ithasanarea of279.03sqkm Kor Sabina Strmi Island ofKor Stop 4.3: up untilrecently. started asearlyPleistocene,andhascontinued lithological types. Accumulation ofthismaterial the boundariesbetweengeneticallydifferent more than30meters.Itisnotpossibletoplace thickness ofthecomplexisestimatedtobenot exhibiting cross strati ora; atsomeplacesthere are pineforests. č ula isanislandinthecentralDalmatian č ula) andinJuly26.9°C;theaverage č ć č ula, Lumbarda, Vela Luka,Ra ula č i ć č fi , LadislavPalinkaš sig and shing, ula withthemainland. Korkyra Melaina fi cation. Theentire forti the beginningof18thc.),severalimportantpointsonislandwere in Figure 4.4-Duetofrequent attacksoftheTurkish deltaic deposits, of mosttypical the sedimentation characterized by high tides,is the ebbsand fi s processing, sh fl une by uenced fi ed (especiallythetownofKor (remains of č ište, best worksfortheirowncity. buildings alloverDalmatia,buttheysavedtheir left theirmarkinstoneworks,sculptures, and stonemasons, shipbuilders,andseafarers. They involved. ThepeopleofKor writer, mainstays forcenturies.Thefamoustravel eastern coastoftheisland)havebeenimportant (extraction ofwhitemarblefrom aquarryonthe sources, borninKor (town ofKor Croatia. As forthelocaleconomy, shipbuilding the favouritetouristdestinationsinsouthern (similar tothoseofDubrovnik) ranksamong and historicalheritage,itstownramparts forti c.) ,severalimportantpointsontheislandwere pirate ships(alluntilthebeginningof18th Due tofrequent attacksoftheTurkish was underVenice, butitretained itsautonomy. (1413-1417). Intheperiod1420-1797,island rulers (1390),andtheDubrovnik Republic of Lumbarda, Vela Luka(localityBene settlements havebeendiscovered inthevicinity was partoftheRomanEmpire; tracesofRoman of BlatoandinPotirna).From 35BC,theisland island, thetownofKor that wasannexedtoCroatia. Thecentre ofthe occupation intheperiod1918-1921,andafter Kor 1918 Austria). 1805-1813 France,1813-1815Great Britain,1815- period ofvariousrulers (1797-1805 Austria, 4.4). After thefallofVenice, there wasanother the Genovese several rulers from Zahumlje,Venice (in1298, From 1221,overtwocenturies,theislandhad statute ofthetownandislandwere passed). under theHungarian-Croatian king(in1214the AD 1000,byVenice. In1180 theislandcame it wastakenbytheNerentani/Narentini, andin under Byzantinerule (AD555).Inthe9thcentury, of theOstrogoth state(AD493),andthencame Western RomanEmpire, theislandbecamepart Blago, andonPelegrin.Onthecollapseof near Kor fi ed (especiallythetownofKor Marco Polo č ula), KingLodovicI(1358),Bosnian č ula). č ula, Vela Luka)andstonecutting fl eet defeatedtheVenetian , whowas,according tosome č č ula wasundertheItalian ula, wassaidtohavebeen fl eet andpirateships(until č ula, withitscultural č ula were famous č ula) (Fig fl eet and eet 3-06-2004, 10:03:33 fi fl cij), eet ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

western and eastern thirds of the island are lower, but the highland features are also present in the relief and landscape. The climate is Mediterranean with warm, dry summers and mild, wet winters. The average annual precipitation is 973 mm and the annual hours of sunshine are 2,500 hours. The main motives for proclaiming the island a national park were because of its highly indented coastline and rich plant life that abounds in the forests. From the open sea and through a barely Figure 5.1 - The little isle of St. Mary in the Great Lake, with an ancient Benedictine monastery, and a visible passage, the sea seeps into the mainland church dating from the 12th century. This small island to form the Veliko Jezero (Fig 5.1), which covers has become the symbol of the entire Mljet island, 145 hectares and is 46 metres at its deepest, and because of its exceptional aesthetic qualities, and the Malo Jezero, which covers 24 hectares and is strong cultural and spiritual dimensions. 29 metres at its deepest point. Although fi lled with seawater, both are perceived as lakes, as DAY 5 even their names – “jezero” (“lake”) confi rm. Lakes are the most interesting, but certainly not Stop 5.1: the only feature of the coastal indentedness and Island of Mljet landscape of the National Park. There are also Sabina Strmić Figure 5.2 - Geological map of Mljet Island (data Mljet was proclaimed a national park on 12th from Korolija et al., 1976, 1982; partly modifi ed and November 1960. It covers an area of 3,100 updated), Explanation: 1. Upper Jurassic limestone, hectares on the northwestern third of the island 2. Jurassic-Cretaceous dolomite, 3. Lower Cretaceous of Mljet, one of the largest islands in southern limestone, 4. Alternation of Cretaceous limestones Dalmatia. The island is made of strata of and dolomites (Albian - Cenomanian), 5. Pleistocene limestone and dolomite. The limestone created quartz sand, 6. Normal geological boundary higher ground; the dolomite created most of the – continuous transition, 7. Strike and dip of beds, 8. Faults, 9. Profi les: depressions, i.e. the fi elds. The central part of A-B and C-D (geological), E-F (hydrogeological), Mljet is a highland, with three parallel ranges. 10. Fresh-water spring, 11. Brackish spring, The highest point is Veliki Grand (514 m). The 12. Supposed directions of underground water-fl ow. Volume n° 5 - from P37 to P54 n° 5 - from Volume

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura Malo Jezero. sunnier slopes,andaround theVeliko Jezero and island, andespeciallyonthewarmer, more ( forest, primarilybyindigenous Aleppo pine Park. NinetypercentoftheParkiscovered in of theisland,whichborders theMljetNational such anameshouldbegiventothewesternside Mljet isalsocalledTheGreen Island.Credit for area of122.7hectares. numerous coves,bays,andisles,coveringatotal coastal cliffs tothesouthandsouthwestof limestones (about150myb.p.),thatformthe The oldestsedimentsare UpperJurassic the NNE(Figs.5.2,5.3). have aWNW-ESE zonalstrike,anddiptowards Mesozoic carbonatesare ingeneralwell-bedded, developed coverofQuaternarydeposits. carbonate rocks, withathinandsporadically It isbuiltupofUpperMesozoicplatform Mesozoic carbonateplatforms(Jenkyns,1991). of thelargest andmostlong-lastingTethyan Dinaridic carbonateplatform,whichwasone The islandofMljetisapartthe Adriatic- Ivan Guši Geology oftheMljetisland Pinus halepensis ć č i ć ), whichisfoundalloverthe , LadislavPalinkaš Cuviller palastiniensis Henson necessarily muchlarger than1-2mm): called larger benthicforaminifera(thatare not Favre of thegreen dasycladalga their upperpartsthere are abundantremains by thetransitionaluppermostJurassic(Upper 150-200 mthick,andare conformablyoverlain prove theirLateJurassicage.Theyare about alga Praekurnubia cruseiRedmond and contain,intheirlowerpart,theforaminifer Upper KimmeridgiantotheTithonian, Babino Polje.Theyrange,inage,from the limestones, 3.Jurassic-Cretaceous dolomite,4.Lower pro limestone anddolomite(mostlyUpperCretaceous), Cretaceous limestone(withbreccia, conglomerate, and dolomites(onlyinpro Mljet. Explanation:1.MiddleJurassiclimestones fi 6. Tertiary limestoneand les), 7.Faults:left-normal,right-reverse; arrows and,sporadically, twospeciesoftheso- Salpingoporella? sellii Figure 5.3-Geologicalpro and dolomiteintercalations), 5.Alternationof geological columnoftheMesozoicdeposits , Foury and indicate relative movementofrocks, and Pignatti Morano ( Parurgonina caelinensis 8. Geologicalboundary. Crescenti fl fi ysch deposits(onlyin les), 2.UpperJurassic andthedasyclad fi les andschematized Clypeina jurassica ),whereas in Kurnubia , which 3-06-2004, 10:03:37 ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

Tithonian)-lowermost Cretaceous (Lower ostreid bivalve, Chondrodonta joannae Choffat. Berriasian) late diagenetic dolomites, indicating All these carbonate sediments, both Upper extreme shallowing (and sporadically emerging) Jurassic and Cretaceous, originated in shallow conditions at the Jurassic-Cretaceous boundary. marine (shallow subtidal to intertidal) These dolomites make up the largest part of the environments (shoals, sand bars, backreef NW part of the island, but also extend further to lagoons, etc.) of the Tethyan south-margin the SE, from the area of the National Park to the carbonate platforms, situated in a tropical sea, west, to the environs of the Maranovići village by the accumulation of both carbonate mud to the SE. These dolomites, about 400 m thick, and organic (skeletal) remains, resulting in the are, in turn, conformably overlain by a thick production of predominantly mud-supported sequence of Cretaceous limestones, that build up types of limestone (wackestone to mudstone), the northern and northeastern part of the island whereas the grain-supported types (packstone (including, also, most of the area of the Mljet to grainstone), indicating short-lasting phases lakes). The Cretaceous limestones also form the of more agitated water and probably caused highest mountain ridges of the island (Veliki by periodical storms, are much rarer. Such Grad, 514 m) and dip toward the NNE into the types of sedimentation correspond to what is sea (the Mljet Channel). usually called a continuous (uninterrupted) The Cretaceous limestones, sporadically sedimentation, though several minor gaps, interbedded with dolomite intercalations, make indicated by fenestral structure, vadose an 800 m thick, layer-cake type of sequence, features, and black pebble occurrences (Tišljar, ranging, stratigraphically, from the Berriasian 1986; particularly in the Barremian-Aptian (approx. 140 my b.p.), to the Upper Cenomanian part of the sequence), have been recorded. (approx. 93 my b.p.). Chronostratigraphically The sedimentation lasted approximately 50 speaking, all Lower Cretaceous stages are million years or slightly more, the highest paleontologically well documented with outcropping part of that “continuous” numerous species of green dasyclad algae and sequence just preceding the temporary fl ooding “larger” benthic foraminifera, well-known from (drowning) that would spread over the entire other Tethyan regions. (especially abundant are Adriatic-Dinaridic carbonate platform at the species of the dasyclad genus Salpingoporella, Cenomanian-Turonian boundary and in the and foraminifera of, or related to, the genus Early Turonian, respectively (probably caused Vercorsella, whereas orbitolinids, that are by the global--eustatic—sea level rise; Jenkyns, otherwise one of the most widely distributed and 1991; Gušić and Jelaska, 1993). We predict that stratigraphically most useful Tethyan Cretaceous the sediments indicating the Lower Turonian foraminifera, are relatively scarce). drowning event should be present under the sea The Upper Cenomanian deposits, which surface, in the Mljet Channel, not far from the NE make the youngest outcropping part of that coast, but this remains to be proved. uninterrupted Cretaceous sequence, contain Only in the most NW part of the island, west abundant remains of the well-known Tethyan and northwest of the Polače bay, and including the islets at the northwestern tip of the island (Glavat, Maslinovac, Moračnik, Ovrata), younger Upper Cretaceous (Upper Santonian) sediments crop out Volume n° 5 - from P37 to P54 n° 5 - from Volume (not shown in Figs. 5.2 and

Figure 5.4 - Schematized hydrogeological profi le of Mljet Island. Explanation: 1. Mostly limestones, 2. Dolomites, 3. Supposed directions of underground water-fl ow, 4. Supposed level of underground water.

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura From theregional-geologic andtectonicpoint limb ofasouthwestwardly overturnedfold. the NE.Itrepresents anortheastern,normal, Structurally, Mljetisamonocline, tiltedtowards periodically inundated. Prožura), orSlatina(nearKozarica),whichare and uvalas,calledBlatina(nearBlata,Sobra, clay andsiltcanbefoundinsomekarstdolines environment. Recent(Holocene)sedimentsof origin, butwere depositedinashallowwater (Pleistocene) age.Theyare probably ofEolian deposits ofquartzsandEarlyQuaternary in theSaplunaraandBlacaCoves,there are environs ofMaranovi In thesoutheasternpartofisland,in Scandonea samnitica by thepresence ofthelarger benthicforaminifer another tectonicunit.Theiragehasbeenproved Cenomanian limestones,andtheybelongto 5.3). Theyare intectonic(fault)contactwith č i Figure 5.5-LocationandbathimetryoftheMljetLakes(afterVuleti ć , LadislavPalinkaš . ć i, Korita,andespecially distinguished from thesandyandclayeydeposits compact, hard, andstablerocks andare clearly characteristics, thelimestonesanddolomitesare According totheengineering-geological accumulations. fl are nosigni accumulation ofwaterisnegative,andthere in setting inthemiddleofMljetmonocline, 5.4). Becauseoftheirsuperpositionallayer-cake and relatively lowpermeabledolomites(Fig. Mljet isbuiltupofhighlypermeablelimestones, Concerning thehydrogeological characteristics, (Fig. 5.3). Paleogene FlyschandNeogenemarinedeposits is thrust overtheyounger, clasticsediments— a fewmilessouthwestwardly from theisland,it strikes belowtheseainaNW-SE direction, and of view, Mljetbelongstoalarge overthrust that ows, norsigni fl uence ofthedolomiteuponunderground fi cant springsorsurfacewater fi cant subsurfacefresh-water ć , 1953). 3-06-2004, 10:03:44 ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

with their changeable physical qualities. are encountered (Vaniček et al., 2000; Ćosović et Mljet is certainly infl uenced by two epicentral al., 2002). localities: the environs of Dubrovnik and the mouth of Neretva River. Earthquakes of up to Lake formation VIII MSC (destructive) in the western, and up Lake morphology, along with a knowledge of to IX MSC (ruinous) in the eastern part of the the geodynamic evolution of the broader area, island are possible. allows us to reconstruct how and when the lakes originated. Depressions in which marine lakes Stop 5.2: are located are typical karstic depressions (dolina Recent carbonate sedimentation in the and uvala), developed in Mesozoic limestones lakes of Mljet Island and dolomites. One can assume a tectonic Mladen Juračić predisposition of the location of depressions, Veliko and Malo jezero (Large and Small Lake, and a subaeral corrosional process in the i.e. Mljet Lakes) are located in the western part development of depressions. Therefore, the of the Mljet Island (Adriatic Sea) (Fig. 5.5). Due formation of deep dolinas (sinkholes), occurred to its scenic beauty, ecological peculiarities, and while their bottom was above sea level. In the environmental values, this western part of the time span since the formation of limestones, island was proclaimed a National Park in 1960. there have been several such periods. But, as The Mljet Lakes are semi-enclosed, relatively the corrosional geomorphological processes in deep depressions, connected with the open sea limestone terrains are quite fast in humid climatic by a narrow, shallow Soline Channel. Being conditions, it can be presumed that periods in connected with the sea, they contain saline water near geological history with lowered sea level and, therefore, are not true lakes. However, had an important role in their morphogenesis. due to their depth (46 and 29 m respectively), During Pleistocene, the sea level repeatedly they can hardly be termed lagoons, because oscillated, and during glacials, was up to 140 the latter are usually defi ned as shallow semi- m lower than the present level. During the Last enclosed water bodies (Phleger, 1969), “having Glacial Maximum (LGM), between 30,000 and depths that seldom exceed a couple of meters” 19,000 years before present (y BP), the global (Kjerfve and Magill, 1989). Therefore for sea level was approximately 130 m lower than these, and other similar marine water bodies present (Lambeck et al., 2002). Most probably, apparently disconnected with the sea, found dolinas in which today’s lakes have been along the eastern Adriatic coast (e.g. Mir Lake formed, were remodelled, if not formed, during on Dugi otok, Dragoon (Rogoznica) Lake near last glaciation. In those times, karstic corrosional Rogoznica), a term marine lake was proposed processes must have been intensive, and sinking (Vaniček et al., 2000). water with dissolved carbonates drained Most of the water exchange between the Mljet underground towards the sea, which was SW Lakes and the sea under current climatic from Mljet Island. It has been generally accepted conditions occurs through very shallow, narrow that the sea level rise was very fast and steplike straits. The Veliki most (Large Bridge) strait from 18,000 to 6,000 yBP (with an average of 1 cm between the Soline Channel and Veliko jezero is y-1, but with jumps of over 4.5 cm y-1; Blanchon 10 m wide and 2.5 m deep, whereas Mali most and Shaw, 1995), while afterwards, the sea level (Small Bridge), the strait between Veliko and rise attenuated. During Lower Holocene, from Malo jezero is even smaller: 2.5 m wide, and 0.5 10,000 to 6,000 yBP, conditions were favourable Volume n° 5 - from P37 to P54 n° 5 - from Volume m deep. Tidal currents drive water exchange, for the formation of Mljet freshwater lakes and the mixing is constrained only to the surface (similar to the present-day Vrana lake on Cres layer. Due to the summer heating of the surface Island; Wunsam et al., 1999). The seal evel and layer, water stratifi cation develops, which the groundwater level (i.e. erosional base), rose gives rise to temporary stagnant conditions, above the bottom of the dolinas and hindered the with hypoxia and even anoxia in the bottom subsurface draining of rainwater. Depending on waters (Benović et al., 2000). Therefore, stress climatic conditions (humid/arid), percolation of producing environmental factors for organisms freshwater towards the sea or seawater towards

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura dissolved oxygen,butH water deeperthan19mintheMalojezero, no 2001). of terrestrial origin)andpyrite(FeS organic matter(organic detritus,presumably Dark laminaehaveelevatedconcentrationsof laminae corresponds tooneyear. that thosewere varve,i.e.thatonepairof detail bySeibold(1958).Bothofthembelieved them, andafterwards theywere describedin 1953). Suchsedimentsare characteristicfor anoxic conditions. After Vuleti environment intheMljetLakesisdueto The peculiarityofthesedimentation Veliko jezero. 1953). A similarsedimentpatternisalsofoundin stagnalis and freshwater/brackish snailslived( which marshyplants(Chara/Nitella) there were freshwater/brackish conditionsin in theSolineChannel,indicatethat4600yBP of theinvestigationsubbottomsediments men diggingthenarrow isthmus.Newresults between Veliko andMaloJezero wasdoneby sea (SolineChannel)andVeliko Jezero, and a possibilitythattheconnectionbetween currents through theSolineChannel.There is water betweenthelakesandseaduetotidal position, andenabledthesurfaceexchangeof the sealevelreached approximately itscurrent recently (inthelast2,000to4,000years),when formation ofmarinelakesoriginatedrelatively Additional preferable conditionsforthe the lakescouldoccur. Malo jezero), parts (uptothemaximumdepthof29min sandy) sedimentsprevail, whereas indeeper up toadepthof20m,coarse-grained(gravelly- interesting. InMalojezero, inshallowerparts encountered intheMljetLakesare rather Sedimentation conditionsandsediments in theMljetLakes Sediments andsedimentation found. Vuleti white laminae(upto7pairsin1mm!)was a microlamination withalternatingdarkand of anoxia.Inthesedimentcore from Malojezero, encountered. Itindicatestheepisodicformation anoxic conditionsinthewatercolumnwere not However, duringsubsequentinvestigations, , Ventrosia cissana fi ć ne-grained mudisfound(Vuleti č (1953)wasthe i ć , LadislavPalinkaš ) (Govor fi rst toregister 2 ć S wasfound. (1953),in č fl 2 in etal., ourished, ) (Vuleti Lymnea ć ć , , presumed after However, asedimentationrateof2.6mm/y material. when rainwaterwashesawayterrigenousplant were depositedduringautumnandwinter column. Seibold(1958)presumed thatthey sedimentation inanoxicconditionsthewater al., 1989),iswhetherprecipitation ofaragonite al., 1997).Thelong-lastingdilemma(Shinnet or inalkalinefreshwater lakes(Thompsonet seas (Bahamas,Florida,Persian-ArabicGulf), registered onlyeitherintropical andsubtropical Aragonite deposition,uptonow, hasbeen found inthesediments. calcite andMg-calcitebiogenousfragmentswere However, alongwitharagoniteneedles,different matter samplesbothinMaloandVeliko jezero. Aragonite needleswere foundinsuspended during socalled“whitings”oflake(sea)water. of aragonitecrystals,presumably precipitated con crystals 8µmlong.Newinvestigations mineral present wascalcite,andinrhomboedric the x-raydiffraction analysis,statedthatthe events occurred more frequently. Vuleti It indicatesthatinformerperiods,anoxic core ,microlamination hasbeenregistered. anoxic events),whereas deeperinthesediment instrumentally registered episodichypoxicand oxic conditionsprevail (however, with Today, inthewatercolumnVeliko jezero, (e.g. phytoplanktonbloom,heavyrain). but asaconsequenceofdiscrete episodicevents formed episodically, notnecessarilyseasonally, from Malojezero, indicatesthatlaminaewere in sediments.The laminae foundinalternationwithdark the MljetLakesisoriginandnature ofwhite Other interesting sedimentationcharacteristicsin of 2.6mm/yinMalojezero. is inrangewiththepresumed sedimentationrate mm/y inVeliko jezero usingtephralayers,which calculated asedimentationrateof1.03to3.17 (1958, p109)refuted Vuleti with H jezero only. Aragonite depositionwasconnected deposition ofaragoniteisrestricted totheMalo (“drewit”) formedbysinglecrystals,andthatthe that whitelaminaeconsistofaragonitemud the existenceofaragonite,andpresumed Mljet Lakessediments(Vuleti fi rmed thatwhitelaminaeare composed 2 S saturatedwater. However, Seibold 137 Cs distributioni8nsediment fi rst investigationsofthe ć , andaccording to ć , 1953),indicated ć 3-06-2004, 10:03:50 (1953) ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

needles is physico-chemicaly induced (e.g. Milliman et al., 1993) or biologically governed (e.g. Stockman et al, 1967; Thompson and al., 1997). Another peculiarity of the sedimentation in the lakes indicating warm water infl uence is a large recent colony (aprox.600 m2) of coral Cladocora ceaespitosa that makes a coral bank (reef). It is located at the entrance to the Veliko jezero at depth of 5 to 10 m. In the shallow channel area (Soline Channel) on Figure 6.1 - The city of Dubrovnik. the sea bottom, biogenous, well-sorted carbonate sand is found, which forms symmetrical ripples, of maritime and mercantile centers in the with a “wavelength” of 3-6 m. They are formed Mediterranean and the Adriatic, and Dubrovnik most probably due to relatively strong tidal was one of them. During the 15th century, currents in the channel. In the open marine Dubrovnik became the most signifi cant seafaring environment at the entrance to the Mljet Lakes at and mercantile center in the Adriatic, third only a water depth of 38 m, coarse-grained, biogenous, to Venice and Ancona. very poorly sorted sand (with a substantial share A small sovereign state without an army brought of fragments larger than 2 mm) is found. It rests its defensive system to perfection by skilful on the seabottom below wave base. diplomacy and wide consular activities. The One can conclude that the sedimentation rate 16th century was the golden age of the Republic in the Mljet lakes is relatively high (sediment of Dubrovnik, as the splendour and power of the cover exists on the whole bottom, excluding Venetian Republic declined. Dubrovnik reached only the submarine elevation NE of Sv. Marija an impressive level in its urban and architectural islet). Coarse-grained, prevalently biogenous development, which has been sustained to the sediments prevail in the shallower and coastal present day. zone, whereas in deeper parts, the accumulation In the 17th century, a general crisis in maritime of mud, of both biogenous and terrigenous affairs in the Mediterranean and a disastrous origin, occurs. earthquake, forced the Republic of Dubrovnik to In order to obtain the whole picture of recent fi ght for its existence and for political protection and subrecent sediments in Mljet lakes, it would of its sovereignty. In the 18th century, Dubrovnik be necessary to make subbottom profi ling found an opportunity for economic revival in to determine the thickness of the Holocene sea faring trade under a neutral fl ag, before the sediments, and fi nd out if older Pleistocene arrival of Napoleon and the fall of the Republic sediments exist in deeper parts of the lakes. of Dubrovnik in 1808. At the Congress in Vienna in 1815, the region of Dubrovnik became a part DAY 6 of Dalmatia and Croatia, and it has been sharing City of Dubrovnik the same political destiny with them ever since. Following the proclamation of independence of the Republic of Croatia and the Serbian The city of Dubrovnik is situated in the very aggression in Croatia, Dubrovnik was attacked south of the Republic of Croatia. The favourable in October 1991. Today the cultural and historic

geographical position of Dubrovnik has made P37 to P54 n° 5 - from Volume heritage of Dubrovnik, which was barbarously its development based on maritime and trading damaged during the aggression, has been mostly activities very successful throughout its history. renovated. New archaeological excavations have proved Dubrovnik has preserved the beauty of a that the settlement in the foundation of today’s medieval town (Fig 6.1). Its outstanding cultural city existed in the 6th century or even earlier. and historical monuments have earned it a place The intensifi ed traffi c between the East and the on UNESCO’s World Heritage List. West during and after the Crusade wars in the 12th and 13th centuries, induced the prosperity

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura carbonate rocks, with a complexofverypermeable it ispossibletodifferentiate In ahydrogeological sense, with dipanglesfrom 20°-50°. inclination towards theNE, typical Dinaricstrikeandbed catchment area. Theyhavea Carbonate rocks prevail inthe of theOmblaspringarea isQsr=24.4m into theunderground. Theaverageannualyield which enablesdirect in of ponors(swallowholes),pits,and numerous shallowsinkholes,andtheremnants 1977). Thelargest partofthecatchmentcontains deposits (Markovi different typesofQuaternary Eocene Eocene carbonaterocks, Jurassic, Cretaceous, and consists ofUpperTriassic; The terrainoftheOmblacatchmentbasin Bonacci, 1994). and themaximumQsr=138m Ombla isatthelowestpoint.The in thespringarea are eroded tosealevel,and thick Eocene Mesozoic carbonaterocks wichthrust ontoa karst springoccursontheboundarybetween region. Ityieldsmore than139m karst waterobjectinthesouthern Adriatic The springoftheOmbla(Fig.6.2)islargest Renato BuljanandTomislav Paviša The springoftheOmbla Stop 6.1: minimum yieldmeasured wasQmin=3.0m in Israelisnotmore than70m Just forcomparison,thetotalwaterconsuption supply, andafuture hydroelectric powerstation. clear water, whichprovides formunicipal spring catchmentisabout600km at Trebišnjica, thesurfacearea oftheOmbla After theconstruction ofthehydro-system the waterisdischarged atdifferent levels. levels, thespringsfunctionindependentlyand water discharged atOmbla.Duringlowwater Crkvica; theprincipalspringyields80%of Glavni izvor(Theprincipalspring),Baba,and consists ofthree zonesofconcentrateddischarge: m abovesealevel.Thespringarea ofOmbla laterally totheeastandwestrisemore then150 fl ysch deposits,and fl č ysch complex.The i ć , LadislavPalinkaš ć , 1971). fi ltration ofrainwater 3 3 /s. Thistypical /s (Žugajand 3 /s ofperfectly 2 (Milanovi fl fl yc beds ysch yc beds ysch fi 3 ssures, /s. The 3 /s, ć , Figure 6.2-Front oftheoverthrustaboveOmblaspring. tectonic transportofthezoneisevident.The NE-SW alongthelineOmbla-Hum.Sinistral fault, andtherelatively widefaultzonestriking fault zonesoftheSlivnickiandZuba tectonic displacementtowards theSEalong importance are transcurrent faults,withdextral determine theindividualstructures, ofprime major role oftheseriesreverse faults,which major feature oftheunitisfaulting.Besides catchment basinissituatedwithinthisunit.The deposits, andthere from NNW-SSE toNW-SE. Thepositionofthe The regional structures haveastrikeranging relationships. relationships priortothehydrogeological it wasnecessarytodeterminethestructural the formationofsubsurfacechannelnetwork, uniform environment haveamajorimpacton and structural frameworkinalithologically hinterland toOmblaoccurs.Sincethetectonic through whichthesupplyofwaterfrom the of thedirections ofthegroundwater One ofthemajorproblems wasthedetermination as afullbarrier. impermeable clastic occurrence ofdolomiticlayersandacomplex fi Brgat (Prelogovi distinguish thestructural unitHutovo-Slano- and themonoclinebedinclinationtowards NE, the crest ofthenappe,concordant succession onto theEpiadriaticum(Herak,1991).Behind the regional structural unitoftheDinaricum structure isdominatedbythethrust contactof near-surface structural relationships. The the surface,indicatereverse faulting-thrusting ssure-dissolution porosity withasporadic ć etal.,1994;Fig.6.3).TheOmbla fl ysch rocks whichfunction fl ections ofthefaultson 3-06-2004, 10:03:53 fl ow č ki ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

Figure 6.3 - Regional structural sketch. 1. the most important faults of the regional structural fabric: fault of the front of the overthrust of the Dinaricum (1), Slivnica fault (2), Zubak fault (3); 2. others more important faults; 3. faults with marked displacement; 4. zone Hum-Ombla; 5. Dinaricum (I), Adriaticum (II), Epiadriaticum (III); 6. structural unit 1. the The most important faults of the regional structural fabric: fault of the front of the overthrust of the Dinaricum (1), Slivnica fault (2), Zubak fault (3); 2. other more important faults; 3. faults with marked displacement; 4. zone Hum-Ombla; 5. Dinaricum (I), Adriaticum (II), Epiadriaticum (III); 6. structural unit Hutovo-Slano-Brgat; 7. extension zone.

fault zone Hum-Ombla consists of several inclination thus forming an extensional duplex parallel faults, and their branches with a general structure (Davis, 1984). strike direction 50°-230° and a steep to opposite The hydrogeological, geophysical and (antitectic) fault plane dip angles from 70° - 85°. hydrological indicators show that most of the It cuts through the reverse faults, and reaches groundwater from the hinterland is drained into Volume n° 5 - from P37 to P54 n° 5 - from Volume the crest of the Dinaricum knappe. This type of the Hum-Ombla fault zone. This zone is the main tectonic kinematics, together with the favourable drainage area of the studied hydrogeological orientation in regard to the regional stress system, through which concentrated water fl ow (12°-192° direction) and the prevailing sinistral under pressure occurs towards the Ombla spring tectonic dislocation, permitted the continuous area (Buljan, 1999). The hydrological analysis of extension of the Hum-Ombla fault zone, the the H-Q diagram, show that the underground contraction and subsidence of individual retention area of the Ombla hinterland can also segments along the series of faults with antitectic be divided into two parts, in accordance with the

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Volume n° 5 - from P37 to P54 P53 - P53 Figure 6.4-Discovered levelsofkarstcavitiesintheOmblaspringhinterland. Leaders: M.Jura main conduitlevelsinthecrest oftheDinaricum is thedirect hinterlandofthespring.Thefour cave (80mlong,40wideand8high),which 1985). Behindthespringthere isalarge spring were performedtothedepthof-35m(Krašovac, up the springarea hassiphonmorphology. Itisan area. Thedominantchannelinthehinterlandof karst waterchanneldirections towards thespring hinterland, itwasnecessarytodeterminethe During thestudyofterraininspring the discharge zonewaslowered tosealevel. nappe crest zone,andtheerosion of uplifting ofthecarbonaterocks intheDinaricum and the crest ofthenappethatconsistscarbonate intersection oftheHum-Omblafaultzone,and within anextensionalduplexstructure atthe structurally predisposed. Thespringarea occurs The positionoftheOmblaspringarea is 1998). (during highwatersupto50cm/s;Paviša, shows pressurised turbulent the discharge zones,restricted groundwater existence ofkarstchannelsbetweenthisarea and area (theHum-Omblafaultzone).Duetothe from Zaplanikisanarrow, deeplykarsti underground reservoir. Thearea downstream the Omblahinterland,thisarea shouldforman fl of waterare accumulatedthrough laminated an underground area, inwhichlarge quantities The area upstream from Zaplanikconsistsof fl ow. After theconstruction oftheretention in ow regime (Milanovi fl fl ow spring. Speleologicalinvestigations ysch rocks. Duetopermanentneotectonic č i ć , LadislavPalinkaš ć , 1977,Jovi fl ow characteristics ć fl , 1997). ysch rocks, fl fi ow ed dam willbepositionedwithin of over1000m.Thelateralfoundationsthe deposits andthetopofdam,alength contact betweenthecarbonaterocks with the maximumheightof410mabovelowest mass toaheightof130mabovesealevel,i.e. planned some200mwithinthecarbonaterock connected withkarsti fault systems, will containconduits,channelsconnectedwith cause thegroundwater leveltorise.Thereservoir be attained.Theconstruction ofthedamwill importance, sinceretention ofthereservoir could rises abovetheplanneddamheight,isofkey occuring impermeable carbonate complex.Theexistenceofthelaterally porosity andthepermeabilityofcatchment facilitated bytheannualyieldofOmbla,and and reservoir intheOmblahinterlandwas The ideaforthedesignofanunderground dam channels. considerable aircurrent through thediscovered far havenotproven thiscompletely, butthere isa the springzone.Spelaeologicalinvestigationsso all theconduitsare connectedinthevicinityof up to-150mbelowsealevel.Itispresumed that below thedischarge zone,andreach depthsof the activewatertransportconduitsare located (Fig. 6.5).Intheimmediatevicinityofspring, the eastandtowestofspringzone. All which are locatedupto300mabovesealevel channels; Fig.6.4)occurinthePlo nappe (Viline pe fi ssures andotherphenomena ć ine-caves andactivewater fi cation. Thedampro fl ysch complex,which fl ysch deposits, ysch č ice faultzone 3-06-2004, 10:03:57 fl fi ysch le is ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

a

Figure 6.5 a,b - The comparision of the b Pločice fault zone position and four levels of subsurface cavities.

when the the vital power plant facilities are also planned below the surface, in order to preserve the natural landscape as much as possible. The design of the Ombla hydroelectric power plant (Sever, 1998; Fig. 6.6), is based on the principle of a groundwater pressure rise due to the construction of an artifi cial backwater in the underground. The backwater will be constructed with the aid of a grout curtain, performed minimum fl ow falls below 4 m3/s, the water from three grout-injection galleries, at elevations level is expected to drop to 70 m above sea level 5, 65, and 134 m above sea level. Furthermore, (Jović, 1997). spatial concrete plugs are to be constructed The uniqueness of the design of this power plant in all active and fossil channels. In the upper is that the infl uent channel connects the waters course, the groundwater level will rise above its from the power plant with the main infl uent

natural elevation. This retention concept is based P37 to P54 n° 5 - from Volume channel of Ombla in the lake Veliko jezero, 300 on the fact that according to the permeability m upstream from the profi le of the grout curtain measurements of the rock masses, and the fl ow (Fig. 6.6). The evacuation of high waters will be measurements, the rocks along the profi le of the performed through the basic outlet, with two curtain are of low permeability and that more than cone plugs each of which can give passage to 90% of the water fl ows through the main infl uent the maximum centennial fl ow, and the waters channel to the discharge zone. The water level from the turbines will be discharged into the in the reservoir through most of the year will be spring cave. All other facilities have some special at 130 m above sea level. During the dry season, characteristics, but in general they have the basic

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura rocks havebeendetermined:Senonianrocks, side isbuiltofcarbonaterocks. Thefollowing Dubrova The locationofthebridgeoverRijeka the midspan(Fig6.7). bottom ofthesupportingstructure is50.30mat 12.60 mwhiletheheightfrom thesealevelto 518.23 m,andtotalwidthbetweenthecornicesis of thebridge,completewithabutments,is high pylonasthemainsupport.Thetotallength designed asasuspensionbridge,with141.50m two with and synchronic generatorsof30MVA, and The bridgeovertheRijekaDubrova Vladimir JurakandSlobodanŠestanovi The bridgeovertheRijekaDubrova Stop 6.2: Francis turbines,witha with accompanyingobjects.Two ofthemhave Ombla willconsistoffourproduction units facilities. TheOmblahydroelectric powerplant properties ofclassicalsubsurfacehydro-energetic consisting ofstrati water turbidityduringhighwaters. aid ofpumps,andwillreduce theproblems with of Dubrovnik anditssurroundings withoutthe allow amore economicandbetterwatersupply besides theproduction ofelectricpower, will The construction oftheunderground reservoir, expected. the production of223GWhelectricpoweris 8 MVA. Duringanaveragehydrological year, č ka andtheaccessroad onitswest fl ow ofQi=6m č i ć , LadislavPalinkaš fi ed limestonesandmassive 3 /s, andgeneratorsof fl ow ofQi=24m č ka ć č ka is 3 /s,

of poorquality. the rock mass classi are therefore 20 to40,and have GSIfrom 4,50 mthick), places upto surface, in fault zoneandthesurface(weathered purposes, thefollowingcanbeconcluded: classi If GSIisappliedfortheengineering-geological Adriatic micro-plate underthe Adriatic. consequence ofstress duringthesubductionof by anoverturnedfold,canbeinterpreted asthe and tectonicnarrowing ofthearea, represented According torecent structural (morphostructural) unitofthe Adriatic. The investigatedarea belongstoaregional alveolinic, andnummuliticlimestones(Fig.6.8). Eocene rocks (Pc,E),containkozinias,miliolitic, and dolomitesinalternation.ThePalaeocene- limestones withRudists,andplaty limestones anddolomitesinalternation,massive represented by:massivedolomites, (Maastrichtian) hasbeendetermined,andis east sideofthebridg,eupperpartSenonian dolomites onthewestsideofbridge; 31.fossilcave. Figure 6.7-ThebridgeovertheRijekaDubrova fi fi e as ed cation oftherock massforfoundation Rijeka Dubrova road; 28.parkinglotandaccessplatform;29. left building; 25.accessroad totheHPP;26. pumping station;23.Springpond;24.control water supplyintaketunnelinfossilcave;22. in Large cave;20.watersupplytunnel;21. chamber; 19.watersupplyintakestructure chambers; 18.bottomoutletspillway bottom outletgatehousewithdissipation transformers; 16.bottomoutlettunnel;17. cave; 14.accesstunnel;15.switchyardand tunnels; 13.powerhouse spillwayinSpring gate house;11. powerhouse;12.tailrace 8. verticalshaft;9.penstock;10.penstock tunnel; 7.intakestructure accesstunnel; structure (forHPP)inLarge cave;6.headrace 2; 4.grout curtainandgalleryno.3;5.intake gallery no.1;3.grout curtainandgalleryno. 1. underground reservoir; 2.grout curtainand power plantfacilities: Figure 6.6-ReviewsketchoftheOmbla fl ank accessroad; 27.right č a 0 ditchgwy ka; 30.Adriatichighway; fi ndings, interlayerfaults fl ank access 3-06-2004, 10:04:03 č ka. ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

Figure 6.8 - Schematic Engineering-geological Map (geology from: Jurak et al. 1989). Legend: 1. Kozinias, miliolidic, alveolinic, and nummulitic limestones; 2. Platy limestones and dolomites in alternation; 3. Massive limestones with Rudists; 4. Massive limestones and dolomites in alternation; 5. Massive dolomites; 6. Stratifi ed limestones and massive dolomites; 7. Geological boundary – transgressive; 8. Dip of bed (1 normal, 2 overturned); 9. Fault; 10. Reverse fault; 11. Overturned anticline; 12. Part of brachysyncline; 14. Geological Strength Index 20-40 (poor: fault zones); 15. Geological Strength Index 60-80 (good).

References cited Agassiz, L. (1840). Evidence of a Glacial Epoch. In “A Source Book in Geology 1400- 1900.” (Mather K.F. and Mason S.L., Eds.), pp. 329-335, Harvard Platy limestones and dolomites in alternation, University Press. have GSI between 40 and 60, and are classifi ed Allen J.R.L. (1984). Sedimentary structures, as rock mass of fair quality. Limestones with their characteristics and physical basis. (II ed.). Rudists, layered limestones and massive Developments in sedimentology 30, XXVI+663, dolomites, and Palaeocene-Eocene limestones Elsevier Sci. Publ. Co. Inc. (Pc,E), have GSI between 60 and 80 (good Ashley, G.M. (1990). Classifi cation of large-scale quality). subaqueous bedforms: a new look at an old The area of Dubrovnik is located in a zone for problem. Jour. Sed. Petrol. 60/1, 160-172. which, with 63 % probability, the maximum Bachofen-Echt, A. (1925a). Iguanodon Faehrten earthquake intensity of 9 grades of the MCS scale auf Brioni. Palaeontologische Zeitschrift 7, 172-173. is expected in a recurrent period of 500 years. For Bauer, B., (1934/35). Über die Landformen des seismic calculation of the bridge structure, the Nordlichen Velebit. Sonderabdruck Jahrsberichte Volume n° 5 - from P37 to P54 n° 5 - from Volume maximum average, acceleration of 0,35 g for der Bundes-Realgymnasiums Knittelfeld, the east bank and 0,38g for the west bank are Knittelfeld. adopted. Belij, S. (1985). Glacijalni i periglacijalni According to the study conducted by the reljef južnog Velebita. Posebno izdanje Srpskog Hydrometeorological Institute, the expected geografskog društva 61, 5-68, Beograd. maximum velocities of bura (north-eastern Benić J. (1983). Vapnenački nanoplankton i wind), north-western wind and sirocco are 50 njegova primjena u biostratigrafi ji krednih i m/s, 38 m/s and 33 m/s, respectively. paleogenskih naslaga Hrvatske (Calcerous

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura Proteus Gogala, M.(1975).SlediizdavninenajuguIstre. Glasnik hrvatskognaravoslovnogdruštva Gavazzi, A., (1903b).Trag oledbe naVelebitu? 174-175. kršu. Gavazzi, A. (1903a).Tragovi oledbeunašem Gauthier-Villars, Paris,307. Atlas Tethys –Palaeoenvironmental maps. Dercourt, J.,Ricou,L.andVrielynck, B.E.(1993). Ungarische Akademie Degen, A. (1936).FloraVelebitica. and Regions.JohnWiley andSons,New York. Davis, H.G.(1984):Structural GeologyofRocks Istria, Croatia). tracksites intheMainBrioni/BrijunIsland(SW and Late Albian (earlyCretaceous) dinosaur Tarlao A. andTentor, M.(2002).LateBarremian Dalla Vecchia F.M., Vlahovi Italiana interpretation. Mljet lakes–potentialfor(paleo)environmental Vani Ć 141, 189-218. Péninsule balkanique. Cviji Norway. Collinson J.D.(1970).BedformsoftheTana River, Disertacija, RGNfakultet,1-176,Zagreb. on theNorthernVelebit). oledbe naSjevernomVelebitu (Glaciationtraces medusae. special reference totheirresident populationsof island seawaterlakes(South Adriatic sea)with S. (2000).EcologicalcharacteristicsoftheMljet izvorišnog podru u razradizahvataizaštitepodzemnihvoda Buljan, R.(1999).Zna 27-39. Bognar, A., Faivre, S.,Paveli Geology catastrophic sea-levelriseandice-shetcollapse. during thelastdeglaciation:evidencefor Blanchon, P. andShaw, J.(1995).Reefdrowning Cari Benovi Zagreb. p 159,Unpubl.doctoralThesis.Universityof Cretaceous andPaleogenesedimentsofCroatia). nanoplankton anditsusageinbiostratigraphyof osovi ć č ć , M.,Jasprica,N.,andBobanovi ek, V. (2002).Benthicforaminifersofthe , J.(1917).L’Epoque glaciaire dansle Glasnik hrvatskognaravoslovnogdruštva ć ć 37,229-232. 57,533-541 23,4-8. , A., Lu , A., , V., Jura Geogra Scientia marina č Natura Nascosta i fi č Memorie dellasocietageologica ć ska ann.52A i , LadislavPalinkaš č ć č i , D.,Onofri,V., Peharda, M., ć ja OmblakrajDubrovnika. 1,7-202. M.,Bajraktarevi č Annales Géographique enje strukturnog modela 64,supl.1,197-204. Geografski glasnik ć I.,PosoccoL., , 31-56. ć , J.(1991).Tragovi 25,1-36. Verleuterung ć 14,459. , Z.,and ć - Č 26/ oli 53, 14, ć , Guši croatica soline channel(Mljetlakes, Adriatic sea). Onofri, V. (2001).Holocenesedimentationinthe Cenomanian–Lower Turonian sea-levelrise Govor naravoslovnog društva 13/4-6,193-196,Zagreb. iz hrvatskogkrasa.Glasnik Gorjanovi Mamuži Ljubljana 1966,I,203-210. vanjskih Dinarida. Malez, M.,(1968).Orazvojukvartaranapodru three millionyears. Links betweenclimate Lambeck, K.,Esat,T. M., Potter, E.K.(2002). Ljubljana. Rijeke Dubrova Krašovac, M.(1985).Speleoronila 39–58. island ofCres (AdriaticSea,Croatia). along shallowintraplatformbasinmargin –the Cenoma Oštri Korbar, T., Fu Acta geologica und Lika,Kroatien. Mittleres undOberes Perm). Foraminiferen ausKarbonundPermimVelebit Like. Srednji igornjiperm(DieFusuliniden permske fuzulinidneforaminifere Velebita i Kochansky-Devidé, V. (1965).Karbonskei coastal lagoons. and hydrodinamic characteristicsofshallow Kjerfve, B.andMagill,K.E.(1989).Geographic Engineering, Split. i projektom de ponašanja podzemneakumulacijeuprirodnim Herak, M.(1991):Dinaridiimobilisti of theDinarides. Herak, M.(1986). A newconceptofgeotectonics carbonate platform. and itsconsequencesonthe Adriatic–Dinaric genezu istrukturu. Jovi Petrol. Geol.Bull carbonate platformof Yugoslavia. level riseandanoxiceventsintheMesozoic Jenkyns H.C.(1991).ImpactofCretaceous sea društva hrvatskog krasa. Hranilovi ć ć , V. (1997).HEOmbla,numeri ć , I.andJelaska,V. (1993).Upper , N.,Mati č 13/1-3,93-133. in, D.P., Jura 10/4, 247-258. ć ≠ P. (1962).Novijageološkaistraživanja nian carbonatefaciesandRudists ć ć , H.,(1901).Geomorfološkiproblemi iz , D.,(1902):Geomorfološkiproblemi 5,101-137. č ek, L.,Husinec, A., Vlahovi . 75,1007-1017. č Mar. Geol č fi Acta Geologica ke -Omble.Geološkizavod, Glasnik hrvatskognaravoslovnog nrnm veia Aquarius uvjetima. niranim ec, D.andJelaska,V. (2001). Nature I kolokvijogeologijiDinarida Acta geologica č Geol. Rundsch i ć , M.,Horvatin and sealevelforthepast . 88,187-199. 419,199-206. 16/1,1–42. 21/2,35-117. č . 82,676–686. ko istraživanje č Am. Assoc. č ki osvrtna č i ki model ć Facies , N.and 3-06-2004, 10:04:08 Natura ć 45, , I., č ju , ADRIATIC-DINARIDIC MESOZOIC CARBONATE PLATFORM, ENVIRONMENTS AND FACIES FROM PERMIAN TO RECENT TIME P53

otoka Raba (Some recent investigation of the Rab exported. J. Sediment. Petrol. 63, 589-595. island). Geol. vjesnik 15/1 (1961), 121-141. Muldini-Mamužić S. (1962). Mikrofaunističko Mamužić P. and Milan A. (1973). Osnovna geol. istraživanje eocenskog fl iša otoka Raba (Micro- karta SFRJ 1:100000 (Basic geologic map of faunistic investigation of Eocene fl ysch of Rab Yugoslavia, 1:100000), Tumač za list Rab L33- island). Geol. vjesnik 15/1 (1961), 143-159. 144, 5-39, Inst. geol. Istraž. Zagreb, Savezni geol. Nikler, L., (1973). Nov prilog poznavanju oledbe zavod, Beograd. Velebita. Geološki vjesnik 25, 109-112. Mamužić P., Milan A., Korolija B., Borović I. and Pamić, J., Gušić, I. and Jelaska, V. (1998). Majcen Ž. (1969). Osnovna geol. karta SFRJ 1: Geodynamic evolution of the Central Dinarides. 100000 (Basic geologic map of Yugoslavia, 1: Tectonophysics 297, 251–268. 100000), List Rab L 33-114, Inst. geol. Istraž. Paviša, T. (1998) Podzemna akumulacija u krškom Zagreb, Savezni geol. zavod, Beograd. terenu. Hrvatske vode 66, 14-25. Marinčić S. (1981). Eocenski fl iš Jadranskog pojasa Phleger, F.B. (1969). Some general features (Eocene fl ysch of the Adriatic belt) Geol. vjesnik 34, of coastal lagoons. In “Lagunas costeras” 27-38. (Ayala-Castaneras A. Ed.), pp. 5-26. Univ. Nac. Marjanac, Lj. and Marjanac, T., (1999). Polyphase Autonomus de México, México. kame terraces on the Island of Pag (Eastern Poljak, J., (1947). O zaleđenju Velebita. Geološki Adriatic, Croatia). Field Symposium on Pleistocene vjesnik 1, 125-148. Stratigraphy and Glacial Chronology, Southern Prelogović, E., Buljan, R. and Fritz, F. (1994). Estonia 1999, Abstract volume, 34-35. HE Ombla, strukturna istraživanja. Pismohrana Marjanac, T. and Marjanac, Lj., (1991). Pleistocene Instituta za geol. Istraž., br. 111/94, Zagreb. glacial and periglacial deposits on middle Ramovš, A. and Kochansky-Devidé, V. (1981). Adriatic coast. Abstracts IAS 12th Regional Meeting Permian-Triassic Boundary in Brušane Village Bergen, 32. (Velebit Mt., Croatia). Geologija 24/2, 327-330. Marjanac T. and Marjanac Lj. (1991). Shallow- Ramovš, A., Hinterlechner-Ravnik, A., Kalenić, marine clastic Paleogene on the Island of M., Karamata, S., Kochansky-Devidé, V., Krstić, Rab (Northern Adriatic). Abstracts Dolomieu B., Kulenović, E., Mirković, M. Petkovsky, P., Conference on Carbonate Platforms and Sremac, J. and Temkova, V. (1989). Stratigraphic Dolomitization, Ortisei, 159-160. Correlation Forms of the Yugoslav Paleozoic. Marjanac, T., Marjanac, Lj., Oreški E., Rend. Soc. Geol. It. 12, 359-383. (1990). Glacijalni i periglacijalni sedimenti u Roep Th.B. (1991). Neap-spring cycles in Novigradskom moru. Geološki vjesnik 43, 35-42. a subrecent tidal channel fi ll (3665 BP) at Marjanac, T. and Sremac, J. (2000). Middle Schoorldam, NW Netherlands. Sed. Geology 71, Permian calcispongal cement reef on the Velebit 213-230, Amsterdam. Mt. In “PANCARDI 2000, Dubrovnik, Croatia, Salopek, M. (1942). O gornjem paleozoiku 1-3.10.2000. Fieldtrip Guidebook” (Pamić, J. and Velebita u okolici Brušana i Baških Oštarija (Über Tomljenović, B. eds.), pp. 135-138. Vijesti Hrv. oberes Paläozoik von Velebit im Brušane und geol.društva 37/2, Zagreb. Baške Oštarije Gebiet). Rad Hrv. akad. znan. umjet. Marković, B. (1971). Osnovna geološka karta 274, 218-272. i tumač, K 34-49, List Dubrovnik, 1:100000. Schubert, R.J., (1909). Geologija Dalmacije. Matica Zavod za geol. i geofi z. istraž., Sav. geol. zavod, Dalmatinska 3-183. Beograd. Seibold, E. (1958). Jahreslagen in sedimenten der Mezga, A. and Bajraktarević, Z. (1999). mittleren Adria. Geologische rundschau 47, 100-117. Volume n° 5 - from P37 to P54 n° 5 - from Volume Cenomanian dinosaur tracks on the islet of Sever, Z. (1998). HE Ombla, idejni projekt. Fenoliga in southern Istria, Croatia. Cretaceous Hrvatska elektroprivreda. Elektroprojekt, A. Research 20, 735-746. Humbolta 4, Zagreb. Milanović, P. (1977) Hidrogeologija karsne izdani Shinn, E.A., Steinen, R.P., Lidz. B.H., and Swart, Ombla. Geološki glasnik 22, Sarajevo. R.K. (1989). Whitings, a sedimentologic dilemma. Milliman, J.D., Freile, D., Steinen, R.P., and J. Sedimentary petrology 59, 147-161. Wilbert, R.J. (1993). Great Bahama bank aragonitic Sremac, J. (1991). Zona Neoschwagerina craticulifera muds: mostly inorganically precipitated, mostly u Srednjem Velebitu (Zone Neoschwagerina

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Volume n° 5 - from P37 to P54 P53 - P53 Leaders: M.Jura and Vani carbonate production. synsedimentary tectonicsandextensiveorganic in southernIstria(Croatia): in from theLate Albian toMiddle Cenomanian Robson, J.(1998).Carbonatefaciesevolution Tišljar, J.,Vlahovi – Relationswith Adjacent Regions,Zagreb. Symposium onthe Adriatic CarbonatePlatform Excursion Guide-Book,TheSecondInternational Eocene) (Vlahovi the Adriatic CarbonatePlatform”(Permianto aspects oftheshallowwatersedimentationon A –Velebit Mt.,Permian–Jurassic. Veseli, V. andStankovi (Vlahovi Carbonate Platform(PermiantoEocene)” Shallow Water Sedimentationonthe Adriatic Tišljar, J.,Vlahovi Zagreb, Zagreb. Adriatic CarbonatePlatform. Gudebook, SecondInternat.Symposiumonthe Grenz-Horizonte. Stache, G.(1889).DieLiburnischeStufeundderen Yugoslavia). craticulifera Mt.: Permian-Jurassic. bioturbated limestones-Excursion A -Velebit Liassic shallow-marine,tempestiteand marine limestonesandcontinentalsediments, carbonates, MiddletoUpperTriassic shallow- calcispongite patch-reef, Permianperitidal south (1967). Theproduction oflimemudbyalgaein Stockman, K.W., Ginsburg, R.N.,andShinn,E.A. V andStankovi Tišljar, J.,Vlahovi island ofMljet). western IstrianTitonian andBarremian ofthe of blackpebblesinperitidallimestonesthe titona zapadneIstre ibarema otokaMljeta(Origin (“black-pebbles”) uperiplimnimvapnencima Tišljar, J.(1986).Postanakcrnihvaluticaioblutaka 42/1, 133-141. of cyanobacterialpicoplankton. biogenic originduetothephotosyntheticactivity T.J., andDesMarais,D.J.(1977).Whitingevents: Thompson, J.B.,Schultze-Lam,S.,Beveridge, č Č ek, V., Jura fl orida. osovi ć , IandVeli in theMiddleVelebit Mt.(Croatia, ć Geologija , V(2000).Benthicforaminiferal J. Sediment.Petrol. č ć i Geol. vjesnik ć , D.(1991).TheMiddlePermian ć , LadislavPalinkaš ć Abh. Geol.Reichsanst ć , I.andVeli , I.,Sremac, J.,Veli č , I.,Veli ć i ć ć , I.,Sremac, J.,Veli , I.Eds.),pp.3-52,Excursion 34,7-55. , M.,Barjaktarevi Facies In ć “Some Aspects ofthe , D.(1991).Excursion ć 39,75-94. 38,137–152. , I.,Mati

Institute ofGeology ć , I.Eds.)pp.1–49. 37,633-648. Limnol. Oceanogr č fl ć . 13,170. une of uence ec, D.and , I.,Veseli, In “Some ć , Z.,2, ć , I., . naslagama jugozapadneIstre. (Biostratigraphic Veli Brijuniusporedba sodgovaraju i sedimentološkezna 37, Zagreb. Direkcija zarazvijiinženjering, Avenija Vukovar hidrološka obrada.Hrvatskaelektroprivreda - Žugaj. R.andBonacci,O.(1994).HEOmbla, Veli Estiva, Trieste, Soc.Geol.It. Longo Salvador, G.Eds.)pp.452–455.Riunione comunicazioni oraliediposter”(Carulli, G.B.and than 200milionsofyears. 8.000 mthick,builtthrough theperiodofmore Carbonate Platformorcarbonatepieupto Croatia). Eocene oftheOuterDinarides(IslandRab, sandstones depositedbytidalcurrents inthe Zupani Acta Adriatica du MaloetVeliko jezero, surl’illedeMljet, Visser M.J.(1980).Neap-springcyclesre Veli Croatia). example from theMljetlakes(Adriaticsea, assamblages inarestricted environment -an Vuleti preliminary note. Holocene subtidallarge-scale bedformdeposits:a review ofthegeologyIstria). (Vlahovi Geological Congress, ExcursionGuide-Book” (1995a). Op the PannonianBasin”(Vlahovi to theQuaternaryinKarstDinaridesand Depositional Environments from thePalaeozoic and RegionalComparison. Flysch BasinDuringtheEocene:MainEvents Jurassic totheSantonianandFormationof the Adriatic CarbonatePlatformfrom theMiddle Bergant, S.(2003).EvolutionoftheIstrianPart Veli 17–19, 2003,Zagreb. Meeting ofSedimentology, Opatija–September Eds.) pp.3–17.FieldTrip Guidebook.22ndIAS Veli 40, 149-168. Cretaceous depositsinSWIstria). and sedimentologiccharacteristicsoftheLower ć ć ć ć , I.andTišljar, J.(1987).Biostratigrafske , I.(2000).TheKarstDinarides:the Adriatic , I.,Tišljar, J.,Mati , I.Tišljar, J.,Vlahovi ć , A. (1953).Structure geologiquedufond č J.andBabi ć Geol. vjesnik44 Geologia Croatica , I.andVeli ć i prikazgeološkegra 6/1,1-64. Geology 8 ć ć , I.Eds.)pp.5-30. Lj.(1991).Cross-bedded č , 235-245. ajke donjekrede otoka č , 53/2,269-279. ec, D.andVlahovi , 543-546. ć , I.,Mati In In “Riassuntidelle ć , I.andTišljar, J. “Evolutionof In Geološki Vjesnik “1stCroatian đ č e Istre (A ec, Dand fl ected in 3-06-2004, 10:04:11 ć ć , I. im

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