B12_ copertina_R_OK C August 20-28,2004 Florence -Italy

Field Trip Guide Book - B12 Pre-Congress Associate Leader:R.Dimitrescu Leader: M.Sandulescu CARPATHIANS OF THEROMANIAN GEOLOGICAL STRUCTURE 32 Volume n°1-fromPR01toB15 GEOLOGICAL CONGRESS nd INTERNATIONAL B12 28-05-2004, 19:17:12 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

B12_ copertina_R_OK D 24-05-2004, 15:38:15 Volume n° 1 - from PR01 to B15

32nd INTERNATIONAL GEOLOGICAL CONGRESS

GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS

AUTHORS: M. Sandulescu (University of Bucharest - Rumania), R. Dimitrescu (Romanian Academy, Bucharest - Rumania)

Florence - Italy August 20-28, 2004

Pre-Congress B12

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Leader: M. Sandulescu Associate Leader: R. Dimitrescu

Introduction Geology of the South Carpathians in the Danube The fieldtrip “Geological Structure of the Romanian Gorges (Romanian Bank) by Pop et al., 1997. Carpathians” strives to cross the major tectonic units of this segment of the Tethyan Chains, with the General Geological Setting purpose of presenting a general approach to the tec- General Structure and Evolution of the Romanian tonic and paleogeographic (paleotectonic) problems. Carpathians Knowledge of Carpathian geology allows us to under- (according to Săndulescu, 1980, 1984, 1994) stand the prolongation of the Alps toward the Balkans The Carpathians are a segment of the Tethyan and the Dinarides. In order to accomplish the above- Chains; toward west they join the Alps and toward mentioned tasks during the fieldtrip, a part of the south and south-east the Balkans and the Rhodope. significant geological cross sections in the East and The Carpathian Foreland includes several platforms South Carpathians as well as in the Apuseni Mts will (Scythian, Moesian) or cratons (East European) as be visited. Thus we will examine the tectonic units is- well as the Cimmerian North Dobrogea Orogen sued from the Tethyan Ocean - squeezed in the Main (Figure1). The Carpathian Folded Area is the result Tethyan Suture Zone or obducted on the continental of several tectogenetic events of different ages: Cre- margins – and their deformed continental margins. taceous (generating the Inner Zones named Dacides) In the areas crossed by the fieldtrip geological maps and Miocene (the Outer Zones named Moldavides). and older fieldtrip guidebooks are available. It should Upper Cretaceous and/or Paleogene post-tectogenetic be remembered that in respect to the geological maps covers develop above the Inner Zones. The Pannonian or other guides, in the guidebook proposed here more and the Transylvanian, Neogene molassic depressions or less important differences are possible, determined overlie important parts of the Inner Zones and a part by the progress of our knowledge and/or a better un- of their post-tectogenetic covers. A Neosarmatian-Eo- derstanding of the geological processes. pleistocene molassic asymmetric foredeep develops Geological Map of Romania, scale 1: 200,000, sheets: in front of the Orogen, partly (inner limb) superposed Rădăuti, Topliţa, Piatra Neamţ, Odorhei, Brașov, on its external zones (Figure 1). The Folded Area can Turda, Brad, Deva, Tg. Jiu, Baia de Aramă, Reșiţa. be divided into several major tectonic ensembles: Geological Map of Romania, scale 1: 50,000, sheets: Vatra Dornei, Pojorâta, Câmpulung Moldovenesc, The Main Tethyan Suture Zone (MTS) which Dămuc, Voșlăbeni, Miercurea Ciuc, Brașov, Zărnești, groups together tectonic units constituted by Middle Codlea, Zlatna, Câmpeni, Avram Iancu, Biharia, Brad, Triassic-Middle Jurassic ophiolitic complexes over- Deva, Lupeni, Schela, Tismana, Obârșia Cloșani, lapped by sedimentary formations whose age (Middle Orșova, Reșiţa, Bocșa. and Upper Triassic, Jurassic or Upper Jurassic-Lower The Structure of the East Carpathians (Moldavia- Cretaceous) is different from the age of the ophiolites Maramureș Area) by M. Săndulescu et al., 1981, they cover. The MTS which runs along the Vardar Guide to Excursion B1. Zone (between the European and the Apulian conti- Structural Relations between Flysch and Molasse nental margins) splits – from Beograd toward north (The East Carpathians Model) by M.Săndulescu et or north-west - into two branches: the South Pan- al., 1981, Guide to Excursion A5. nonian (separating the Apulian microplate from the The Structure of the Apuseni Mountains by M.Bleahu Fore-Apulian one) and the Transylvanidian-Pienidian et al., 1981, Guide to Excursion B3. (situated between the European and the Fore-Apulian Metamorphosed Paleozoic in the South Carpathians margins) (Figure2).

and Its Relations with the Pre-Paleozoic Basement by PR01 to B15 n° 1 - from Volume H.Kräutner et al., 1981, Guide to Excursion A1. The Fore-Apulian Microcontinent (FAM) is situ- The Structure of the South Carpathians (Mehedinţi- ated on the opposite side with respect to the European Banat Area) by S.Năstăseanu et al., 1981, Guide to margin, considering the MTS a major geotectonic axis Excursion B2. of symmetry of the Tethyan Chains. The FAM groups Excursion to South Carpathians, Apuseni Mountains together the Austroalpine, the Central West Carpathi- and Transylvanian Basin. Description of stops by ans and the North Apusenide units (Figure 1), as well Berza et al., 1994 ALCAPA II. as the units covered by the Pannonian Depression

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Figure 1 - Tectonic Sketch of Romania (acc. to (Figure 1). The cover type of nappes are well devel- Săndulescu, 1994). Carpathian Foreland: 1- East oped in the Flysch Zone of the East Carpathians and European Craton, 2 - Scythian (Sy) and Moesian (Mo) in the Subcarpathians. In the South Carpathians only platforms, 3 - North Dobrogea Orogene. Carpathians: 4 - the Severin Nappe (situated tectonically between the Inner Dacides (Northern Apusenides), 5 - Transylvanides, Getic Nappe and the Danubian) is of this type. 6 - Pienides (5 + 6 - Main Tethyan Suture), 7 - Median Dacides (Crist. - Mesoz. Zone, Getic and Supragetic), 8 - Outer Dacides (Ceahlau- Severin), 9 - Marginal Dacides Geotectonic History. (Danubian), 10 - Moldavides, 11 - Post - tectogenetic End-Proterozoic (Panafrican) cratonisation is rec- covers, 12 - Neogene Molasse depressions and Foredeep, ognized in the whole Carpathian Foreland and in 13 - Up. Cret.- Paleoc. magmatic arcs, 14 - Neogene the Carpathian Orogen as relics. This huge cratonic magmatic arcs, 15 - thrust - sheets, 16 - faults. area, preserved actually in the East European Craton, (Figure 2). was split south and west of the former within the The European Continental Margin (ECM) groups Paleozoic mobile areas. The folded basement of the together the main part of the East Carpathians (the Pi- Scythian Platform proceeds from one of these, while enides belong to the MTS) and the South Carpathians. the Paleozoic metamorphic series of the Carpathians There are two basic types of units: basement shearing comes from another branch. Within these branches, nappes and cover nappes. The first type is built up of remnants of Paleozoic oceanic crust-bearing domains

Figure 2 - The major Tethyan sutures and continental crystalline formations (metamorphics and sometimes areas in the Carpathian realm (post- tectonic covers is not acid and/or intermediate granitoids) and their normal shown) (acc. to Săndulescu, 1987). 1 a - Inner Dacides, PR01 to B15 n° 1 - from Volume sedimentary envelope (sedimented on the continental 1/2 - Bükk Unit and correlative units, 2 - Major Tethyan margin). This type of unit, which developed in the Suture (Vardar, South Pannonian, Transylvanides, FAM too, constitute the Central East Carpathians Pienides etc), 3 - Măgura Group (belonging to the (the Crystalline-Mesozoic Zone excepting the Tran- suture, 4 - Median Dacides (Central East - Carpathians, sylvanian nappes which are obducted from the MTS Getic & Supragetic nappes), 5 - Outer Dacides (Ceahl u - Severin), 6 - Marginal Dacides (Danubian), - Figure 1,2), its correspondent in the South Carpathi- ă 7 - Moldavides. Bc - Bucharest, Be - Beograd, Bd - ans (Getic-Supragetic ensemble) and the Danubian Budapest, K - Krakow, W - Wien.

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu which occursinsomeunitsofthe Transylvanides subduction), expressed in thecalc-alkalinevolcanism crust subductionbelow oceaniccrust(Marianne type Tithonian/earliest Neocomian.Itconsistsofoceanic the Carpathian Tethys was recorded inthelatest The earliestmeaningfulcrustalshorteningin Kimmeridgian age. youngest ophiolitesproceedingfromitbeingofpre- the Tethyan Oceanreachesitsmaximumsize,the Aulacogene. At theMiddle/LateJurassicboundary deformation oftheNorthDobrogea-SouthCrimea of theMoesianBlock,determinecompressive tioned rift,accompaniedbythenorth-easternmotion opening ofthe Tethys andthedistensionofmen- Margin (theBlack Flysch-Ceahl the MiddleJurassicwithinEuropeanContinental ing processesoccurduringthelateEarlyJurassicand and spreadingduringthislastperiod(Figure3).Rift- Jurassic, thePienidiansegment ofthe Tethys opening continue duringtheLate Triassic, EarlyandMiddle pean ContinentalMargin. The spreadingprocesses the Fore-Apulian MicrocontinentfromtheEuro- obducted fromthe Transylvanidian suture)separating ance withtheageofoldestophioliteswhichwere spreading startsintheMiddle Triassic (inaccord- Tornquist-Teisseyre Lineament. Tethyan oceanic to theright-lateralstrike-slip movements alongthe represents apossiblepull-apartstructureconnected the openingofoceanic Tethys, thesecondone South Crimea Aulacogene. The first oneprecedes the future Tethyan OceanandintheNorthDobrogea- The earliestriftings–Early Triassic –occuralong Carpathians andpartsofitsForeland. occurs aftertheEarlyCarboniferous,including seem tobeacceptable. A secondlarge cratonisation Tatrides, WA- WesternAlps. - Silicicum,SvSeverin, SP-SerboPelagonian, Ta - - SouthCarpathians,SgeGeticandSupragetic,Si Pn -Pontides, Rh-Rhodopes,SCSouthCrimea,SCA ND -NorthDobrogea,PPieninyKlippen,PdPindus, Djirula, EA-Eastern Alps, MM-Moesia,M CWC -Central West Carpathians,D-Danubian,Dj - Choc,ChCeahl - Apuseni Mts.,B-Bükk,BA -Balkanides,BiBihor, Cc Upper Austroalpine,Lower AM - Austroalpine,- Aas Aai crust, 7-ThinnedcrustofMoldavides. AA - Austroalpine, Aulacogene, 5-Continentalcrust,6deformed oceanic Dacides), 4-NorthDobrogeaSouthCrimeaCimmerian crust (Pindus),3-Thinnedandoceanic(a)(Outer - Tethyan oceaniccrust,2-Thinnedand/or their Foreland duringtheMesozoicandPaleogene. 1 Figure 3-Palinspastic sketches oftheCarpathiansand ă u, COC-CentralEastCarpathians, ă u-Severin Rift). The ă 24-05-2004, 15:42:47 gura, GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

(South Apuseni). A largely developed tectogenetic changed lithofacies with respect to the Moldavides, event is the Meso-Cretaceous one. It involved the fill the Getic Depression. This represents a (proto-) European Continental Margin generating the base- foredeep of the South Carpathians (where Tertiary ment shearing nappes of the Central East Carpathians shortenings are not recognized). (Median Dacides) and a part of the oceanic Tethys expressed in obductions above the former (Tran- Geological Structure of the East Carpathians sylvanidian Nappes). Meso-Cretaceous shortenings The Romanian East Carpathians are the natural south- are also known in the Getic-Supragetic Domain, as ward prolongation of the Ukrainian East Carpathians. well as in the Ceahlău-Severin Rift. The Intra-Turo- Conventionally the boundary between the East and nian (Pre-Gosau) tectogenetic compressional events North Carpathians is situated along the Dniester, San affected the Fore-Apulian Microcontinent (Inner and Uj valleys, but from the geological point of view Dacides), although mesocretaceous deformations are there are only minor changes (if they exist). Roughly also recorded. The End-Cretaceous tectogeneses de- the boundary between the East and South Carpathians termined the final closing of the oceanic Tethys in the shows the same features, but the correlation is more Transylvanidian sector and partially in the Pienidian difficult because of the development of post-tectoge- one (Figure3). The European Continental Margin was netic covers and a complex system of Quaternary affected by the End-Cretaceous deformations, too. At Depressions. that time the South Carpathians recess-type bending The major geological ensembles of the East Carpathi- was accomplished by the westward motion of the ans are (innward-outward) (Figure 1) (Săndulescu, southern panel of the Moesian Platform, facilitated 1984, 1994): 1) The Pienides, situated north of the by the right-lateral slip of the Intra-Moesian Fault Transylvanian Depression and the North Transyl- (Figs.1, 3). The motion of the Moesian Platform was vanian Fault; 2) The Crystalline-Mesozoic Zone accompanied by the underthrusting of the Danubian (Median Dacides and Transylvanian nappes) and its (Marginal Dacides) below the Getic and Severin nap- post-tectogenetic cover (above which the Pienides pes determining the consumption of the crust of the are overthrust); 3) The Flysch Zone, showing an in- Severin sector of the rift, process which generated the ternal and an external zone; 4) The Subcarpathians. Banatitic (calc-alkaline) Arc intruded in the overrid- The innermost units of the Flysch Zone are grouped ing units, the Getic-Supragetic nappes respectively. A in the External Dacides, while the Moldavides group similar calc-alkaline (“Banatitic”) arc develops within together the other units of the Flysch Zone and the the margin of the Fore-Apulian Microcontinent, gen- Subcarpathians. Inward with respect to the Crystal- erated by subduction of the oceanic Tethyan crust line-Mesozoic Zone and crossing the Pienides, a below the continental crust of the yet deformed Inner Neogene Volcanic Chain develops. Dacides (Figure 6 ). The Pienides consist of cover nappes overthrusted Starting with the Early Paleogene, the mobile areas, above the Upper Cretaceous-Paleogene-Lowermost receiving important turbiditic (flysch) sedimenta- Miocene post-tectogenetic cover of the Crystalline- tion, remain the Pienidian (Pieniny + Măgura) and Mesozoic Zone, during the Burdigalian. the Moldavidian domains (Figure 3) as well as some The Crystalline-Mesozoic Zone is built up of base- post-tectogenetic basins (e.g. Maramureș-Bârgău). ment shearing nappes, each of them showing large The Pieniny-Magura Domain, with a partly con- developed metamorphic formations covered by a sumed oceanic crust, ends southward on the North Mesozoic or Permo-Mesozoic sedimentary envelope. Transylvanian Fault, which separated it from the The nappes, of Meso-Cretaceous age, cover each yet “sutured” Transylvanidian sector of the oceanic other. They are (up/down) the Bucovinian Nappe, the Tethys. The Moldavidian sedimentary Cretaceous Subbucovinian Nappe and the Infrabucovinian nap- and Paleogene-Lower Miocene basins develop above pes. The metamorphics consist of several superposed a thinned crust, which will be consumed during the series (partly tectonically as a result of Paleozoic tec- PR01 to B15 n° 1 - from Volume Miocene together with the crust of the Ceahlău sector tonic events) (Tab.1) (Kräutner, 1983, 1985; Balinto- of the Ceahlău-Severin Rift, during the Miocene gen- ni, 1985, 1997). The most important part of them are erating the East Carpathian Neogene Volcanic Arc. mesometamorphic and Precambrian. The youngest The south-west end of the Moldavidian troughs is one (Tulgheș Series) is of Lower Paleozoic age and, connected to the Intra-Moesian Fault (Figure1). West perhaps, epimetamorphic. During the Middle Triassic of it the Paleogene formations, which generally show a first paleogeographical differentiation took place: on

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu (excepting thePer ophiolitic complexes fromthebasal partofthenappes ferent lithostratigraphicsuccessionsandagesofthe main nappes(Per the Meso-Cretaceoustectogeneses. There arethree Tethyan SutureZone(Figs.1,2)obductedduring The Transylvaniannappes tectonically superposedonthe Wildflysch. ceeding fromthe Transylvanian nappeswhichare contains thesedimentaryklippen(“olistoliths”)pro- succession isthe Aptian-Albian Wildflysch which developed inthetopofBucovinian sedimentary sedimentation tookplace. A meaningfulformation ian domainandtheInfrabucovinian one,pelagiclimy Subbucovinian domain,whileonthecentralBucovin- arenites beingsuppliedbysomeelevated partsofthe the Bucovinian domainaflyschtroughdevelops, its differentiation isrecorded:alongtheexternal partof thonian-Neocomian timeasecondpaleogeographical Middle Jurassicisgenerallydetritic.Duringthe Ti- water environment (hard-groundtypeorparalic), the gap). The discordant Lower Jurassicisofshallow- Upper Triassic formationsareabsent(stratigraphic bituminous, dolomitesandlimestonesdevelop. The while ontheInfrabucovinian domainbasinal,weakly ter (mainlydolomites)carbonaticrocksaredeposited, the Bucovinian-Subbucovinian domainshallow-wa- Formations oftheCentre.EastCarpathians Table 1-CorrelationSketch oftheMetamorphic ward above theunderthrustForeland (Figure4,5). from theirprimarybasementandoverthrusted east- up essentiallyofsedimentaryformationsdetached The FlyschZone basic unitsmaybealsorecorded. Ocean). Transitional successionsbetweenthesethree ing zonewhichprecedestheopeningof Tethyan groupstogethercover nappesbuilt ș ș ani, OltandH ani oneproceedingfromtherift- proceedfromtheMain ă ghima ș ) withdif-

Axios -Vardar Zone. Around Belgrade,abranchof which intheBalkanPeninsulaisalsoknown asthe to theprolongationofMajor Tethian SutureZone The Southern Apusenides correspondongenerallines Apuseni Mountains Geological Structure oftheSouth Wallachian “Phase”. ing theLower Pleistocenetectonicevent known asthe Foredeep isfolded. The deformationstookplacedur- In theCarpathianBending Area theinnerlimbof the external deformedpartofthechain(Figure1,4). situated discordantlyabove theForeland elementsand The Foredeep the Foreland). carpathian Nappe,thelastimportantunderthrustingof Folds Nappe)Intra-Sarmatian(overthrust oftheSub- thrusting ofthe Tarc Macla and Audia nappes),Intra-Badenian(over- Burdigalian (overthrusting oftheConvolute Flysch, slight foldingoftheConvolute FlyschNappe),Intra- End-Cretaceous (overthrusting oftheCeahlau Nappe; and BaraoltnappesfoldingoftheCeahl Meso-Cretaceous (overthrusting ofthe Black Flysch of theFlyschZoneandSubcarpathiansare: events whichgeneratedtheactualstructuralfeatures Upper Eoceneonesareassociated. The tectogenetic of someanticlines-Oligoceneandexceptionally mostly ofMioceneformationstowhich–inthecore overthrust unitoftheEastCarpathians. Itconsists Subcarpathian Nappe(Figs.1,4,5)istheoutermost (Lower andMiddle)sedimentaryformations. The Folds) compriseCretaceous,Paleogene andMiocene (Convolute Flysch,Macla, Audia, Tarc tectogenetic cover. The otherunits(theMoldavides) formations, thePaleogene onesbuilding uptheirpost- etc.) (Figure1)containonly Tithonian-Cretaceous The innermostnappes(BlackFlysch,Ceahl isanasymmetricmolassicdepression

ă u NappeandoftheMarginal ă u, Marginal ă u,Baraolt ă 24-05-2004, 15:42:55 u one), GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

Figure 4 - General cross - section through the Romanian Carpathians (acc. to Săndulescu, 1984). Inner Dacides (1+ 2) : 1 - Codru - Arieșeni nappe system, 2 - Bihor Unit; Main Tethyan Suture: 3 - Transylvanides: Median Dacides (4 - 6) : 4 - Bucovinian Nappe, 5 - Subbucovinian Nappe, 6 - Infrabucovinian nappes; 7- Remnants of the primary basements of the Flysch Zone in the Benioff paleoplane; Outer Dacides (8 + 9) : 8 - Black Flysch Nappe, 9 - Ceahlău Nappe; Moldavides (10 - 15) : 10 - Convolute Flysch, 11 - Macla Nappe, 12 - Audia Nappe, 13 - Tarcău Nappe, 14 - Marginal Folds Nappe, 15 - Subcarpathians Nappe; Foredeep : 16- Focșani Depression; Underthrusted elements (17 + 18) : 17 - Crystalline basement, 18- Sedimentary formations (Pz - Paleozoic, Mz - Mesozoic, Pg - Paleogene).

the latter curving to the NE joins under the mainly Tertiary and Quaternary cover (Vojvodina-Banat) the complicated Southern Apuseni orogenic system em- placed mainly on oceanic crust; another branch, also concealed by younger formations, runs WNW along the Sava river (South Pannonian Suture - Săndulescu, 1980, 1984). North and South of the Southern Apuse- nides suture zone, units with continental basement represent its margins, called respectively Internal, Median Dacides.

The different units of the Southern Apusenides, mainly obduction nappes, consist of sedimentary Up- per Jurassic and Cretaceous formations, at the base of which magmatic complexes of ophiolitic or island arc character were conserved. The age of the ophiolites is Middle Jurassic, whereas the calc-alkaline island- arc series belongs to the Upper Jurassic (Berriasian, at most). From north to south, the tectonic units which will be crossed during the excursion are: Bucium Unit, Feneș Nappe, Techerău Nappe, Căbești Nappe and Bejan Nappe. We shall describe them according to Bordea, 1992 and Bleahu et al., 1981. The Bucium Unit overlies a crystalline basement characteristic of the Northern Apuseni (Internal Dacides). The sedimentary sequence starts with the Ciuruleasa Formation consisting of black argillaceous shales with sandstone lenses in which an Early Cre-

taceous flora was found. A sandy calcareous-shaly PR01 to B15 n° 1 - from Volume flysch-like formation called the Valea Povernei For- mation follows, of Upper Hauterivian-Lower Aptian age, established according to paleophytological data (Antonescu, 1973). The most characteristic term of this formation is a quartzitic sandstone with calcare- ous matrix and calcitic veinlets, interbedded with dark argillaceous shales. Graded bedding and parallel or

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu Formation ( Mountains. ItstartswithaUpperSantonianGosau as thecrystallineschistsofNorthern Apuseni sively thepreviously describedformationsaswell The SenonianoftheBuciumUnitoverlies transgres- (Cenomanian). es intotheortho-quartziticNegrileasa Conglomerates At itsupperpart,thePârâul Izvorului Formation pass- another structuralunit(theCurechiuNappe). data werefoundinthesameformationoccurring The constrainingmacro-andmicropaleontological rock typesbeingmicaceoussandstonesandmarls. graded beddingandconvolute structure,themain lui Formation. Itconsistsofagrey flyschwithevident The Upper Albian isrepresentedbythePârâul Izvoru- also occurs. basic tuffs orjaspers,aparatypicflyschoidfacies calcirudites, calcarenites,polymicticconglomerates, the SoharuFormation. Besidesthechaoticblocksof mafic rocksrepresentsalateralfacies variation of olistoliths ofUpperJurassicmassive limestonesand A grey Lower Albian Wildflysch Formation with limit theageasUpper Aptian-Lower Albian. Micropaleontological evidence aswell rocks andlimestones. calcirudites andconglomerateswithpebblesofmafic stones andweaklycalcareoussandstones,darkclays, flysch with Wildflysch episodes.Itconsistsofsilt- which couldbecharacterizedasagrey argillaceous The sequencecontinueswiththeSoharuFormation, Orbitolinids - MiddleMiocene. 2 -Eocene,o1Oligocene,mLower Miocene,m2 Cretaceous, k2-UpperPg1Paleocene, Pg - Mesozoic,NNeogene,ThTithonian, k1-Lower Cr -crystallineformations, Pz-3UpperPaleozoic, Mz - MarginalFolds Nappe,SC-Subcarpathians Macla Nappe, A - Audia Nappe,TC-Tarc - Ceahl - Infrabucovinian Nappe,FN-Black Flysch Nappe,CH Bucovinian Nappe,SB-Subbucovinian Nappe,IB onstrated by observed. The Aptian ageofthisformationwas dem- mafic rocksandofNeojurassic limestonescanbe conformably. Inthegradedcalcareniteselementsof with intercalationsofgreenish-grey shalesfollows of calcareoussandstones,calcarenitesandcalcirudites Next, ashaly-calcareousflyschformationconsisting cross laminationcansometimesbeobserved. St Carpathians (incentralMoldavia)(acc.toS Figure 5-SyntheticcrosssectionthroughtheEast ă nic ă ă and Visarion inS u Nappe,FC-Convolute Flysch Nappe,M- andapalynologicalassociation. rudist Brachiopods -bearing limestones)followed by ă ndulescu ,1994).B- ( Belbeckella ă u Nappe,MA ă

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GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

Figure 6 - Structural cross - section through the Apuseni Mts. and the South Carpathians (acc. to Săndulescu, Stănică and Visarion in Săndulescu ,1994). 1 - Bihor Unit (BH) (a - sedimentary formations), 2 - Codru - Arieșeni nappes system (CA), 3 - Biharia nappes system (B) (a - Gosau Formation), 4 - Transylvanides (M) (Southern Apusenides) (Main Tethyan Suture), 5 - Getic (G) and Supragetic (SG) nappes (a - sedimentary formations), 6 - Severin Nappe (SV), 7 - Danubian (DA), 8 - Senonian - Paleocene calc - alkaline magmatites (Banatites), 9 - Moho Discontinuity.

of quartz sandstones and grey clays which towards the top grades into slumped clays with interbedded tuffs and spilitic lavas as well as with either massive bio- constructed or thin bedded micritic limestones. In the massive limestones, Pachyodonts were found provid- ing proofs of their Barremian-Lower Aptian age. The Feneș Formation grades up into the turbiditic Valea Dosului Formation, consisting of calcareous polymictic conglomerates, alternating with sand- stones, green clays and mafic pyroclastites. In inter- calated calcarenites Orbitolinids were found, indicat- ing an Aptian age. The Meteș Formation, overlying unconformably the two above-mentioned sequences, has a typical Wild- flysch character. It includes two members: a lower one characterized by an olistostrome-like marly-silty facies with some interbedded turbiditic and coarse layered sandstones; an upper member which consists of breccias with silty-marly green, grey or reddish matrix and exolistoliths of ophiolitic rocks, Upper Jurassic massive limestones or granodiorites. The Upper Aptian-Middle Albian age of the Meteș Formation was established according to macropal- eontological and palynological studies. Next follows the Valea lui Paul Formation, consist- ing of grey, loose sandstones which pass into sands. Micropaleontological and palynological studies have provided evidence of a Upper Albian-Cenomanian age. The Senonian of the Feneș Unit is represented by medium or fine-grained sandstones and polymictic conglomerates. A megabreccia Wildflysch Formation grey marls with Inoceramus balticus and a gritty- follows, interpreted by some authors as an independ- Volume n° 1 - from PR01 to B15 n° 1 - from Volume shaly micaceous flysch. ent unit (Valea Mică-Galda Nappe). The Feneș Nappe is overthrown northwards onto the The Techerău Nappe is developed in a widespread Bucium Unit and has an ophiolitic basement. It begins area in the western and the central part of the South with the Feneș Formation, the most significant within Apusenides. It is the unit which shows a major part the Southern Apusenides. It could be defined as a vol- of the Tethian oceanic crust. Its basement consists of cano-sedimentary calcareous olistostrome with flysch ophiolitic rocks as well as of an island arc calcalkaline sequences, and starts with a thick turbiditic sequence series, which interfingers with Callovian radiolarites. The sedimentary sequence starts with these jaspers

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu Frasin (Fr) Nappes;Gr, Gro Hospea Nappe;Bj,BejaniUnit;Bo,Boze Unit. Southern Apusenides: Ri,RimeteaNappe;Be,BedeleuNappe.NappesSystem:Fu,FundoaiaH, (S) andFerice (F)Nappes;U,Urm Valea Mic A, Moma(M)and Arie impossible toevaluate. Fault. Consequently, theiroverthrusting characteris displacement, paralleltotheSouth Transylvanian ing vertical dislocations probablywithahorizontal The following two unitsareborderedby EWtrend- are alsopresent. stones andmarlysequences,ascribedtothe Albian, ment inseveral places.Inplaces,interbeddedsand- limestones andmafic rocksdirectlyoverlie thebase- taining olistolithsofUpperJurassicandUrgonian Wildflysch sequencesconsistingofdarkclayscon- well astheeruptive rocksdirectly. Orbitolinids Nappe; HP, Highi remian -Aptian(?)marlyorsandylimestoneswith sive limestonesofKimmeridgian-Tithonian age.Bar- followed byOxfordianmicriticlimestonesandmas- Northern Apusenides: BihariaNappesSystem–BA, Baiade Arie magmatites; +++UpperCretaceouscalc-alkalineSn,post-tectogeneticcover oftheNorth Apusenides. Figure 7-Structuralsketch-map ofthe Apuseni Mountains.....Neogenemolassecover; vvvvNeogenecalc-alkaline ă -Galda Nappe;T, Techer overlie theUpperJurassiclimestones as ș (H)andPoiana (P)Nappes;CodruNappesSystem:Co,Cole ș eni (A)Nappes; Vt, Vetre Nappe;DBa,Dieva(D)andB ș i Nappe;Bu,BuciumUnit.MedianDacides:DM,SuprageticNappes ă ă t Nappe;Fi G,Fini u Nappe;C,Curechiu Nappe;FB,Fene ș Nappe; V Ar, Vulcan (V)and Ardeu (Ar)Nappes;Cb,C ș (Fi) andGârda(G)Nappes; Vl, V

(uppermost Albian) duetothe calcareous sandstones,ascribedtothe Vraconian quartzose conglomerateswhichlaterallypassinto is overlain bytheFornpdia Formation, consistingof comparison withthe Valea Povernei Formation. It like sequences.ItisascribedtotheBarremian,by an olistostromewithquartzsandstone-shalyflysch- The BejanUnit also dueto marls, areconsideredtobelongtheCenomanian, calclithitic sequencewhichfollows, aswell reddish The C black argillaceous clayswithintercalationsofbasaltic Upper Jurassic-Neocomianlimestonesembeddedin a Wildflysch with exolistoliths ofbasalts, Triassic and South Apusenides. The BejanFormation consists of ș Nappe;ML,Muncel-Lup ă be ș Ammonite ti Unit ș -Bl ă isthesouthernmostoneof ă trânescu (Ba)Nappes;SF, begins withtheCpbe ș jani Nappe;CrFr, Cri ti Nappe; Va, Va faunas. ă lani Nappe;UB,Bihor ș a Nappe;B,Biharia Ammonites ș ă c be ă u Nappe;M ș ti Nappe; VG, ș ș ti Formation, (Cr)and found. The Ș asa 24-05-2004, 15:43:13 GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

flows and pyroclastics. Its age was ascribed to the series represents a magmatic island-arc setting devel- Barremian. oped over the previously formed oceanic lithosphere. The Deva Formation which follows after an evident Relations with sedimentary formations constrain the unconformity is represented by poorly sorted, loose, age of the calc-alkaline series to the Upper Jurassic. thick bedded sandstones interbedded with silty marls. No genetic relationship with the underlying ophiolitic According to palynological data, its age may be as- rocks exists. A younger alkaline series consists of lim- signed to the Turonian and Senonian. burgites, trachyandesites (oligophyres) and trachytes The Bozeș Nappe represents the uppermost unit in (orthophyres) intercalated in the Lower Cretaceous the south-eastern part of the Southern Apuseni. The Feneș beds. Bozeș Formation represents its main lithostratigraph- Microtectonics and metamorphism ic term. It is a typical flysch formation in which the of the Feneș beds. following rock types can be recognized: sandstones, Two folding phases developed during the time-span silty marls and microconglomerates. Graded bedding, from Early Aptian to Late Maastrichtian. The D1 sole markings and bioglyphs are frequent. Towards phase produced west-northwest-verging isoclinal the top, the flysch sequence is replaced by a molassic to very tight folds, associated to a slaty cleavage. one, with conglomerate levels. The top itself consists Illite and chlorite were formed, metamorphic condi- of continental deposits. The age of the formation is tions being close to the diagenetic zone/anchizone ascribed to the Senonian, reaching the Maastrichtian, boundary. The subsequent D2 phase produced north- established on the basis of faunal remains and micro- northwest- verging, parallel folds. The burial of the faunal studies. formation took place at a depth of 8-10 km (Ellero Mesozoic eruptive rocks. et al., 2002). At the beginning of the eighties, Savu (1981) for Main tectonic features The geotectonic evolution of the first time stated the clear distinction between the the Southern Apusenides was typically polyphasic. ophiolitic complex of the South Apusenides, consist- The Mesocretaceous tectogenesis involved two ing of a tholeiitic series, and an island arc volcanism moments:1) the first one, in the uppermost Aptian, forming a calc-alkaline series, emplaced in the same marked some unconformities in the Bucium, Feneș Carpathian unit. and Căbești Units; 2) the second, an intra-Late Albian The most recent data concerning both magmatic com- one, was much more important and caused thrusting plexes are due to Saccani et al. (2001), Bortolotti et al. between some units. The Wildflysch character of some (2002) and Nicolae, Saccani (2003). We shall describe Albian formations pleads also for important compres- them according to the latter. sive movements; 3) The pre-Gosau tectogenesis does The ophiolitic sequence is characterized by: 1) an in- not display evident structures. It is the Laramian tec- trusive section represented mainly by small gabbroic togenesis that accomplished the structural framework bodies as well as scarce ultramafic cumulates; 2) a of the Southern Apusenides. The overall transport basaltic sheeted dike complex; 3) a volcanic sequence direction of the nappes is a north- western one. including basalts and rare pillow breccias; 4) very rare Concerning the Neogene tectonics, it is noteworthy Callovian radiolarian chert. that characteristic NW-SE structures can be consid- Basaltic rocks display MORB patterns and a high-Ti ered also as tectono-magmatic alignments. magmatic affinity; all the geochemical features sug- gest that the ophiolites were generated in a mid-ocean Geological Structure of the North ridge setting and that they can be correlated with the Apuseni Mountains ophiolites of the Vardar-Axios zone. K-Ar ages of The Northern Apusenides (Internal Dacides) group microgabbros, dolerites and basalts from the Mureș together units issued from the deformation of a conti- Valley (Techerău Nappe) fall between 138.9 ± 6.0 nental crust. These units consist of metamorphic and and 167.8 ± 5.0 M. a. (Middle to Upper Jurassic) granitic basements of Precambrian or Paleozoic age PR01 to B15 n° 1 - from Volume (Nicolae et al., 1992). and of sedimentary Upper Paleozoic and Mesozoic The overlying calc-alkaline rocks are represented formations. by massive lava flows including basalts, andesites, Bihor Unit. It has to be underlined from the begin- dacites and rhyolites, as well as by some granitoid ning that, although this fact is not compulsory, every complexes intruded into the ophiolitic sequences; Alpine tectonic unit having a crystalline “sole” is they show locally high-K calc-alkaline affinity. This characterised by specific features of this metamorphic

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu Jurassic, whichisofwildflyschtype. Nappe, withlithofacial variations atthe level ofthe The nian-Neocomian. -development ofaflysch-typesequenceinthe Titho- Jurassic; -marine, marly-calcareousfacies oftheLower latest Triassic; Carpathian Keuper andKössen facies intheLateand -complete development ofthe Triassic sequence,with imbritic volcanism; -large development ofthePermian,withfelsicign- features, thefollowing aretobementioned: Dallmeyer etal.(1994). As specific lithostratigraphic sions beingpre-Hercynian (400m.a.)accordingto Granitoids andMigmatites,theoldestbasicintru- a metamorphicbasementconsistingoftheCodru The first majorunit,the spond totheSouthHungarianBekes Realm. thrust fromtheSEontoBihorUnit;they corre- Codru NappesSystem. A numberofnappesareover- northwards ontothe Tethysian Suture. Slovakian Carpathians,andisprobablyoverthrust southern Hungaryandtothe Tatride unitsinthe The BihorUnitcorrespondstothe Villàny Unitin continues inthe Turonian. Aptian, passingintoamarlysedimentationwhich -calcareous neriticlithofacies oftheBarremianand marked bybauxites; -lag ofsedimentationatthebaseCretaceous, meridgian andthe Tithonic; -development ofacarbonaticplatformintheKim- base oftheUpperJurassic; -marine sequenceoftheMiddleJurassicand -Gresten paralicfacies oftheLower Jurassic; -absence ofthemajorpartUpper Triassic; Upper Werfenian tothebaseofCarnian; -development ofacarbonaticplatformseriesfromthe lined: specific lithostratigraphic featuresmustbeunder- pre-Senonian Cretaceousformations. The following (besides very scarcePermian) Triassic, Jurassicand The sedimentarysequenceoftheBihorUnitincludes, are Paleozoic. The agesofthemetamorphismandintrusion both intrudedbytheMunteleMaregraniticmassif. Series (chlorite-sericite-albiteschists,metarhyolites), amphibolites, leptynites)andtheretrogressive Arada of themedium-gradeSomesSeries(micaschists, For thelowermost BihorUnit,thisbasementconsists basement. Urm ă t Nappe is developed similarlytotheFini Fini ș -Gârda Nappe, has ș

Baia de Arie The - alagatthelevel oftheJurassic. the UpperNorian); - development ofReiflingandDachsteinfacies (until rocks intercalatedbetweentwo rhyoliticsequences; - acomplex magmatisminthePermian,withmafic The St to NW-SEtrendinglineaments(Brad-S 2001). They cropoutalongthreemain WNW -ESE ing; many plotat theedgeofadakitefield (Ro from basalt-andesitestodacites,andesitesprevail- 7.4 M.a.,theircalc-alkalinecompositionvarying the Apuseni Mountainsrangeinagefrom14.8to Neogene magmatism. andesitic andrhyoliticminorintrusions. out onlyonrestrictedareasandisalsoassociatedto Southwards, agranodioritic-graniticbatholithcrops minor intrusions. lites, allcrossedbyquartz-dioriticandmonzogranitic overlain byandesites, dacitesandignimbriticrhyo- Vl Late Cretaceousmagmatismisthevolcano-plutonic Apuseni Mountains,anoutstandingexample of Banatitic LateCretaceous magmatism. is representedbybanatites. Formation. The post-tectonicsubductionmagmatism are post-erosionallyoverlain bytheSenonian Gosau the Slovak CentralCarpathiansortotheEastern Alps) ized bya Turonian principaltectogenesis(similarlyto Internal Dacides(Northern Apusenides), character- Post-tectogenetic cover. Upper CarboniferousP metarhyolites) overlain bythemetaconglomeratic Muncel Series:sericiteschists,myloniticgranites, bolites, chlorite-schistswithalbiteporphyroblasts; pre-Carboniferous age(BihariaSeries:orthoamphi- consists essentiallyofmetamorphicformations Biharia NappesSystem. assic sequencesinHallstattandDachsteinfacies. The highestnappesoftheCodruSystemdisplay Tri- with theRhaetian. Upper Triassic formations,incalcareousfacies, end including acidiceruptive products. The Middleand sic formationsofreddishcolourarewelldevelopped, veins). The UpperCarboniferousandPermianmolas- Arie of theformerconsistsLower Carboniferous units includingtheBihorUnit. The oldestformations ă ă nija-Zlatna, Ro deasa Massif;avolcano-sedimentary formationis ș Moma-Arie Dieva-B eni Series(greenschistsintrudedbydoleritic ș zone. ă trânescu Nappe ș eni Nappe ș ia Montan ă Neogenemagmaticrocksin iu The nappesbuilding upthe ș eni Series. This groupofnappes overlies alltheother ischaracterizedby: ă -Bucium), plusthe ă Inthe 24-05-2004, 15:43:20 c ă râmb, ș u, GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

Geological Structure of the South Carpathians Zircon U-Pb data on an intercalated augengneiss have As results from the general introduction, the South given an age of 777 ± M.a. for the emplacement of Carpathians, which extend from the Prahova Valley the protolith of the gneiss, while Nd model ages for in the east to the Timok Valley in the south, consist the amphibolites range from 717 M.a. to 817 M.a. of the following main Alpine structural elements: (Liégeois et al., 1996). Major and trace elements from Lower Danubian Units, Upper Danubian Units, Sev- the Drăgșan amphibolites consistently display an is- erin Nappe, Getic Units, Supragetic Units. Important land arc signature. K-Ar model ages of the Drăgșan pre-Alpine tectonic units (nappes) are involved and rocks or the associated granitoids range between 325 preserved in these Alpine nappes. The Danubian on and 97 M.a. (Grünenfelder et al., 1983), showing later the one hand, the Getic and Supragetic Units on the reworking. other hand, represent two sialic microplates, while the The Lainici-Păiuș Group is exposed in the same two Severin Nappe, lacking a metamorphic basement, is areas mentioned above (Retezat and Mehedinţi-Vâl- related to a basin with oceanic crust. With the excep- can-Parâng Mountains). The main features of this tion of the latter, all the main Alpine units consist of group are the sedimentary origin and the invasion a metamorphic basement including Precambrian and of granitoids as a number of large plutons, countless Paleozoic rocks and of a sedimentary cover beginning small bodies and various migmatites. with a Variscan molasse and including Mesozoic for- Two formations were recognized: a lower Carbon- mations up to the Senonian. ate- Graphitic Formation, consisting of crystalline South of the Danube, in Serbia and Bulgaria, the Dan- limestones and dolomites, sillimanite-andalusite- ubian Realm corresponds to the Stara Planina, Miroc´ cordierite-graphite mica gneisses, amphibolites and and West Porec´ Units (Krstic´, Karamata, 1992). calc-silicate gneisses, and an upper Quartzitic and Lower Danubian Units The Lower Danubian units Biotite Gneiss Formation. are represented by several pre-Alpine nappes with The two main types of plutons intruded into the a common Upper Paleozoic-Mesozoic post-nappe Lainici-Păiuș Group are the Șușiţa type and the cover; only in the south-eastern part of the area an Tismana type. The former is made up of medium-K important Alpine overthrust was recognized (Schela). calc-alkaline granodiorites and tonalites; the latter The main pre-Alpine nappe (Retezat-Parâng Unit), (Tismana and Novaci) belong to the shoshonitic consisting of a distinct sequence of polymetamor- series, displaying a complete range of compositions phic rocks (Drăgșan Group) intruded by granitoid from ultramafic to felsic rocks. Widespread mingling- bodies and covered by Lower Paleozoic low-grade mixing relationships give rise to a variety of facies. A formations, is overthrust onto metadetrital sequences liquid line of descent from the diorites to the granites of polymetamorphic rocks (Lainici-Păiuș Group), was reconstructed. The intermediate and felsic rocks associated granites and low-grade Lower Paleozoic are commonly porphyritic (Duchesne et al., 1998). formations (Vâlcan-Pilugu Unit). The ages of the various syn-to late-kinematic grani- Metamorphic basement. The Drăgșan G r o u p is toid intrusives in the Lainici-Păiuș basement are in exposed in the Retezat Mountains in the north and in the 588 - 567 M.a. range (U-Pb zircon ages). The the Mehedinţi-Vâlcan-Parâng Mountains in the south. regional LP- HT metamorphism is probably not much Its main part is represented by an Amphibolite Forma- older (Liégeois et al., 1996). tion, in which the dominant banded amphibolites are Lower and Middle Paleozoic very low-grade forma- interlayered with biotite augen-gneisses, leptynites, tions. Although the presence of the Cambrian in the mica gneisses and scarce serpentinites, crystalline Lainici-Păiuș Group was advocated, the evidence is limestones or kyanite-staurolite gneisses. Retrogres- not convincing. The oldest Paleozoic sequence, the sive events have caused alterations of amphibolites to Upper Ordovician age of which was proved by pale- greenschists over large areas. The volcano-sedimen- ontological evidence (Corals, Crinoids, Brachiopods Volume n° 1 - from PR01 to B15 n° 1 - from Volume tary origin of the amphibolites from mafic igneous as well as Acritarchs and Chitinozoans) is the Valea rocks and tuffs is evidenced by rock associations and Izvorului Formation (quartzites, metaconglomerates chemical data. and slates); notwithstanding its scarce development, The Drăgșan rocks are intruded by the Retezat, Parâng it serves to constrain the age of the high-to medium- and Culmea Cernei plutons, dominantly granodiorite grade metamorphic formations underlying it. bodies with biotite-hornblende diorites or biotite ± A younger sequence is the Valea de Brazi Formation muscovite granites occurring in restricted areas. (metaconglomerates, sandstones, slates) attributed to

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu (1983) comparethisgroupwiththeDr greenschists orsericiteschists.BerzaandSeghedi fected sostronglybyretrogressionthatthey looklike and micagneisses(±kyanite, staurolite)generallyaf- ing amphiboliticsequence,withassociatedleptynites basement ofseveral nappesandconsistsofaprevail- The ZeicaniGrouprepresentsthepolymetamorphic northern andwesternpartsoftheDanubian Window. The UpperDanubianNappesareexposed inthe Metamorphic basement. Upper DanubianNappes sandstones withprehniteandpumpellyite. pyrophyllite); theUpperCretaceousvolcaniclastic (metaconglomerates andphylliteswithchloritoid low metamorphism:theLiassicSchelaFormation of theLower DanubianMesozoicdisplayingvery A specialmentionhastobemadeofthenorthernpart ian. Upper Cretaceousturbidites,reachingintotheSenon- stones; MiddleCretaceousshales(Nadanova beds); Upper Jurassic-Lower Cretaceousmassive lime- Middle Jurassicsandstoneswithcarbonaticmatrix; Gresten facies deposits(conglomerates,sandstones); are thefollowing: Permianred-beds;Lower Jurassic overlying the Variscan andpre-Variscan basement Upper Paleozoic andMesozoic. the Devonian. the mafic-ultramafic Tisovi Ogradena, etc);specialmentionhastobemadeof toid plutons(MunteleMic,Sfârdinu, Cherbelezu, with restrictedextension) areintrudedbygrani- The two groupsofmetamorphicrocks(andothers Lainici-P It was comparedbyBerzaandSeghedi (1983)tothe plagiogneisses, amphibolites,ishighlymigmatised. ing ofaprevailing quartziticsequence,muscovite The metaterrigenousM the Lower Danubian. Râu Alb Formation (Ordovician-Silurian phyllites, mations arerepresentedbythefollowing: Nijudimu- Lower andMiddlePaleozoic (Grünenfelder etal.,1983). ing Variscan and Alpine reworking ofthebasement toids rangebetween447and96M.a.,demonstrat- Danubian metamorpfic rocksandassociatedgrani- The K-ArmodelagesofsamplesfromtheUpper massif ofSerbia. the southernpartofwhichconsistsDeliIovan dismembered aformerlymuchlarger ophioliticbody, horizontal displacementof40km(trendingNE)has dextral Cerna-PorecˇkaRekafault systemwitha ă iu ș GroupoftheLower Danubian. ă gura Marga Groupconsist- ţ a-Iu very low-grade for- ţ The formations i complex. The ă g ș an Groupof than 300kminlengthand80maximalwidthon main partoftheGeticNappe,extending over more The LotruGprepresentsthebasementof Getic NappeMetamorphic basement. pes (Grubic´etal.,1997). corresponds totheKosovica andSub-Kosovica Nap- a microfauna of deposits (Sinaiabeds:distallimestoneturbiditeswith beds), andUpperJurassic-Lower Cretaceousflysch marly pelagicdeposits-anchimetamorphic Azuga crystalline schists,limestones,inamatrixofsiliceous liths ofbasalts,gabbros,serpentinites,harzburgites, includes aUpperJurassictectonicmelange(olisto- formed intheJurassiconEuropeanmargin. It in ariftwithoceanicorthinnedcontinentalcrust, Carpathians consistsofobductedslicesgenerated Severin Nappe. The Severin NappeintheSouth grade, increasingeastwards. formations betweenhigh-gradediagenesisandlow- The intensityof Alpine metamorphismvaries inthese Upper Cretaceousflysch(Arjana). stones andshales(Arjana),orbylimestones(Svini and alkalinelava flows, pyroclastic deposits,lime- either byavolcano-sedimentary formationwithmafic morphic facies; Middle-UpperJurassic,represented noires”), sometimesdeveloped inSchelaanchimeta- ing conglomerates,sandstonesandslates(“terres and volcaniclastic rocks;Lower Jurassiccoal-bear- slates; Permianred-bedswithrhyolitic volcanic iferous coal-bearingconglomerates,sandstonesand The following aretobementioned:UpperCarbon- Svini iscan basementaredeveloped intwo mainzones: The formationsoverlying the Variscan andpre-Var- Upper Paleozoic andMesozoic proved by the Drencova Formation, theageofformerbeing Silurian andtheDevonian couldbeparallelizedwith strained by in aDevonian olistostrome;its Arenigian ageiscon- the oldestfossiliferousformationisfoundasblocks But southoftheDanube,inStaraPlaninaUnit, constrained bypalynologicalassociations. eridae, the latterwhichbearsmacrofaunal remains( sandstones, mafic volcanics). With theexception of Formation (Lower Carboniferouslimestones,slates, sandstones, slates,mafic tuffs andflows); Sevastru Rece-Drencova Formation (Devonian conglomerates, Formation (probablySilurianconglomerates);Râul conglomerates, sandstones,mafic tuffs); Brustur ţ a- Arjana and Cornereva-Mehadia. and a- Arjana etc),theagesofformerformationsare TabulateCorals Acritarchs Calpionellids . Inthesameunit,Upper . ). InSerbia,thisunit 24-05-2004, 15:43:24 Spirif- ţ a); GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

Romanian territory. It consists of a thick sequence e.g., is exposed at Criva (329 M.a. K / Ar) in the of polymetamorphic rocks, mainly in amphibolite southern Poiana Ruscă. Older intrusions are found as facies (sillimanite-kyanite-staurolite-garnet-bearing orthogneiss associated with the crystalline schists. micaschists and plagiogneisses, orthogneisses, lep- Upper Paleozoic and Mesozoic formations. tynites and amphibolites), as well as of dismembered The post-Variscan formations of the Getic Nappe, ophiolitic slabs of metaperidotites, metagabbros; a exposed mainly in the Reșiţa-Moldova Nouă zone, siliceous manganiferous formation with tephroite begin with Upper Carboniferous coal-bearing con- concentrations; only in the deepest horizons are glomerates and sandstones, followed by Permian calcareous or dolomitic rocks found e.g. Armeniș; black shales and red sandstones. tectonic inclusions of anisofacial rocks-eclogites and A new transgression begins with the Lower Jurassic granulites-are hosted in places). An elaborate subdivi- coal-bearing detrital sequence, continued with Mid- sion of this group is still in progress. dle Jurassic marls or sandstones, Upper Jurassic The bulk of K-Ar ages as well as the preliminary limestones, Lower Cretaceous marls and Urgonian 40Ar / 39Ar results “suggest that regionally penetrative limestones. The Upper Cretaceous is represented ei- high-temperature mineral assemblages and associated ther by red marls, by a volcano-sedimentary forma- ductile structural elements are likely related to Late tion (Rusca Montană basin), by sandstones and red Variscan tectonothermal activity” (Dallmeyer et al., clays with Dinosaurs (Haţeg), or as conglomerates, 1994). Isolated pre-Variscan mineral ages still sug- sandstones and marls (Vânturariţa, Olănești). gest a Precambrian age of the protoliths as well as of Reșiţa-Sasca-Gornjak Nappe. The following struc- a first metamorphism of the Lotru Group. The main tural unit is characterized by the presence of Triassic part of the Getic corresponds in Serbia to the Kucˇaj formations. In Serbia, its basement consists of an Nappe and in Bulgaria to the Srednogorie. anchimetamorphic Devonian-Lower Carbonifer- Lower and Middle Paleozoic (?) low-grade ous flysch, with Corals, Tentaculites, Orthoceratids formations. and Pelecypods, including olistoliths with Late The Miniș Formation is a monotonous metaterri- Silurian Orthoceratids and Crinoids (Dimitrijevic´, geneous sequence (mainly chlorite-biotite-quartzitic 1997). Upper Carboniferous conglomerates and Per- schists) with minor bodies of metarhyolites. mian black shales and red sandstones are overlain by The Buceava Group (Ordovician?) includes a discon- Lower-Middle Triassic conglomerates followed by tinuous slab of metabasaltic rocks with associated fossiliferous dolomites and limestones, the Jurassic black shales, siltites, carbonatic rocks, metapsephites being similar with the same formations of the Reșiţa- and metapsammites. Moldova Nouă zone. In Serbia, the Lotru Group corresponds to the Osanica Supragetic Nappes. The Supragetic Units can be di- “Series”; it is overlain by an anchimetamorphic Or- vided in Western and Eastern ones; the former appear dovician, beginning with Cˇaradoc, with Trilobites, in Banat while the latter are exposed in the Făgăraș Brachiopods and Acritarchs. The sequence continues Mountains, east of the Olt. with the Kucˇaj-Cernogorje Flysch (Devonian) bear- Western Supragetic Units Metam ing floral remains and Conodonts and with a Lower orphic basement. Carboniferous, both non-metamorphic (Pantic´, The Bocșiţ a - Drimoxa Formation consists mainly 1963). of garnet-bearing paragneisses with oligoclase por- The Sicheviţa granitoid massif (Brnjca in Serbia) is phyroblasts, and amphibolites overprinted by ret- the most important of the Getic Realm, its length in rogression. It corresponds probably to a part of the the north - south direction on both sides of the Dan- Locva “Series” exposed at the entrance of the Danube ube being about 100 km. It post-dates the Paleozoic into Romania. Its age could be Upper Precambrian to formations in the Banat region. Two magmatic suites Lower Paleozoic. can be distinguished, a plagioclasic and mafic one (in- The Caraș Group includes the Naidăș-Rafnic vol- PR01 to B15 n° 1 - from Volume cluding trondhjemites and tonalites) and a predomi- cano-sedimentary Formation at the base, the Dog- nantly potassic-felsitic one (including leucogranites, necea-Zlatiţa terrigenous Formation and the Tâlva monzogranites, granodiorites). Isotopic age determi- Mare quartzitic Formation, all exposed either in the nations gave results of 237 - 310 M.a. (K / Ar) and Bocșa Massif or in the Locva Massif (SW Banat). 328 - 350 M.a. (Rb / Sr and U/ Pb). The characteristic feature of the Caraș Group is the Another small granitoid intrusion in the Lotru Group, development of a bimodal magmatic association: rhy-

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu The to apolymetamorphichistory. M olites, gabbros,dolerites(Iancu,1982,1986;Iancu, The sented mainlybytwo groups:Cump e nt. E asternSupgicUs.Mmohb Lower Cretaceous. age ofwhichcouldbeascribedtotheUpperJurassic- tion isoverlain, westofRe Mesozoic formations. ries” ortotheBoc Vlasina SeriescouldbecomparedtotheLocva “Se- Iancu, M Their metamorphismislow-grade (Iancu,1982; bros anddiorites-granodiorites. rocks, scarceacidmetatuffs andsmallbodiesofgab- metatuffs withinterlayeredmetapeliticandcarbonatic Lower Carboniferous).Itincludesmainlymafic mentary Valea SatuluiFormation (UpperDevonian- is constrainedby morphic Lisinabeds,the Tremadocian ageofwhich silegrad, insouth-easternSerbia,bytheanchimeta- Series” (Dimitrijevic´, 1997).Itisoverlain atBo- main partofitsbasementconsiststhe“Vlasina to the Western SuprageticistheMorava Nappe. The In Serbia,thehigheststructuralunitcorresponding Amphibolite, theLere lar totheBoc Precambrian, accordingtopalynologicaldata),simi- sequence consistsofthe Voine (1984) andothersasbelongingtotheGeticNappe.Its The sive overprint developed over large areas. phibolites andgraphiteschists;anintensive retrogres- chists, crystallinelimestonesanddolomites,para-am- The nilor Micaschists(+kyanite, staurolite). ite), theCozia Augengneisses andtheM linear Gneiss(originatinginapolymetamorphicgran- Supragetic. However thetwo unitsareseparatedbya jevic´, 1997)aspartofthesame structuralunitasthe sidered bysomeauthors(S massif falls outsideourobservation area. Itiscon- Serbo-Macedonian Massif. Albe schists. The Bughea Amphibolite isintrudedbythe C bite-porphyroblast schistsandalbitegneissesthe Ordovician, accordingtopalynologicaldata)ofal- ă ă lu run EastoftheOlt,Suprageticbasementisrepre- F L eaotGrup ș ș Moniom Group C ump ti Granite(473-486M.a.,K/ Ar). u Formation (Devonian ?)consistingofgreen- ă ţ g iu, 1994). The metamorphicparagenesespoint ă ă ra run ă ș Group naGroup ţ iu, 1994). ș i ţ a-Drimoxa Formation, theBughea ș i Brachiopods. ţ consistsofasequencemicas- a-Drimoxa Formation. consistsofthevolcano- sedi- ș ti Formation (definitely Lower The Boc The isconsideredbyS iscomposedoftheCump ă ndulescu, 1984;Dimitri- The Serbo-Macedonian The ș i ţ a, bylimestones,the ș ș ti Formation (Upper i Consequently, the ţ a-Drimoxa Forma- ă na andF ă gura Câine- ă ndulescu ă g ă ra ă na ș . part oftheFlyschnappesiswellexpressed. Foreland willbe crossed. At P 30 kmfromSuceava, theSarmatianformationsof following mainroadno.17.Until P From Suceava thefieldtrip leaves toward thewest, will bevisited. tween 91and65M.a.(Berzaetal.,1998). is exposed. IsotopicK/ Ar agesarecomprisedbe- pragetic anandesiticvolcano-sedimentary formation Cretaceous basinoverlying boththeGetic andSu- and lamprophyres.OnlyintheRuscaMontan diorites, monzogranites,andesites,dacites,rhyolites as byhypabissalminorintrusionsofporphyryquartz- line plutons(granodiorites,granites,diorites)aswell along threelineaments;itisrepresentedbycalc-alka- magmatism was mainlyintrusive anddeveloped Romanian SouthCarpathians,theUpperCretaceous B anticLeCrousmgm. Eastern Suprageticiscontroversial. even Alpine subunits. The ageofoverthrust ofthe above iscomplicatedbypre-Variscan, Variscan and first phase.Each of themain Alpine unitsdescribed ern SuprageticontotheGeticprobablybelongto onto theLower Danubianaswellthatofthe West- darcea, 1940). The overthrust oftheUpperDanubian “piggy-back” was overthrust ontotheDanubian(Co- togenesis, theSeverin NappebearingtheGetic onto theSeverin Nappe.2)DuringtheLaramiantec- taceous tectogenesis,theGeticNappewas overthrust Carpathians was polyphasic:1)DuringtheMesocre- Apusenides, thegeotectonicevolution oftheSouth Main tectonicfeatures. Serbo-Macedonian massifstr.s. Buzia Danube, thewesternpartsof Vrsˇac (Serbia)and Kobila line,Kräutner, Krstic´, 2002). Northofthe major shearzone(Dusˇanovo, Rozaj-Bovan or Vrvi pes). The XV pes). The Central EastCarpathians(withtheirsuperposednap- examine theSubcarpathians,FlyschZoneand pathian structure. Along itthereisthepossibilityto cepting theMaramure Aims nesc - Vatra Dornei Suceava -GuraHumoruluiCâmpulungMoldove- Field itinerary : This is oneofthenorthernmostprofiles (ex- ș (Romania)crystalline“islands”belongtothe th centuryfrescoed Voronet monastery DAY 1 ș ) acrossthewholeEastCar- SimilarlytotheSouth ă ltinoasa, thefrontal ă ltinoasa, about 24-05-2004, 15:43:27 ă Inthe Upper GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

Stop 1.1: beds-type flysch”) of the Plopu Formation Păltinoasa Quarry. (Uppermost Lutetian-Priabonian). Red and purple On the left-hand bank of the Moldova, at Păltinoasa, clayey shales (an equivalent of the Strujinoasa For- a sequence crops out of the Lutetian - Bartonian for- mation) are inlayered in the lower third. The Eocene mations of the Păltinoasa “Rabotage” Slice. The most / Oligocene boundary is situated within a sandstone important part of this sequence is represented by the sequence (Săndulescu et al., 1987). The lower part Păltinoasa Sandy Limestone of Lutetian age (Ionesi, of it - the Lucăcești Sandstone - shows inlayerings 1971). It is equivalent to the Paszieczna and Doamna of “Globigerina marls” (white compact marls rich in limestones (see Tab.I). On the top of the quarry, above planktonic microfauna, nanoplankton and silicoflag- the Păltinoasa Sandy Limestone, lies the Strujinoasa ellates of Late Priabonian age), while the upper part Formation, a variegated shaly - clayey formation, in - the Fierăstrău Sandstone – has inlayerings of dark which red - purple clays are dominant. The Lutetian bituminous siltstones and/or clays (containing nano- / Bartonian stratigraphic boundary is situated within plankton and silicoflagellates of Earliest Rupelian). the Strujinoasa Formation. The sandstones are both orthoquartzitic (oligomictic), Upstream, in the town of Gura Humorului, the front the Lucăcești one also containing grains of glauco- of the Tarcău Nappe will be crossed. In front of nite. The Lower Menilites with Brown Marls is the the Tarcău Nappe the Păltinoasa “Rabotage” Slice next lithostratigraphic unit. It is built up by well-lay- is situated. Furthermore, all along the front of the ered bituminous silicolites (menilites), which pro- unit such “rabotage” slices are common, until the ceed from the diagenesis of the Diatomaea rich muds. East Carpathians Bending Area (Vrancea Mts.). In Dark brown bituminous marly limestones (the so the Gura Humorului area boreholes situated on the called “Brown Marls”) are associated with the Lower external part of the Tarcău Nappe, penetrated in the Menilites. Very thin intercalations of bituminous Păltinoasa “Rabotage” Slice and, crossing a nar- clays or siltstones also occur. The Lower Dysodilic row Subcarpathian Nappe, reached the underthrust Shales follow between the Lower Menilites and the Foreland, there represented mostly by the Scythian Kliwa Sandstone. They are dark-coloured bituminous Platform. Similar geological situations were drilled clays or clayey siltstones, very thinly layered in sub- northward in the Putna Valley (near the Roumanian / mm. sheets (“paper-sheeted”). Intercalations of cm. to Ukrainian boundary). decimeter-fine quartzitic sandstones occur. Massive orthoquartzitic sandstones – Kliwa Sandstone - de- Stop 1.2: velop in the top of the succession of this outcrop. The Voronet. quartzitic grains of the Kliwa Sandstone are of aeolian In Voroneţ, along the river with the same name, the origin, subsequently transported and resedimented in Paszieczna Limestone (Lutetian) crops out. It is a the outer part of the Moldavidian sedimentary basin. pelagic lithographic white-yellowish limestone, with The source of this detrital material was situated in cherts and, sometimes, with resedimented Nummu- the Foreland, a conclusion documented by the lithic lites. They are followed by the Plopu Formation (see fragments of “Green Schists” (Dobrogean type) in- the next stop). cluded in the arenites. Of the same origin as the Kliwa In the southern part of the village the Voroneţ Mon- Sandstone are also the Lucăcești and the Fierăstrău astery, founded in the XVth century by Stephen the sandstones. The first three lithostratigraphic units of Great, Prince of Moldavia, will be visited. The outer the Oligocene belong to the Rupelian. The boundary and the inner walls are covered by frescoes. between the Rupelian and the Chattian runs within the Kliwa Sandstone. The complete succession of Stop 1.3: the “Bituminous Lithofacies with Kliwa Sandstone” West of Gura Humorului. above the Kliwa Sandstone consists of: the Upper Volume n° 1 - from PR01 to B15 n° 1 - from Volume At 1.6 km upstream from the western end of Gura Dysodilic Shales (the Oligocene/Miocene boundary Humorului a profile open on the left-hand bank of the runs within their lithostratigraphic unit), the Upper Moldova allows us to examine the Lutetian-Rupelian Menilites (without “Brown Marls”), the Goru-Mișina succession, specific for the external part of the Tarcău Formation (coarse-grained rocks rich in “Green Nappe (Suceviţa lithofacies). Above the Lutetian Schists” debris), the (lower) Evaporitic Formation Paszieczna Limestone, follows the two-component, (Burdigalian) (Săndulescu and Micu, 1988). dense rhythmically turbiditic sequence (“hieroglyphic

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu in theCentral-EastCarpathiansandinnermost ceeds fromaninternal(Carpathian)sourcesituated rhythms of30-100cm. The areniticmaterialpro- respect totheclayey pelites, withintwo-component sandy flyschwithmica-richarenites,whichprevail in ping out)isthe of thedigitationcropout. The oldestsequence(crop- banks oftheMoldova River thePaleogene formations Nappe, the Vama Digitationrespectively. Onboth ocene isrepresentedbythe the SenonianageforHanguFormation. The Pale- S and arichpelagicforaminiferassemblage(Ion- fragments of basal partgrainsof“GreenSchists”,limestonesand developed. The graded-beddedarenitesshow attheir marls/marly orlithographiclimestones)rhythms are arenites/marls) orthree-components(limyarenites/ turbiditic (flysch)formation. Two-components (limy The several SenonianandPaleocene sequencescropout. cated structure,alsobelongingtothe Tarc left-hand (northern)bankofMoldova, inanimbri- of SuhaBucovinean The localityofFrasinissituatedattheconfluence Frasin. Stop 1.4: ing totheinnersubunit (digitation)ofthe Tarc The localityof Vama issituatedinanareacorrespond- Vama. Stop 1.5: examples of supported byarichpelagicmicrofauna andbyscarce too. The Paleocene age(Antonescuetal.,1989)is for theHanguFormation) containing“GreenSchists” ness. The arenitic materialisofpolymictictype(as in whichthesandstonesareratherdominantthick- a sandy/marlyflyschwithtwo-component rhythms Subcarpathian nappes. Nappe aswellthoseoftheMarginal Folds and Miocene successionoftheexternal partofthe Tarc well asforthewholeCretaceous-Paleogene-Lower area fortheStrajaarenitesisexternal (Foreland), as Uppermost Paleocene-Lower Ypresian. The source formation is(accordingtothemicrofaunal content) may befrequentinthesandstones. The ageofthis pelites arered-purplish,greenandgrey. Glauconite arenites arepolymictic,withasilicamatrixandthe built upbytwo-component rhythmsinwhichthe younger thanthePutnaone.Itisavariegated flysch ă ndulescu, 1975; Antonescu etal.,1989)document Hangu Formation

Dyscocyclina Inoceramus Moldovi ă withtheMoldova. Onthe ţ isaSenoniancalcareous a Sandstone . The StrajaFormation is . Ammonites, inocerams . Ammonites, Putna Formation . Itrepresentsa ă u Nappe, . This is . This ă ă u u the out theirinterfingering. The youngestsequenceis Sandstone ismixed withKliwa Sandstone,stressing In theouterpartof Vama DigitationtheFusaru proceeding fromthesamesourcearea(Carpathian). stone, lithologicallysimilartothe Tarc stone follows. This isamassive, micaferoussand- Dysodilic Shales.Intheinnerparts,FusaruSand- It isanequivalent oftheLower Menilites andLower also rare,sideriticpelagiclimestonesaredeveloped. blackish claysandsilts,thinsandstoneinlayering tion the scale ofthe Vama Digitationabove thePlopuForma- as inthemoreexternal zones(seeabove). Intheinner Menilites Digitation, above thePlopuFormation, the in two lithofacies. Intheexternal scalesofthe Vama 1.3). The Lower Oligocenesequencesaredeveloped Sandstone follows thePlopuFormation (seeStop inlayered atdifferent levels. Above theMoldovi permost Paleocene also.Somered-purplishshalesare associations, isLower-Middle Eocene,possiblyup- The age,accordingtotheagglutinatedforaminifera nappes (BlackFlysch,Ceahl which overthrusts the Tarc In PrisacaDorneithefrontpartof Audia Nappe, (fide S Oligocene/Lower Mioceneboundaryrunswithinit with limyarenites,oftenconvolute, andmarls. The in relief. Sandstone andthe“BlackShale”Formation. egated Clay”Formation) situatedbetween thePrisaca quence ofthe Vraconian-Lower Senonian(the“Vari- may beobserved whichrepresentthecondensedse- downstream fromtheoutcrop slidedvariegated shales Formation ofthe samesedimentarybasin.100-200m canyons -fromthe Lower Cretaceous“BlackShale” by thefluxoturbiditiccurrents-perhapsinsubmarine pebbles” (“galetsmous”)of“BlackShales”reworked In theanalysedoutcropitispossibletoobserve “soft mica-bearing, proceedsfromtheCarpathiansource. material ofthePrisacaSandstone,polymictic,rich, tian-Lutetian (S of the Audia Nappeinthisarea;itsageisMaastrich- Sandstone lage, massive sandstonesrepresentingthe m westofthewesternborderPrisacaDorneivil- On theleft-handbankofMoldova River, 700 West ofPrisacaDornei. Stop 1.6: Vine ă ndulescu etal.,1995). “Shaly Horizon” ţ i and the ș cropout. This isthe youngestformation u Formation, ă ndulescu etal.,1992). The arenitic Lower DysodilicShalescrop out,

atwo-component flysch withgrey, dark-grey and ă u one,iswellexpressed ă u) oftheFlyschZone. ă u Sandstone, 24-05-2004, 15:43:31 Prisaca Lower ţ a GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

The town of Câmpulung Moldovenesc, about 10 km precedes the “arrival” – at the end of the Albian - of long, develops along the Moldova Valley, more or less the Transylvanian Nappes, the sedimentary klippen parallel to the tectonic structures. involved within the wildflysch proceeding from the front of the nappes in movement. Stop 1.7: From the Izvorul Alb Brook or from the suburbs, Câmpulung Moldovenesc – Izvorul Alb brook. downstream from the town of Câmpulung Moldove- The frontal part of the Bucovinian Nappe is well ex- nesc it is possible to see the Rarău Mts. The white posed in the lowermost part of the Izvorul Alb Brook, cliffs which are visible correspond to the Middle Tri- at the periphery of the town. At the same time it cor- assic dolomites and the Urgonian limestones, tectonic responds with the anticlinorium which limits the ex- outliers of the Transylvanian nappes. ternal limb of the Rarău Syncline. In the Izvorul Alb brook a complex of anticline folds are marked by the Stop 1.8: outcropping of the Anisian massive dolomites (shal- West Sadova. low water, with intratidal “cracking breccia” zones). On the left-hand bank of the Moldova River, 120 m With a large erosional gap the Pojorâta Formation, west of the railway/national road crossing, an anticline which is a two-component flysch sequence, 700-800 of the Bucovinian Nappe can be examined, marqued m thick, follows. The arenites are polymictic (sub- by the outcropping of the “Aptychus Beds” Formation greywackes) with limy or marly matrix, the lutites are of Tithonian-Valanginian age. This formation consists marls. Red and yellowish marly pelagic limestones of well bedded, white, yellowish, grey or red-purplish are intercalated at different levels. The age of the lithographic limestones, sometimes with cherts. Typi- Pojorâta Formation is Tithonian-Neocomian, stressed cal assemblages of Tintinnides (Calpionella alpina, by their Tintinnides and Aptychus content (Lamel- C. elliptica, Crassicolaria massutiniana, C.parvula laptychus beyrichi, L. beyrichi var. fractocostata and followed by Tintinopsella carpathica, Calpionellites Lamellaptychus gr.A and Calpionella alpina, C. el- darderi and Calpionellopsis simplex - Săndulescu, liptica, Tintinopsella carpathica - cf. Turculeţ, 1971; 1976) corroborated with the Aptychus fauna (Turculeţ Săndulescu, 1973; Săndulescu et al., 1976). Above 1971) support the above-mentioned age. The “Apty- one of the dolomitic anticlinal cores, between them chus Beds” Formation is, more or less, a stratigraphic and the Pojorâta Formation, red-purplish silts may be equivalent of the Pojorâta Fm., but with a more observed. They may be an equivalent of the “Radi- internal position, stressing that the arenitic material olarite Beds” of Callovian-Oxfordian age, which in of the latter has an external source in respect to the other areas of the Rarău Syncline are well developed. paleogeographic position of the Bucovinian Nappe, The filling of the Rarău Syncline and consequently, the source being situated in the area corresponding the youngest sedimentary formations of the Bucovini- paleogeographically to the Subbucovinian Nappe. On an Nappe, is represented by the Wildflysch Formation the western limb of the complex anticlinal structure of of (Upper Barremian ??) Aptian-Albian age (Mutihac West Sadova the Muncelu Sandstone (conglomerates and Bratu, 1965; Săndulescu, 1975). It can be exam- and coarse grained sandstones outcropping in a large ined along several km in the Izvorul Alb Brook, up- quarry) of Hauterivian age, develops. This Sandstone stream of the confluence with the Limpede Brook (the is recorded also, slighty discordant (?) above the Po- dolomites quarry). Wildflysch is a mixed formation jorâta Formation. with a dark-coloured, clayey or siltic-clayey matrix The Wildflysch Formation constitutes, normally, the in which sedimentary klippen from different rocks of filling of the Rarău Syncline, but with an asymmetri- different ages are incorporated, but all older than the cal position: the post-Triassic formations known on matrix. In the Bucovinian Wildflysch Formation the the outer limb of the syncline are absent on the inner sedimentary klippen – of very different sizes - belong one where the wildflysch lies directly on the Triassic to the different lithofacies of the Transylvanian Nap- dolomites and the “Radiolarite Beds”, both cropping PR01 to B15 n° 1 - from Volume pes (basic and ultrabasic rocks, Middle and Upper out in Pojorâta in several quarries. From Pojorâta Triassic limestones and dolomites, Lower and Middle the fieldtrip follows the Moldova Valley upstream to Jurassic sandy-marly rocks, Upper Jurassic-Neoco- Breaza. In this tract the road crosses the metamorphic mian and Urgonian (Barremian) massive limestones) formations of the Bucovinian Nappe and, once more, (Săndulescu, 1975, 1976; Săndulescu et al., 1981). the Rarău Syncline. The sedimentation of the Wildflysch Formation

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu the Tulghe of thePutna Valley consistofmetamorphicrocks Brook (lefttributary ofMoldova River). Bothslopes The field-trip returnstoPojorâtaandentersthePutna tween thelatterandCeahl the Transylvanian andBucovinian nappes andbe- from erosion. They sealthetectoniccontactsbetween grained sandstonesofCenomanianagearepreserved cally transportedatthebaseof Tulghe mites, whichmaybelongtotheRebraSeries,tectoni- Seriesformations.Massive metamorphoseddolo- m above thebrook,onitsslopes,by Tulghe sedimentary rocksaretectonicallyoverlapped, at50 blackish siltstone coflagellate assemblages) the window areLower Jurassic(accordingtothesili- cover thedolomites. The youngestsequenceknown in siliceous silts,possiblyLadinian,certainly Triassic, tions croppingoutarethe Anisian dolomites. Thin red Subbucovinian Nappeareexposed. tectonic window thesedimentaryformationsof ian Nappe. At 4kmalongthePutna Valley withina in theP rocks ofLadinian/Carnianage.Furthernorthward lent oftheOltNappe,whichalsocontainsultramafic Outlier cropout. This nappeoutliermaybeanequiva- peridotites cline. Onthesummitssituatednorthofbrook Formation (or Ladinian?) by Anisian dolomitesandCallovian-Oxfordian (?) morphic ous flysch)cropsout;itisoverthrust bythe of theCeahl examined: onthefirst 300mthe of thechurch,following cross-sectionmaybe tributary oftheMoldova River, inBreaza,front less developed thantheinternalone.Onaleft-hand asymmetric shapeinthisarea,withtheexternal limb is locatedintheaxisofsyncline,whichhasan 1973; S the Transylvanian nappesaredeveloped (S ultramafic rockswhich representatectonicoutlierof Formation ofthenorthensectorRar time andweathersituation). Breaza tectonicoutlierwillbeconditionedbythe Breaza Ultramafic Tectonic Outlier(thevisitofthe Stop 1.9: Putna ValleyTectonic Window. Stop 1.10: ă ă rocksoftheBucovinian Nappe,overlapped ndulescu andRusso-S ltini ș , asarule,representsthefilling ofthesyn- and ă

Series, whichbelongstotheBucovin- u Nappe(Tithonian-Neocomian calcare- ș Summitconglomeratesandcoarse- “Radiolarite Beds” serpentinites intercalations. The Subbucovinian limonitic sandstones ă oftheBreaza Tectonic u Nappe. Above the Wildflysch ă The oldestforma- ndulescu, 1981).It Sinaia Formation ; the ă ș Wildflysch u Syncline, ă ndulescu, ș meta- with ern margin oftheMestec Mestec From the Valea PutneiRailway Stationupto window. the Infrabucovinian nappescropsoutwithinatectonic Carpathains unit,theIacobeniNappe,highestof Bistri weak bituminous(“stinking”) Anisian dolomites and phylliteswithintercalationsofmetabasalts;(3) mation” some kilometerssouthwards; (2)the the oxidationzone. The principalminesarelocated Mn-carbonate andsilicates,enrichedinMn-oxydes level ofsyngeneticmanganeseores,whichconsist north ofPuciosuBrook. The blackquartzitesmarkthe or limestonesandcalcschists,areknown, southand black quartzites;thinintercalationsofmetabasalts itic andchloritic-graphiticschists,withtwo levels of (Bercia etal.,1975)representedbysericitic-quartz- of the Tulghe beautiful view opensoutontheBistri reached 5kmwestof Valea PutneiRailway Station,a In theMestec sion asinthe Valea Putnei Tectonic Window. tions whichshows thesamelithostratigraphicsucces- nappe above theSubbucovinian sedimentaryforma- superposition ofthemetamorphicformations of theBucovinian Nappeisstressedbythetectonic Valea PutneiRailway Stationtheerosionalcontour The fieldtrip continues upstream,westward. At the dolomites. bucovinian Anisian drilled intheBucovinian NappeandreachedtheSub- situated 100mwestofthefault). The boreholewas placement ofabout500m(controlledbyaborehole border ofthewindow isavertical fault withadis- after Kräutnerin:Sndulescuetal.,1981. The western Complex” (Tg2)ofthe Tulghe and schistscropout. The rocksbelongtothe“Median of asmalltributary, athinbankofgraphitequartzites window. Inthethalweg ofthePutnabrook,infront Series,canbeexamined attheeasternborderof the Tulghe examine: (1)the are exposed. Upstream-downstream itispossibleto formations oftheIacobeniInfrabucovinian nappe of theSubbucovinian Nappeandthesedimentary hand slopeofPuciosuBrook,thebasalsequence Along thenationalroad,whichrunsonright- Puciosu Valley Cross Section. Stop 1.11: ţ a Aurie Valley, wherethe deepestCentralEast ă ni (seealsobelow), built upofmetapsammites ș ș Pass andfromtheredown untilthewest- SeriesoftheSubbucovinian Nappe. ă

ș ni SeriesoftheSubbucovinian Nappe ș Black QuartziticFormation

Pass (1083minaltitude),whichis ă ni ș Village, theroadcrosses ș

Series.Descriptions “Argestru For- ţ a Mts.andthe 24-05-2004, 15:43:35 (TG2)

GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

and limestones. Up on the slope, with a large strati- Central East Carpathians nappes (Crystalline-Meso- graphic gap, Middle Jurassic limy sandstones follow zoic Zone). The Infrabucovinian, Subbucovinian (Săndulescu, 1976). and Bucovinian nappes crop out represented by their Before the first houses in the Iacobeni locality, down- metamorphic formations. stream from a right-hand tributary, a small window of Infrabucovinian Anisian dolomites are exposed Stop 2.1: underneath the metamorphic rocks of the “Argestru Broșteni-Cotârgași. Formation”. The western border of the window is a At the downstream margin of Broșteni and 700 m vertical fault. About 350 m downstream the well-lay- upstream, the confluence of Cotârgași Brook with the ered Anisian dolomites crop out in a large quarry. At Bistriţa River, the frontal contour of the Bucovinian its uppermost part, massive dolomites seem to cover Nappe crosses the Bistriţa Valley. 200 m upstream the layered dolomites with tectonic disconformity. of this contour a small tectonic window is opened Downstream, west of the large dolomite quarry, in the metamorphic formations of the nappe; within towards the Bistriţa Aurie River, blocks and frag- this window Anisian dolomites crop out. They belong ments of Lower Triassic quartzitic sandstones to the sedimentary sequence of the Subbucovinian and conglomerates as well as purplish siltic clayey Nappe. The dolomites were transported as a tectonic shales occur. Near the confluence between Puciosu outlier (“lambeau de charriage”) by the Bucovinian Brook and the Bistriţa Aurie River, along the road to Nappe. Such situations are frequent all along the fron- Ciocănești, an outcrop of muscovite-quartz schists tal contour of the Bucovinian Nappe (see also Stop with chloritised biotite can be examined. It is ascribed 2.10). Downstream from the front of the Bucovinian to the Bretila Series, which also crops out several Nappe the innermost unit of the Flysch Zone – known hundreds of meters upstream on the left-hand bank in this area - crops out. It is the Cotârgași Unit (Scale). of the river, where gneisses may be recognized too. The Cotârgași Formation can be examined in a large In the metamorphic schists axes of mesoscopic folds outcrop where well-bedded pelagic micritic or marly trend N 20 W / 10 NW. Descriptions after Kräutner in: limestones are exposed; they show relatively rare in- Săndulescu et al., 1981. tercalations of polymictic graded bedded sandstones. The tectonic framework and the age of the “Argestru In the Cotârgași Formation at different levels and with Formation” was subject of controversy. Firstly it was different thicknesses, polymictic (amphibolites, mi- considered a lithostratigraphic Paleozoic unit which caschists, chloritic phyllites, quartzites, Triassic and/ builds up an independent tectonic unit (“Argestru or Jurassic dolomites and limestones) limy breccias Unit”) situated between the Subbucovinian Nappe and/or microbreccias, are inlayered. From the lower and the Infrabucovinian nappes. Afterwards the “Ar- and middle part of the formation poor Tintinnide as- gestru” sequence was considered an equivalent of the sociations (with Calpionella alpina, C.elliptica, Tinti- Rebra Series or later of the Bretila Series, squeezed nopsella carpathica) stress the Tithonian-Neocomian in both interpretations at the base of the Subbucovin- age. The upper third, where the breccias prevail, may ian Nappe (Kräutner, 1980, 1988; Balintoni, 1985, be Hauterivian or even Barremian. 1997). Following its tectonic position between the Central East Carpathian nappes and the Ceahlău one, the DAY 2 Cotârgași Unit may be correlated with the Baraolt Vatra Dornei – Bicaz - Lacul Roșu - Gheorghieni Nappe known southward in the inner Bend Area. In - Miercurea Ciuc fact the lithofacies of the Cotârgași Formation shows some similarities with the isochronous sequences of Aims: Along the Bistriţa Valley, south-east of Vatra the Baraolt Nappe. The fieldtrip proceeds downstream. For more than 20

Dornei, the formations which built up the inner units PR01 to B15 n° 1 - from Volume of the Flysch Zone (the Ceahlău, Convolute Flysch km the Bistriţa Valley crosses the Sinaia Formation and Audia nappes) can be examined, as well as the in- of the innermost sub-unit (digitation) of the Ceahlău ner part of the Tarcău Nappe. In the upper Bicaz Val- Nappe, the Ciuc Digitation respectively. ley the Hăghimaș Syncline (Bucovinian Nappe and Hăghimaș Transylvanian Nappe) will be crossed. Stop 2.2: From Vatra Dornei the fieldtrip follows the Bistriţa Sinaia Formation in the Bistriţa Valley. valley downstream. Until Broșteni it crosses the The Sinaia Formation (4-5 km in thickness) is a

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu calcite andalsosomezonesofschistosity. Sinaia Formation shows frequentdiaclasesfilled with dolomites andlimestones,quartziticsandstones). The and epizonalmetamorphics, Triassic and/orJurassic ized byinlayeringsoflimypolymicticbreccias(meso- (limy sandstonesanddarkcolouredmarls)character- peregrina) per Member,Hauterivian inage(with supporting theBerriasian-Valanginian age. The Up- carpathica, Calpionellitesdiv.sp. The presenceof (see above) andrepresents75-80%ofitsthickness. shows thetypicallithofacies oftheSinaiaFormation age consideredas Tithonian. The medianmember alpina and scarcesandstones.Inthelimestones marls) withinlayeringsofmarlypelagiclimestones The lower oneisdominantlypelitic(marlsandsiltic Sinaia Formation canbedivided intothreemembers. taking intoaccountthewholeCeahl containing Tintinnides atdifferent levels. Generally, ymictic, themarlylimestonesarepelagic,micritic, limestones), 25-75cmthick. The sandstonesarepol- / marlylimestones,limysandstonesmarls ponent rhythms(limysandstone/marls,siltymarls calcareous flysch,withturbiditictwo- andthree-com- Ugra Formation atS Stop 2.3: also onthewesternbankof(antropic)BicazLake, stream ofthelarge viaductfromPoianaLargului, and On theright-handbankofBistri Piscu cuBraziFormation atPoiana Teiului. Stop 2.4: glomerates. the PiscucuBraziFormation andtheCeahl the Ceahl Ciuc one. The specific formationsofthis sub-unitof enters theDur Downstream ofS inward relative tothesedimentarytrough. mafics andultramafics) itssourceareabeingsituated sic andJurassiclimestonesdolomites,aswell quartzites, meso-andepizonalmetamorphics, Trias- rial ispolymictic(subgreywacke-type) (quartzand prevail over marlsorsiltymarls. The areniticmate- thick, two-component rhythms,sandstones(65-90%) sandy flysch–theUgraFormation. Inthe30-150cm tion arerepresentedbyaturbiditicandfluxoturbiditic The Barremian-AptianformationsoftheCiucDigita- (frequent ă , isrepresentedbyatwo-component flysch u Nappe,above theSinaiaFormation, are ă u Digitation,external inrespecttothe ) ă Calpionella elliptica, Tintinopsella and vine ă C.elliptica ș vine ti near Topliceni thefield trip ș ti locallity. was determined, werefound,the ţ a River, 1kmup- ă u Nappe,the

Peregrinella Calpionella ă u Con-

and is built upofUrgonian limestoneswith at thenorthernendofBicazLake (neartheviaduct).It At Poiana Teiului acalcareousisolatedrockissituated up theCeahl are the Albian Ceahl along thenorth-easternslopeofBicazLake. Nappe. FromPoiana Teiului thefieldtrip proceeds Cordillera -andtransportedtothebaseofCeahl of theOuterDacidiantrough–Peri-Moldavian sents atectonicslice,pulledoutfromtheoutermargin tian. The youngestformationoftheDur Maicilor Sandstonesaredeveloped intheUpper Ap- different levels (fide S cording tothedifferent ammoniticfaunas recordedat age ofthePiscucuBraziFm.isBarremian-Aptianac- m ofsandstone(PoianaMaicilorSandstones). The cu BraziFormation grows moremassive with0.5-1.5 is marlyorsiltymarly. Toward itsupperpartthePiscu Ugra sandstones–seeabove), thepeliticcomponent sandstones arepolymictic(samecompositionasthe component flysch,withrhythms10-50cmthick. The the Stop 2.6: above the Ceahl sandstones of theConvolute FlyschNappe. of theCeahl of thetectoniccontactbetweenouternmostpart viaduct, thefieldtrip reachestheerosionalcontour About 4kmdownstream fromthePoiana Teiului Flysch Nappe. Frontal contact oftheCeahl Stop 2.5: sive sandstonesrepresentthe microconglomerate intercalationscropout. The mas- route, massive sandstoneswithconglomeratesand ates. Cotumba SandstoneandLe 1985; S (S blages specified a Vraconian-Lower Senonianage is fullydeveloped, themicropaleontologicalassem- areas oftheEastCarpathians,wherethisMember Member is Vraconian-Cenomanian; insomeother this lower sequenceoftheUpperConvolute Flysch or lessfrequentinlayeringsofredmarls). The ageof component turbiditicrhythms,10-20cm,withmore ă ndulescu J.,1976; Antonescu andS Piscu cuBraziFormation Orbitolina ă About 1.6kmdownstream along thenational u Nappe(?theBodocDigitation)isoverthrust ă ndulescu etal.,1993). Upper Convolute FlyschMember representing theoutermostsub-unitof

ă ă u Mts.,visiblesouthofBicazLake. u Nappeandtheyoungestformations (Barremian-Lower Aptian) andrepre-

ă u Conglomerates,whichbuilt ă ndulescu, 1990). The Poiana ă Cotumba Sandstone u Nappe/Convolute crops out.Itisatwo- Massive micaferous ţ e ș ti Conglomer- ă Pachyodonta u Digitation ă ndulescu, 24-05-2004, 15:43:39 (two- ă u GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

situated at the middle part (Middle- and a part of the (actually underthrust – Figure - below the nappes of Upper Albian) of the Convolute Flysch Formation. It the Flysch Zone). The “Silesian Lithofacies” is also is a quartzitic-micaferous sandstone, graded bedded known in the more external nappes (Tarcău and Mar- or with fluxoturbiditic features, showing thin to very ginal Folds) and represents the outer development of thin (joints) intercalations of dark or grey marls. The the Flysch Zone sedimentary basin. It was sedimented Leţești Conglomerates develop as lenses of different in euxinic conditions, the dark shales having a rela- sizes within the Cotumba Sandstone. They are domi- tively high content of bituminous material. nantly quartzitic, with few lithic fragments repre- A few hundred of meters downstream from Stop sented by metamorphic schists. The source area of the 2.8 the field-trip penetrates into the Tarcău Nappe Cotumba Sandstone and of the Leţești Conglomer- outcropping area. The Hangu Formation (see Stop ates, as well as for all arenites of the Convolute Flysch 1.4) crops out in numerous points. 700-800 m before – represented by the Peri-Moldavian Cordillera - are reaching the Bicaz Dam the “Black Shales” Forma- situated on the inner border of the Convolute Flysch tion crops out in the core of the Cârnu Anticline, a sedimentary trough. structure of the Tarcău Nappe. Stop 2.7: Stop 2.9: Lower Convolute Flysch Member at Chiriţeni. Tarcău Sandstone at the Bicaz Dam. The Bicaz 3.5 km downstream from the preceding stop, several Dam is built on massive Tarcău Sandstone. The lat- outcrops of Convolute Flysch may be visited. This is ter can be examined near the western margin of the a two-component flysch, with rhythms of 10-25 cm dam. It is a typical sandy flysch with two-components of arenites (limy or marly sandstones, graded bed- (quartzose-micaferous, with rare lithic fragments, ded, frequently with convolute laminated bedding at arenites and clayey lutites) rhythms of 30-120 cm.. the upper part) and pelites (marls or silty marls, dark, The age of the Tarcău Sandstone (total thickness of grey or green). According to the micropaleontological about 3-4 km) is Upper Paleocene-Middle Eocene and palynological assemblages, this Lower Convolute (Lutetian), according to the micropaleontological Flysch Member is of Lower and partly of Middle data (agglutinated foraminiferas assemblages); at the Albian age. In the Bicaz Lake area the Lower Convo- Bicaz Dam the uppermost level of the Tarcău Sand- lute Flysch constitutes the frontal part of the nappe, stone (with Cyclammina amplectens and Sphaeram- overthrusting the Audia Nappe. mina subgaleata) crops out also showing red clay intercalations. The Tarcău Sandstone is followed by Stop 2.8: a two-component flysch (limy sandstones / marls and “Black Shales” Formation in the Audia locality. clays) with rhythms of 10-25 cm of Upper Eocene age The Audia locality and brook are situated in the Audia – the Podu Secu Formation – with inlayerings of Nappe outcropping area. The main formation known Globigerina Marls (see also stop 1.3) at the terminal in this nappe, developed in the so-called “Silesian levels. The “Shaly Horizon” of the lower part of the Lithofacies”, is the “Black Shales” Formation of Bar- Oligocene and the Fusaru Sandstone (see Stop1.5) remian-Albian age (according to the palynological follows. assemblages and the ammonitic faunas). This Forma- From the Bicaz Dam the field-trip reaches the town tion may be divided into three sequences: Member of Bicaz and from there it turns westward along the with pelosiderites (lower), Shaly Member (middle) Bicaz Valley. It will cross the whole inner part of the and Quartzitic Sandstones with glauconite Member Flysch Zone in reverse sense (Audia, Convolute Fly- (upper). The specific lithology is represented by black sch, Ceahlău nappes) as the field-trip crossed them in or dark-grey clays and silty clays. Different inlayer- the Bistriţa Valley. ings make the difference between the different mem- bers: calcareous sandstones and sideritic limestones Stop 2.10: PR01 to B15 n° 1 - from Volume (pelosiderites) in the lower member, black jaspers The front of the Bucovinian Nappe at the locality (lyddites) in the middle and largely developed graded of Bicazul Ardelean . bedded quartzitic sandstones in the upper one. The On the right-hand bank of the Bicaz River, at the con- sandstones also contain lithic fragments of Dobrogean fluence with the Dămuc Brook in the western part of type “Green Schists”, which is proof that the source Bicazul Ardelean, the front of the Bucovinian Nappe area of the arenites is situated within the Foreland as well as a tectonic (“rabotage”) outlier carried from

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu Lower Jurassic (?) dolomites tratigraphic successioncanbeexamined : the SIn u b b u c o v i n i aexposed (S n o u t l i elithos- rfollowing the the Subbucovinian sedimentaryenvelope, arewell The External LimboftheH Stop 2.11: mites along theBicaz Valley, themassive At 1,5kmwestfromtheBucovinian front,upstream Jurassic sandylimestones by theoutliersofH The Wildflysch Formation istectonicaly overlapped that oftheRar flysch Formation follows, withasimilarlithologiyto be examined. With anangulardiscordance, the Wild- where ascaleinvolving MiddleJurassicrocksmay be demonstratedontheleft-handbankofBicaz of thesyncline–pre-LateJurassicimbricationmay ing intoaccountthegeneralstructureofouterlimb develop attheirbase. A pre-Barremianoreven -tak- Lower Triassic quartziticsandstones upstream untiltheeasternmargin ofthetouristiclo- be examined inthe BicazGorges (Cheile Bicazului) the quarries. The H erates cropoutalongtheroad2kmupstreamfrom constitute thePost-Tectogenetic Cover. The conglom- Conglomerates Nappe aretransgressively covered bythe 2.11). Both Wildflysch Formation and Transylvanian (the biglimestonesquarriesupstreamfromStop limy polymicticbreccias etc. Discordantly, thinbedded Bositra buchi,Zeilleria with inlayeringsofmetabasaltsandporphyroids). ries (sericitic-quartziticandsericitic-graphiticschists sented bymetamorphicformationsofthe Tulghe FThe r o n t arepre- lis pNappe aBucovinian rthe tof considered thePutna Valley succession(Stop1.10). third typeofSubbucovinian lithostratigraphymaybe domain, withdifferent paleogeographicevolutions. A proceed fromdifferent partsoftheSubbucovunian in theNeocomian. This two typesofsuccessions mian pelagiclimestones,withbrecciasinlayerings Callovian-Oxfordian radiolarites, Tithonian-Neoco- cession withrespecttotheGuraD (cf. Stop2.1too). Another lithostratigraphicalsuc- nappe such“Rabotage”Outlierscropoutfrequently limestones mark theouterlimbofH ă . Along thefrontalpartofBucovinian representing themainpartofoutlier/ ndulescu, 1975). ă u Syncline(seeStop1.7). (Vraconian ?–Cenomanian)which ă coarsegrained ghima div.sp., ă ghima ș with inlayeringsof Transylvaniancan Nappe with Parkinsona parkinsoni ș Tithonian limestones/

Transylvanian Nappe ă ghima quartzites/Middle Trocholina ă ghima ă mucului shows: discontinously Anisian dolo- ș Syncline: ș Syncline. Bârnadu Anisian div.sp., marly ș Se-

Berriassiella privasensis Calpionellopsis oblonga,Neocomitesneocomiensis, with is representedbywelllayeredpelagiclimestones div.sp., Elipsactinia, Cladocoropsis mirabilis, Clypeina carinata contain Pachyodonts [ reddish limestonesandcalcareniticbrecciaswhich by Urgonian-type ones (white,yellowish andlight limestones arecovered, withaslight discordance, from theconfluence(about600m),Neocomian clearly above theBerriasianformations.Downstream lar lithology(massive neriticlimestones)andfollows careous algae( alpina, T.elongata, Kurnubia, Kilianina, gastropods ( light colouredneriticlimestoneswhichcontain 1975). The Tithonian isrepresentedbymassive of theH the Bic In theareaofconfluencebetweenBicazwith Bicaz Gorges (confluencewiththeBic Stop 2.12: mafic andultramafic rocks which the erosion hasexposed atectonichalf-window from around theChalet“CheileBicazului”(BicazGorges) On theleft-hand(northern)slopeofBicazRiver “Cheile Bicazului” Tectonic Half- Window. Stop 2.13: H cality ofLacuRo remian ??] Aptian formationsofthe Wildflysch). are inbeddedassedimentaryklippenin([UpperBar- Barremian asawholebut notyoungerbecausethey these limestonesisatleastLower Barremian,possibly well ascalcareousalgae andbriozoarians;theageof serpentinites whichalsoproceedfromtheobducted at thebaseofH slope oftheBicazRiver, 300mbehind theChalet the massive Tithonian limestones.Ontheleft-hand Jurassic oceaniccrust. The successioncontinueswith senting thefirst sedimentarylevels above theMiddle siliceous shalesandredmarls(Kimmeridgian),repre- basalts andamygdaloidbasalts,overlapped bysiltic may beexamined: above the Wildflysch, pillow-lava bank oftheBicazRiver thefollowing succession and Russo-S ă ghima Calpionella elliptica, Tintinopsella carpathica, Actinoporella podolica ă ], large foraminiferas [ ș jel the Tithonian-Neocomian succession ă Wildflysch Formation Nappe. At thebaseoflatter, bodiesof ghima ă Nerinea ndulescu, 1981). Along theleft-hand Salpingoporella anulata ș ș Nappeisexposed (S u. ă ), foraminiferas( ghima Requienia . The Neocomianhasasimi- ș emplaced(S Nappearetransported Orbitolina conica etc. The Berriasian cropsoutbelow the div.sp. ) aswell ă jel Brook). Trocholina ă Toucasia ă etc.), cal- ndulescu, ndulescu 24-05-2004, 15:43:42 ] as

GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

oceanic crust emplaced at the base of the Transylva- (N. Stan, 2000). nian nappes. The fieldtrip reaches the Pângăraţi Pass (1257m) situ- From the Chalet “Cheile Bicazului” the fieldtrip ated on the main East Carpathian crest, separating the continues upstream. After 2 km crossing the massive Transylvanian hydrographic basins from the Molda- Tithonian limestones the road arrives at the inner vian ones. From the Pângăraţi Pass a panoramic view erosional contour of the Hăghimaș Nappe and enters of the Volcanic Chain and the Gheorgheni Quaternary the inner limb of the Hăghimaș Syncline. There the Depression opens westwards. Eastwards the Meso- Mesozoic sequence of the Bucovinian Nappe crops zoic Hăghimaș Syncline with the Hăghimaș Nappe out largely. in the axial part shows its panoramic view. From the Pângăraţi Pass downstream along Belcina Brook Stop 2.14: (left-hand tributary of the Mureș River) the metamor- Lacu Roșu - Bucovinian Middle Jurassic-Triassic phic formations of the Tulgheș Series of the Bucovin- formations. ian Nappe are crossed. Below it the Negrișoara Series, Along the northern bank of the Lacu Roșu (Red belonging also to the Bucovinian Nappe metamorphic Lake), a lake generated in 1837 by a natural dam basement crops out in several points. The Pietrosu formed by a huge landslide of the right-hand slope Gneisses (cropping out 4 – 4.7 km east of Gheorgh- of the Bicaz Valley, the following geological section eni), a schistose gneiss with relict phenoclasts of vio- (upside/downside) may be examined: sandy lime- laceous quartz can be examined. From Gheorgheni stones (several hundred meters) with massive layer- the fieldtrip turns toward south proceeding to Miercu- ing (Aalenian-Bajocian) / oolithic-hematitic silty rea Ciuc. After crossing the Gheorgheni or Ciucul de limestones (50-200 cm) containing condensed fauna Sus (Upper Ciuc) Quaternary Depression, situated of Sinemurian-Carixian age / rauhwacke dolomites between the Volcanic Chain (west) and the Crystal- and limestones (20-70 m) with calcareous algae line-Mesozoic Zone (east), 11 km from Gheorgheni in (Upper Anisian-Lower Ladinian) / massive Anisian the village of Voșlabeni, the median part of the Rebra dolomites. Series crops out. In the filling of an inward overturned syncline, situat- ed westward in respect to the previously analysed se- Stop 2.16: quence, above the Middle Jurassic sandy limestones, Voșlăbeni Quarry – Rebra Series well layered radiolarites of Callovian-Oxfordian age (middle sequence). are exposed. The Rebra Series is the lowermost series known in the metamorphic basement of the Bucovinian Nappe. Stop 2.15: The same position is recorded in the Subbucovinian Hăghimaș Granitoids. Nappe. The Rebra Series is divided into three For- Below the Anisian dolomites or the Lower Triassic mations. The middle one – named in this area the quartzitic sandstones and/or conglomerates of the Voșlăbeni Formation – consists of dolomitic mar- inner limb of the Hăghimaș Syncline, the basement bles with tremolite and talc, exposed in the Voșlăbeni of the sedimentary formations consists of compact quarry. From Voșlăbeni to Miercurea Ciuc metamor- red augengneisses, with fine intercalations of biotite- phic formations (mainly Rebra Series) of the Bucov- muscovite paragneisses. Their general attitude is N inian Nappe will be crossed as well as the Ciucul de 50-67 W/55 NE. The red gneisses consist of quartz Mijloc (Middle Ciuc) Quaternary Depression. (35%), orthoclase (49%), oligoclase (11%) and bi- otite (5%). A gradual transition can be seen from red DAY 3 orthogneisses to gray granular gneisses, which also Miercurea Ciuc - Brașov - Sibiu carry garnet. The augengneisses are interpreted as Volume n° 1 - from PR01 to B15 n° 1 - from Volume laminated granitoids.The Hăghimaș Granitoids are A i m s : In the Brașov and Perșani Mts. it is possible to a part of the Bretila Series which is overthrust above approach the problems concerning the correlation of the Tulgheș Series, during the Paleozoic (a Caledo- the East and South Carpathians. nian or a Hercynian tectonic event). This overthrust, From Miercurea Ciuc the fieldtrip proceeds south- corresponding to the Rarău Nappe, is a structure of wards, downstream along the Olt Valley. In the the metamorphic basement of the Bucovinian Nappe suburbs of the town, on the left-hand slope of the and was not involved in the Mesozoic tectogeneses valley small quarries are opened in lava flows of py-

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu above the The S frontal partoftheGeticNappe. accentuates theexistence ofastratigraphicgapinthe ally developed intheotherpartsofGeticDomain, the Callovian-Oxfordian radiolariteswhichareusu- sented bymassive neriticlimestones. The absenceof of MiddleJurassicage. The UpperJurassicisrepre- sandstones the south-eastendofvolcanic chain. At Tu Depression, theOltRiver (andthefieldtrip) crosses crossing theCiuculdeJos(Lower Ciuc)Quaternary alkaline volcanic arc oftheEastCarpathians. After ? –Lower Pleistoceneage,whichbelongtothecalc- roxene- andhornblende-andesitesofUpperPliocene of theLower Jurassic,MiddleJurassic a few silticblackshalesoftheGrestnerLithofacies Mts. area,whichbelongtotheGeticNappe. After the wholePost is built upofJurassicformationssimilartothose In thetown ofS Getic Nappe. S Stop 3.1: material consistsoflimysandstones,whichwere in theXV The BlackChurchisafamous Catholicchurchbuilt an earlymedieval citywithmany importantvestiges. Bra of theCeahl Ceahl favourable), alongtheskyline, across-sectionofthe sion, itispossibletoreconstruct(iftheweather Between H per Pliocene-Pleistoceneformations. the innerpartofCarpathianBend Area -withUp- whole complex developed Quaternarydepressionsof Gheorghe QuaternaryDepression,filled -asthe From Ghidfal (both sub-unitsoftheCeahl tween theCiucDigitationandBodoc are developed. At Malna Cretaceous flyschformationsoftheCeahl ries. Ontheleft-handslopeandtributaries, Lower (Lower Pleistocene)areexposed intwo large quar- Valley, two subvolcanic bodiesofbasaltoidandesites the Micfal Pleistocene oreven Holoceneage.Downstream, in ture iswellpreserved. Itisavery youngvolcano of spa, eastofthevalley, theSfânta Ana volcanic struc- ă cele -Jurassic formations inthefront ofthe ș ov isoneofthemaintowns of Transylvania. Itis ă ă u NappeandthefrontofGeticNappe. cele JurassicGeticformationsareoverthrust ă Piscu cuBraziFormation th ă u area,ontheright-handslopeofOlt ă centuryinGothicstyle. The building follow, hostingasilloftrachytes,also rman andBra u Nappe. ă

u theOltRiver runswithintheSfântu ă ă varu Mts.-Codlea-PiatraCraiului cele, themainpartofBonlocHill ș ș thetectoniccontactbe- ov, southoftheDepres- ă u Nappe)iscrossed. (see Stop2.4) quartzitic ă u Nappe ș nad Romanian printingoccurred. the OrthodoxSaintNicholasChurch,wherefirst city museum.SouthoftheBlackChurch,upstream,is Council Squareistheoldcentreofburg, witha in theCatholicorProtestantchurches Transylvania. The organ ofthechurchisonebiggestorgans slope Hill, notfar fromthecentreoftown. Onitseastern Dealul MelcilorHillisthenorthernendof Tâmpa Quarry. Bra Stop 3.2: East Carpathians. longs) withtheInfrabucovinian nappesof theCentral the GeticNappe(towhichCristiansectionbe- (Stop 1.12).Consequentlyitispossibletocorrelate sian dolomitesandlimestonesoftheIacobeniquarry Cristian-Vulcan area,maybecorrelatedwiththe Ani- The Anisian limestonesofGuttensteintype,the angular discordance. type formationsoverlie the Triassic formationswith assic was foldedbeforetheLower Jurassic;Gresten- palynological assemblages. The Guttenstein-type Tri- age isdocumentedbyammoniticfauna andbythe (“stinking”), frequentlywithdiaclases. Their Anisian crop out,blackishordark-grey, slightlybituminous of Cristianinanoldquarry, welllayered limestones North ofRâ Cristian – Anisian limestones(Guttensteintype). Stop 3.3: the PiscucuBraziFormation oftheCeahl of Bra worked outfromquarriesaround Teliu village(east is representedby truded inablacksilticsequence. The MiddleJurassic stones); asillofarfvedsonite graniteporphyryisin- shales dominatewithintercalationsofquartziticsand- Lithofacies Nappe. Above theLadinianlimestones of anE-WorientedanticlinebelongingtotheGetic are exposed inanoldquarry. They constitutethecore western foothillsofthePost Cristian (6kmtoward south-west)situatedinthe From Bra as doesthenorthslopeofDealulMelcilor. limestones. Kimmeridgian-Tithonian bythe ș ov –LadinianlimestonesinDealulMelcilor ș Ladinian organogenous massive limestones ov) andaremassive sandstonesintercalatedin

ș ov thefieldtrip proceedstothevillageof Tâmpa Hillconsistsoftheselimestones oftheLower Jurassicfollows (blacksiltic ș nov, atthesouthernmargin ofthevillage quartzitic sandstones ă varu Mts. massive Stramberg , whilethe ă u Nappe. Gresten 24-05-2004, 15:43:46

GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

Stop 3.4: sideritic limestones. In the middle part of the Gresten Râșnov – Upper Jurassic limestones. lithofacies, in the Holbav area, alkaline rocks (alkali- About 7 km south of the Cristian quarry, in the center basalts, trachytes, camptonites, bostonites) are inlay- of Râșnov, massive neritic Stramberg-type Kim- ered as lava-flows or sills. This volcano-sedimentary meridgian-Tithonian limestones crop out in a cliff- formation is a specific feature of the Holbav Gresten like hill. The specific feature of the Cetăţii Brook Lower Jurassic and is absent in the other zones where outcrop (at Râșnov) consists of a changed lithofacies the Gresten Lithofacies is known (Cristian, Brașov, of the lower part of the carbonate sequence (well- Săcele). layered limestones, probably Kimmeridgian-Lower Tithonian. Such situations are scarce, but emphasize Stop 3.8: that in some areas sedimentation starts with basinal Holbav Gneiss west of Holbav. lithofacies, synchronous with the massive neritic one, 150 -200 m downstream from the westernmost houses passing upwards to neritic, generalized lithofacies. of Holbav, large outcrops of the Holbav Gneisses may On the top of the limestone relief, in the XIVth century be examined. They consist of augengneisses with cen- , a peasant fortress was built, which is one of the sev- timetric pink or white augen of K-feldspar, interpreted eral defence fortresses built around Brașov. either as migmatites or as orthogneisses derived from From Râșnov the fieldtrip returns to Cristian and from porphyric granites. there proceeds west crossing the Bârsa Plain (which The Holbav Gneiss is overthrust above the Lower corresponds to the Bârsa Quaternary Depression) Jurassic. This overthrust coresponds to the frontal until Vulcan . part of the Supragetic nappes, the Șinca Nappe re- spectively. Northward the frontal overthrust of the Stop 3.5: Supragetic nappes can be followed, in outcrop, until Vulcan – Anisian / Spathian boundary. the Dealu Mare Fault (easternmost segment of the At the western margin of the village of Vulcan, 250 m South Transylvanian Fault) (Figure1). The Supragetic from the Vulcan-Holbav road, in a small old quarry, nappes correspond, in the Central East Carpathian limy shales and thin black limestones, weakly bitu- area (Crystalline-Mesozoic Zone) to the Subbucovin- minous crop out. With a thickness of 10-30 m, they ian and the Bucovinian nappes. develop at the base of the Guttenstein-type Anisian The fieldtrip returns to Vulcan and from there contin- limestones. From the stratigraphical point of view ues northwards to Codlea. The Măgura Codlei Scale they are situated at the boundary between the Middle is well expressed in the relief. It is constituted mostly Triassic (Anisian) and the Lower Triassic (Spathian). of Upper Jurassic massive neritic limestones (Stram- From Vulcan village the fieldtrip follows a local road berg-type), which preserve at their base Callovian - until Holbav village and west of it. Oxfordian radiolarites and Middle Jurassic calcareous sandstones. The Măgura Codlei Scale is thrust in front Stop 3.6: of the Subbucovinian (Șinca) Nappe. Dealul Merezi (Merezi Hill) – metamorphics of the From Codlea, where a medieval fortified church Voinești Formation. marks the center of the locality, the fieldtrip turns In several small outcrops, on the western slope of west, entering the Vlădeni Couloir. This is well Dealul Merezi in the eastern suburb of Holbav, expressed in the flat and lower relief. The southern feldspathic quartzites and retrogressed micaceous margin of the Vlădeni Couloir is represented by the paragneisses are exposed. They belong to the Voinești Dealu Mare Fault (see above). This fault is marked Formation of the Leaota Group. by a sharp morphology corresponding to the eleva- tion of the southern border of the Couloir, which is Stop 3.7: in fact a half-graben, tilted at its southern part. The Volume n° 1 - from PR01 to B15 n° 1 - from Volume Holbav – Lower Jurassic in Gresten Lithofacies. Vlădeni Couloir filling consists of Upper Cretaceous 130 m upstream on the Bisericii Brook, in Holbav, conglomerates and coarsegrained sandstones and of in several mining, the rocks which constitute the marls (Senonian), thin and discontinous developed Gresten lithofacies developed in the Holbav area may Eocene formations (sandstones and marls) and Oli- be examined: quartzitic sandstones, coarse-grained gocene-Lower Miocene dominantly marly lithofacies, sandstones with quartzitic grains and coal-bear- slighty bituminous. ing siltic matrix, coal-bearing clays or clayey silts, Near Perșani village the south-east border of the

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu ramic view ofthePer From Carpathian Bend Area. Panoramic viewoftheinnermostpart Stop 3.9: seismic lines. Depression clearlyfollowed inboreholesandonthe out. Itisageneralmarker ofthebasalsequence ries ontheslope,northofroad,Dej Tuff crops road whichisfollowed bythefieldtrip. Insomequar- Transylvanian Depressioniscrossedbythenational southern borderofthe Transylvanian Depression. Af- From Sibiuto Alba Iuliathefieldtrip runsalongthe Sibiu - Alba Iulia-Câmpeni the Louvre. oldest paintingexhibition, openedoneyearbefore in Constantinople. The showing anarchitecturesimilartothatofSaintSophia Cathedral XVI F Mare Fault iswellexpressed inrelief(seeabove). The northern limbofthe Vl cover oftheBucovinian Nappe.Itcorrespondstothe overlain bytheUpperCretaceouspost-tectogenetic sion ofthenappedevelops. The south-easternslopeis slope ofGârbova Mts.)thewholesedimentarysucces- Nappe cropout.Onthenorth-westernslope(left-hand of whichmetamorphicformationstheBucovinian large domalanticline(Gârbova Anticline) inthecore Subbucovinian Nappe.Onasmallareaat skyline, correspond-withasmallexception - tothe visible reliefofthePer north-eastern endoftheF the DealuMare(South Transilvanian) Fault andthe From inian Nappeispreserved. peak ontheskyline), atectonicoutlieroftheBucov- and Vârful luiPetru(thelattervisibleasthehighest preserved. Parts ofthedefenceworks oftheXV the town, wherethemedieval architecturewas well Evangelic Cathedralwas built intheoldestpartof Sibiu isalsoanimportantmedieval town. The matian and,mostly, Pannonian formations. Depression. Northward thehillsarebuilt upof Sar- Southward (left-hand) theF southernmost partofthe Transylvanian Depression. ă g ă th r centuriesarealsowellpreserved. The a Ș Ș ș ercaia villageitispossibletohave apano- ercaia toSibiuthefieldtrip runsacrossthe Mts.,withthebeautifulpanoramaoftheir was thefirst onebuilt in Transylvania, ș DAY 4 DAY 4 ani Mts.,the Vl ă Brukenthal Museum deni Depression. The Dealu ș ani Mts.correspondstoa ă g ă ă g ra ă ra ș Mts. The highest ș Mts.borderthe ă deni Couloir, Ș inca Nou Ortodox * isthe th - ă

Valley. ter crossing Alba Iulia,thefieldtrip entersthe Ampoi The outcropsoftheMete Trasc its prolongationeastoftheBradDepression,or (southern andeastern)units(Techer and sedimentaryrockswhichproceedfromtheinner klippen (“olistoliths”)beingrepresentedbyophiolitic is atypicalwildflyschformation,thesedimentary Nappe isrepresentedbythe across theFene After Badenian age. tion whichisofuppermostBurdigalian/lowermost quently they maybecorrelatedwiththeHidaForma- is olderthantheDej Tuff (Lower Badenian).Conse- formation molassic Mountains.This South Apuseni types, proceedingfromtheMioceneerosionof be examined. The pebblesandgrainsareofdifferent coarsegrained sandstonesofredorgrey colourmay Brook. Conglomerates,microconglomeratesand exposed in Depression, croppingoutinthe Alba Iuliaarea,are The oldestformationsbelongingtothe Transylvanian The Upper Aptian -AlbiansequenceoftheFene Ampoi Valley -theMete Stop 4.2: (Transylvanides). Ș Stop 4.1: Fene Stop 4.3: The roadcontinuesacrossthesameMete limestones. thonian and/orUrgonian (Barremian-Lower Aptian) klippen of:basalts,calc-alkalinerocks,Oxfordian, Ti- (turbiditic) ormassive silticmatrixandsedimentary et al.,1981). Upper Jurassicolistolithscanbeobserved (Bleahu enters the Valea luiPaul Formation in whichsome At Presaca Ampoiului, aftercrossingafault, theroad and slopes. exposures aresituatedontheleft(northern)affluents built upbytheFenesFormation, but thefavourable Poiana Ampoiului andPresaca Ampoiului, theareais of UpperJurassiclimestoneolistoliths.Between the landscapedominatedbycharacteristic“Klippen” Along theFene ard -Miocenemolasse ș ă Ș valley. Very low-grade Fene u Nappe). ard, alongthe Ampoi Valley thefieldtrip runs Ș ard, ontheright-handbankof Ampoi ș ș valley silticclay UnitoftheSouth Apuseni Mts. . ș ș Formation show alayered Formation Mete ș ș Formation chemoliticlime- ș beds ă . u-Drocea and ș Formation, . 28-05-2004, 19:19:48 . This ș

GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

stones, greywackes, spilites, are exposed; they are DAY 5 very slightly metamorphosed. This formation is Câmpeni - Petru Groza - Brad - Deva considered (Bleahu et al., 1981) volcano-sedimen- tary-olistostrome, with sequences of turbiditic rocks. Stop 5.1: The age of the Feneș Formation is probably Titho- Vadu Moţilor. Contact between Lupșa nian-Barremian. and Gârda Nappes. After Paleozoic marbles exploited in a quarry and Stop 4.4: a rather monotonous sequence of either sericitic Petringeni. Faţa Băii conglomerates and volcanites or chloritic schists, for several kilometers, at Vadu (Paleocene). Moţilor, south of the confluence with the Neagra val- The molasse deposits of the post-tectonic Paleo- ley, at the base of the Muncel Nappe, chlorite-sericite gene-Miocene Zlatna basin, transgressive on the schists with an intercalation of tuffogeneous amphi- Cretaceous Flysch are represented by the Faţa Băii bolites are exposed, dipping 35°SE. conglomeratic Formation. The polymictic conglom- North of the confluence, silvery-violaceous laminated erates admit intercalations of sandstones, red clays, conglomerates crop out with strongly flattened peb- as well as interlayered lavas and volcaniclastics of bles, the schistosity dipping southwards. Their age is rhyolitic and andesitic composition. The rhyolitic Upper Carboniferous-Lower Permian; the conglomer- flows, sometimes brecciated, consist of plagioclase, ates belong to the Finiș -Gârda Nappe, the basement sanidine, quartz and biotite. The andesites are am- of which consists of the Codru Granitoids, exposed phibole-and pyroxene-bearing. The thickness of the upstream (Bleahu et al., 1981). lava flows does not exceed 50 m. Paleocene age was Further on, the road runs across the Codru Granitoids confirmed radiometrically and biostratigraphically. and migmatites of the Gârda Nappe, as well as across Westwards the age of the sedimentary and volcanic violaceous quartzitic sandstones and conglomerates formations extends well into the Miocene (E. Roșu in belonging to the Bihor Unit, the basement of which Udubașa, 2001 ed.). consists of retrogressed chlorite-sericite schists At Zlatna, at the crossroad to Almăș, Senonian for- (Arada Series). The contact between the two units is mations are exposed in a small quarry, consisting of a vertical fault. sandstones, microconglomerates and conglomerates with pebbles of quartz and limestones. Stop 5.2: Upstream from Izvorul Ampoiului the valley crosses Albac Gorge. Skythian-Anisian boundary the tectonic contact between the Feneș Nappe and the in the Bihor Unit. Bucium Unit, the latter being represented by the Up- At the confluence with a small left-hand tributary per Albian Pârâul Izvorului Formation (coarse convo- decimetric beds of Skythian violaceous or white lute sandstones, marls and clays). quartzitic sandstones are conformably overlain by The road traverses the watershed between the Ampoi Anisian yellowish-white bedded dolomites. The and Arieș basins at Dealul Florii. abrupt contact suggests a break in sedimentation (Bleahu et al., 1981). Stop 4.5: Confluence Abrud valley - Cerbu valley. Stop 5.3: Soharu Formation (Upper Aptian-Lower Albian). Zugăi Gorge, Bihor Unit. Detrital formation An overturned Wildflysch sequence of the Bucium at the base of the Ladinian. Unit can be examined in a small quarry. The sequence After crossing for a longer distance massive, brittle consists of grey-greenish convolute shales alternating yellowish-white Anisian dolomites, a detritic forma- in the higher levels with calcarenites and calcirudites. tion is exposed along the road for about 100 m, its Volume n° 1 - from PR01 to B15 n° 1 - from Volume Conglomerates with calcareous cobbles and green sequence being as follows: dolomitic breccia with tuffaceous-clayey matrix are also exposed, as well as clasts of black dolomites; white limestone breccia greenish or violaceous siltites (S. Bordea, 1992). with rounded pebbles of Wetterstein limestones and of Anisian black limestones (regionally unknown in outcrops); violaceous argillaceous or marly shales, appearing yellow or grey when weathered, with inter- beds of violet quartzitic sandstones.

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu calcite mylonites(Bleahuetal.,1981). migmatites oftheGârdaNappearetransformedinto limestones overthrust byCodruGranitoidsand Some hundredsofmetersupriver, the Wetterstein senting akarstinfilling. limestone pebblesandthevioletclayspossiblyrepre- dence ofacontinentalenvironment deposition,the The detriticformationpresentedabove gives evi- white Wetterstein limestones. The topofthesequenceconsistsmassive greyish- Tatrides (Bleahuetal.,1981). and withtheMedódoly(Kopersady) brecciasof the glomerati diDossodeiGalli”oftheSouthern Alps transport andpresentastrikingsimilaritytothe“Con- believed tobeanalluvialdeposit,withoutfluvial and quartzitesincludedinashalymatrix. They are 20 cminlengthofgneisses,muscovite, schistsquartz taken byabrecciaconsistingoffragmentsreaching the placeofLaminatedConglomeratesbeing continues acrosstheformationsofGârdaNappe, the Anisian dolomitesoftheBihorUnit,road After crossingagain,duetotheGârdamajorfault, Permian oftheGârdaNappe. Gârda deSus-confluencewithIarbaRea.Lower Stop 5.5: 1995). the maindeformationwas flattening(Dimitrescu, was predominantlyanextensional one,but inplaces Measurement ofthepebbleshasshown thatthestrain glyphs) (Bleahuetal.,1981). interbeds ofredmicaceoussandstones(withhyero- green rhyoliticignimbritesandvioletshaleswith obseved. Upsequencefollows laminatedvioletor slaty matrix. An obliquefoliationmaysometimesbe sist offlattened,mainlyquartzpebblesinaviolaceous age ofwhichwas evidenced bypalynology. They con- glomerates, theUpperCarboniferous-Lower Permian term oftheGârdaNappe,namelyLaminatedCon- a half-window, theroadreachesfirst sedimentary atites andahorstexposing Wetterstein limestonesin After crossinglaminatedCodrugranitoidsandmigm- Permian oftheGârda Nappe Sc Stop 5.4: Confluence withtheBucini Stop 5.6: After crossingaspectaculargorge cutacrossasyn- overthrusting theGârdaNappe ă ri ș oara -Gârda.UpperCarboniferous-Lower ș valley. Arie . . ș eni Nappe From thefrontof Arie (Upper Carboniferous). Arie Stop 5.7: Poiana Nappemadeupofanarrow stripofmetacon- Biharia crystallineseries.Itoverlies horizontallythe the formationsofBihariaNappeconsisting The wholecrestoftheBihariaMassifisbuilt upof Arie Stop 5.8: ity S measurable foliationplanescorrespondtoaschistis- bedding isapproximatelyN45° W /12° SW. Directly developed; theattitudeofgraphicallydetermined of therocks,onplaneswhichnofoliationhas Conglomerates ofthe Arie by theelongationofpebblesinGreenschist The regional trendofthestretchinglineations,marked / 04°NW. cur locally. The intersectionlineationtrendsN67°W foliation smallfaultings ofthelithologichorizonsoc- ding; itsattitudehereisN70°W/45°SW. Along this Northern Apuseni (Dimitrescu, 1995). (Dimitrescu, Northern Apuseni ling thedirectionof Alpine tectonictransportinthe (Bleahu etal.,1981). of theirschistositybeingaboutEWwithsoutherndip litic schistsofLower Carboniferousage,theattitude and rhyolites,whilethelatterconsistsofgreenphyl- represented bylaminatedconglomerates,sandstones and the Arie with theBucini feldspathic sandstonesandshales,attheconfluence and sandstonesoverlying thePermianmicaceousor cline ofSkythian violaceousquartzconglomerates of thelithologicalhorizonsexpresses theS cropping outjustatthewater level. The alternation ish-green sandstoneandoverlie greenpelitic schists metaconglomerates admitanintercalationofgrey- quartz andwithgreyish-green quartziticmatrix;the strongly rolledpebbles,composedpredominantlyof ing ofweaklymetamorphosedconglomerateswith a subhorizontalexposure maybeobserved consist- about 10mlongontheleftsideof Arie At km40+350mofmainroadnr. 75,inanexposure NW.towardsand W Arie unit. The large outcropsreveal theschistosityof sively theLower Carboniferousgreenschistsofthis amined attheprevious stop,theroadcrossesexclu- ș 1 ș ș eni Formation showing various dips,generally (flow cleavage) obliquewithrespecttothebed- eni. Greenschist Formation eni. GeneralviewoftheBihariaMassif.

ș eni Nappesisexposed. The formeris ș valley thecontactbetweenGârda ș ș eni Nappe,isNW, signal- eni Nappeoverthrust ex- ș 0 bedding ul Mare, 24-05-2004, 15:43:53 GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

Figure 8 - General cross-section in the Bihor Mts (M.Bleahu in Ianovici et al., 1976) I Bihor Unit: SA, Arada Series; ws, Seisian; wc- an,Campilian-Anisian; ld,Ladinian; J1, 2, 3 , Jurassic; br, Barremian. II Arieș eni Nappe: P, Permian; T1,Werfenian; III Poiana Nappe: SP, Păiușeni Series; IV Biharia Nappe: SB, Biharia Series; SP, Păiușeni Series. V Muncel Nappe: SM, Muncel Series; g, granitoids. Southern Apusenides: b, ophiolites; br, Barremian; st-cp, Santonian, Campanian; ma, Maastrichtian.Post- tectogenetic formations: gd, granodiorites; a, andesites; gdp, granodiorite porphyry.

glomerates and sericite-phyllites (Upper Carbonifer- ous-Păiușeni Series). The Poiana Nappe overlies the Arieșeni Nappe, which covers the whole area lying at the foot of the Biharia Massif; this nappe consists of the Arieseni Greenschists Formation and the reddish- violet formations of the Upper Carboniferous-Lower and Middle Permian. In front of and under the Biharia (Cucurbăta) MicăPeak, a lower peak covered by wood, rises. It is the Stânișoara Peak, which consists of banatitic granodiorites piercing the whole pile of Permian formations. The intrusion determined a contact meta- morphism changing in large areas the red colour of the Permian into black (“Black Series”) (Bleahu et al., 1981). Stop 5.9: Arieșeni. Unconformity Upper/Lower Carboniferous. After leaving the centre of Arieșeni, at km 36 + 550 m, after the confluence with the Șteului valley, in a large exposure the unconformity between the Laminated Conglomerates (Carboniferous-Lower Permian) and the Arieșeni Greenschists (Lower Carboniferous) may be examined. In this exposure the pelitic greenschists are overlain by laminated conglomerates containing as pebbles weakly rolled quartz fragments included in a violaceous-silvery sericitic matrix; the conglomer- ates alternate with schistose quartzitic sandstones and argillaceous violet phyllites.

The attitude of the common schistosity S1 of both Volume n° 1 - from PR01 to B15 n° 1 - from Volume formations is N 40°W / 35°SW. The S0 bedding of the greenschists, graphically plotted according to a slight banding is N 40°E / 38°NW, the trend of the intersec- tion lineation being EW / 30°W. The attitude of the bedding of the laminated conglom- erates cannot be observed here. However 200 m up- river, this attitude put in evidence by pebble grading and by shaly interbeds is NS / 60°W (trend of inter-

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu the Arie been aplaneoneintheLaminatedConglomeratesof majority ofthepebblesshows ak~1,thestrainhaving that didnotaffect thelatter. OnFlinn’s diagram,the undergone anolderMidcarboniferoustectonicphase deformed (Es=0.55-1.22versus 0.55-0.80),having be concludedthattheformerweremoreintensely nated Conglomeratesinthe Arie Greenschist conglomerateswiththoseoftheLami- Comparing theEsparametersforpebblesof the intensityofdeformationbeingmedium. sional one,asmeasurementoftheirshapehasshown, The strainofthepebbleswas exclusively anexten- direction ofthe Alpine tectonictransport. Arie of thepebblesinLaminatedConglomerates of thestretchinglineationsmarked bytheelongation section lineation:N53°E/36°SW). The regional trend Urgonian limestones Piatra Muncelului.Lamprophyre dykes crossing Stop 5.11: andesite sill. be observed. The Permianispiercedbyabanatitic sandstones, bioglyphsofburrow -fillings typecan micaceous sandstonesandargillaceous shales.Inthe above theroad,Permianis represented byred At km32+120m,ontheleftslopeofvalley Formation. Banatiticsill. Bube Stop 5.10: cement. and ofigneousrocks,enclosedinacalcareous-gritty ments ofwhitelimestones(recrystallizedasmarbles) breccia about1mthick,composedofangularfrag- 1 and3m;theeasternonepresentsatitscontacta stones. The thicknessofthedykes rangesbetween dykes strikingaboutNSareintrudedintothelime- At km21+50m,threealmostvertical lamprophyre Unit arecontinuouslyexposed. Urgonian facies belongingtothelowermost Bihor and thenwhitemassive limestonesofBarremianin into hornfelses(“BlackSeries”),afault istraversed across Lower Jurassicdetritalformationschanged After anumberofroadwindingsandhair-pin bends formations. ing reddishPermianandquartziticLower Triassic basin andenterstheCri Mountains, theroadleaves the Arie After reachingthemainwatershed ofthe Apuseni ș eni Nappeisalsonorth-western,confirming the ș ti Hill.Permian Vermicular ș eni Nappe(Dimitrescu,1995). . ș ul Negru basin,intersect- ș eni Nappe,itmay ș hydrographic Depression withoutcropsofPliocene. age canbenoticed.FinallytheroadreachesBeiu lowed bydolomitesandlimestonesofMiddle Triassic Arie 1981). presence ofpyroxenes asphenocrysts(Bleahuetal., having anintergranular texture. Itisworth notingthe ing ofbasicplagioclaseandaugite,theground-mass The lamprophyrescorrespondtoodinites,consist- mation oftheB Past thetown ofB observed (“BlackSeries”). contact withblackargillites andquartzitesmaybe micaceous sandstones,whileinthehangingwall, the able. The footwall consistsofblackishvermicular N 20°E/40°SE;two mainjointsystemsareobserv- foliation; theattitudeoflayeringisapproximately hues atplaces. The rock presentsafeeblypronounced to thermalmetamorphismwithvery slightviolaceous rhyolitic bodyisexposed. Itscolourislightgrey, due rului, oppositethefirst houses,ontherightslope,a Stop 5.13: Arie Stop 5.12: On enteringtheoldmininglocalityofB numerous In thelastoutcropsoflimestones(km20+60m) Nappe /Urm the latter(N.StaninBorco matrix. Characteristic“fiamme” areoftennoticedin as leafybiotite,includedinagreenish-grey schistose crystals about1-3mminsizeareconspicuous,aswell the Va Ignimbritic rhyolitesareexposed about400mwestof Va Stop 5.14: B small depth(Bleahuetal.,1981). thermal actionofthebanatiticbodyintrudedhereata by blackcolouredones(“BlackSeries”)duetothe rocks. Redcolouredrocksaregraduallyreplaced Nappe consistingmainlyofthePermianviolaceous Further on,theroadleadsagain intothe Arie carenites, allofthemassignedtotheLower Jurassic. shales, yellowish quartzsandstonesandgreyish cal- Urm cabin, theroadcrossesfromBihorUnitinto odonts ă ș i ţ c a Bihorului.Rhyolites intheblackPermian ș ă ș ă eni Nappealongafault. Skythian quartzitesfol- eni -B t Nappe. The latterconsistsofslightmicaceous ș u. Permian ignimbriticrhyolites aretobeobserved; then,attheroadsurveyor’s c ă u railway station. White feldsparandquartz Coral ă ă i ţ t Nappe/BihorUnit. ă a road. Contacts Arie tracesaswellremnantsof trânescu Nappeappearcontactingthe ă i ţ a, ontheright-handside,for- ș etal.,1980). ș eni . ă i ţ 24-05-2004, 15:43:58 a Biho- Megal- ș eni ș .

GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

Figure 9 - Simplifi ed map of Vâlcan-Parâng Mts. Stop 5.15: (T.Berza and V.Iancu, 1994). Dealul Mare. Metaconglomerates of the complex beginning at Săliștioara the road crosses Păiușeni Series. ophiolitic rocks belonging to the Techerău Nappe, The road crosses the divide between the hydrographic porphyritic basaltic lavas with augite phenocrysts, basins of the Black and the White Criș; at this point, andesites with hornblende as well as porphyroclastics the metaconglomerates of the Poiana Nappe are ex- (aglomerates and tuffs) are conspicuous (Savu et al., posed. 1986). Measurements on their pebbles indicated an exten- Some “Klippen” of Upper Jurassic and Urgonian sional strain for the whole Poiana Nappe, in one point limestones can be noticed. only the strain is a flattening one. Succeeding the ophiolitic complex, after an EW strik- The road continues across the Miocene post-tectonic ing fault, the Căbești Formation (Barremian-Lower basin. Aptian) is exposed, namely black gritty shales with Between Brad and Vălișoara upriver the Luncoiu val- intercalations of siliceous sandstones; they belong to a ley on both sides of the main road, Mesozoic island- particular unit, the Căbești Unit (Bleahu et al., 1981). arc (U3-K1) andesitic-basaltic volcanics (basalts and andesites are associated with gabbros, but also with Stop 5.16: dacites, rhyolites as well as with orthophyres and oli- Fornădia. Mesocretaceous unconformity. gophyres as pyroclastics) as well as the Miocene mo- A small hill marks the unconformity between the lasse deposits represented mainly by the red “Almasu Căbești Formation, represented by strongly disturbed Mare gravels” (Badenian) are exposed; the latter be- quartzitic sandstones and clayey shales and the gently long to the Brad-Săcărâmb sedimentary basin where

dipping Fornădia Beds (Vraconian-Cenomanian). PR01 to B15 n° 1 - from Volume the Neogene volcanics are widely developed. The latter start with quartzitic micro-conglomerates In the Dealul Mare col the characteristic landscape of and calclithites. The coarse bedding becomes thinner volcanic peaks is to be seen. (15-50 cm) towards the top of the formation. In thin At Vălișoara, the Upper Jurassic andesitic and ba- slides Paraphillum primaevum is frequent. saltic flows and pyroclastics are overlain by Upper After another EW oriented fault, the road reaches Jurassic calcareous olistoliths and by Aptian Wildfly- the area of the Bejan Unit, in which the Bejan For- sch formations. mation is characteristic. This formation consists of Downstream the Vălișoara valley, after the island-arc

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu tury onitstop. volcanic neck)with aruinedfortressoftheXV built upbyaNeogene amphiboleandesite(+biotite The fieldtrip reaches Deva, atown dominatedbyahill micropaleontological data(Bleahuetal.,1981). marls areofConiacian-Santonianage,constrainedby ined. The conglomerates,massive sandstonesand fault, outcropsoftheDeva Formation canbeexam- Along theMure an olistostrome. clastics andepiclasticssandstones,representing limestones, interbeddedwithbasalticflows, pyro- basalts, Upper Triassic andUpperJurassicmicritic black argillaceous shaleswitholistolithsofJurassic middle oftheXV plants but alsoforthebeautifulcastle,built inthe famous inthecountrynotonlyforitsmetallurgical From Deva, thefieldtrip reachesHunedoara,atown Deva - Tg.Jiu - Turnu Severin basin. From Hunedoara,theroadcrossesNeogeneStrei lurgical industry. were minedrepresentingthebasisforlocalmetal- Underlying thedolomites,low-grade irondeposits belonging totheSuprageticUnitsofPoianaRusc a cliff ofLower Carboniferouscrystallinedolomites 10,Alpine overthrust; 11,pre-Alpineoverthrust P deposits; 2,Lotrurocks; 3,UpperCretaceousFlysch withLupenilimestoneklippen;4,Schela Formation;5,Lainici- Figure 10-Schematic cross-sectionalongtheJiuGorges(Berza,Dr ă iu ș rocks; 6,Dr ș ă valley, againafteranEWtrending g th ș century. Itsfoundationsrest on an amphibolites;7, DAY 6 Ș u ș i ţ a Pluton;8,unconformity; 9,”decollement”stratigraphicboundary; th cen- ă . On thesouthernslopeof Vâlcan Mountains,the metapelitic andmetapsammiticrocksofGrestentype. immediately beforethemotel.Itconsistsofblack Formation isexposed alongaforestroad beginning m leadstotheGambrinusMotel. The LiassicSchela (km 125onnationalroad66),asmallafter150 At theconfluenceofEasternand Western Jiu Gambrinus Motel.LiassicSchelaFormation. Stop 6.2: sandstones. tanian conglomeratesandcoal-bearingChattian The Petro minerals aresubstitutedbysericiteandchlorite. times affected byretrogression,whichtheprimary with muscovite, biotiteandgarnet. They aresome- consisting ofmicaschistsandmicaceousparagneisses Before enteringPetro al., 1994). micritic Urgonian limestones(T. Berza,in:Berzaet Callovian) andUpperJurassic-Aptianpelletal limestones withsiliceousdeposits(Lower-Middle and bioclasticlimestonesarefollowed bybioclastic er Cretaceouscover. Aalenian-Bathonian sandstones Lotru Group crosses theGetic(Austrian)Napperepresentedby Between Crivadia andB and Mesozoiccover. Crivadia Bridge.GeticNappe:Lotrubasement Stop 6.1: ă g ă ș nescu,in Berzaetal.,1994).1,Tertiary ani Tertiary basinfollows, withred Aqui- basement andtheLower Jurassic-Low- ș ani, theLotruGroupisexposed, ă ni ţ a, nationalroad66 24-05-2004, 15:44:03

GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

same formation bears fossil flora. garnet and muscovite are frequent. Scarce layers of The dominant attitude of the schistosity in the black mica-gneisses occur in the amphibolites (T. Berza, in: phyllites is N 75°E / 40°SW; it represents an axial Berza et al., 1994). plane foliation of concentric decimetric and metric folds trending N 22°E / 30°SW (B 1), accompanied Stop 6.4: by a faint crenulation lineation with the same attitude. Cârligul (Cornul) Caprei bridge, km 115.500. Pre Younger chevron folds trend N 50°W / 75°SW (B 2). - Alpine tectonic contact between two distinct base- Along B 1, conspicuous boudins of quartzose mate- ments (Lainici - Păiuș and Drăgșan) of the Lainici rial can be observed, due to contrast in competence; Nappe. they indicate a tectonic transport top-to-NE. A parallel The last outcrops of the Drăgșan Group are fine- to system of short centimetric quartz veins lead to the large-grained massive garnet amphibolites (metagab- same conclusion. bros), preceded by serpentinites (metaperidotites). Downriver to 100 m north of the bridge, the retro- Stop 6.3: gression is limited to fracture zones, frequently with Km 118.500 on national road 66. Amphibolitic quartz veins. Near the bridge, contrasting mechanical Formation of the Drăgșan Group. properties of carbonates and silicates and pervasive A typical leptyno-amphibolitic formation is exposed, deformation produced black (amphibolite) or white with an alternation of millimetric to centimetric (leucogranite) boudins in the marbles. black and white layers dipping 45°SE. All propor- On the following hundreds of meters downriver to tions between 100% hornblende and amphibole-free km 114.500, the road exposes para-amphibolites, oligoclase + quartz layers can be found. Biotite, mica-gneisses, graphitic metapelites and silicate Volume n° 1 - from PR01 to B15 n° 1 - from Volume

Figure 11 - Tectonic sketch-map of the south-western part of the South Carpathians. (Codarcea et al.,1968).

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu Lainici -P Nappe). Onthenext 500moftheroad,rocks southwards bytheLainici-P further west. The Schela Formation isoverthrust The Liassicageiswelldocumentedbyplantremains chloritoid slates(famous occurrenceofchloritoid). conglomerates andsmallerdebrisofpyrophyllite- hand tributary, withhugeblocksofsandstones and mostly Quaternarydepositsatthemouthofaleft- At theRafaila Cross,theleftbankofJiushows and SchelaFormation. Gorges arecarved intotheLainici-P Downriver tokm106(LainiciMonastery),theJiu Lainici Nappe. to theLainici-P al., (1983)ascribethiscarbonatic-graphiticsequence nolescu (1937),Pavelescu etal.,(1964)andBerza foliation andEW-trendinghorizontallineation.Ma- the entiresequenceisstronglysheared,withasteep marbles withubiquitousleucograniteinjections; Km 105.Rafaila-Lainici-P Stop 6.6: 1994). epidote, stilpnomelane)(T. Berza,in:Berzaetal., greenschist retrogression(albite,chlorite,tremolite, cordierite, hornblende),stronglyoverprinted bylater in places(andesine,garnet,sillimanite,andalusite, T-low Pmetamorphism(Precambrian)arepreserved sequence. Relictmineralassemblagesofanearlyhigh zation. Several porphyriticdykes areemplacedinthis foliation andretrogradegreenschistfacies recrystalli- mylonitic, withapervasive north-dippingmylonitic are widespread. The generalaspectoftherocksis es). Leucograniticinjectionsandvarious migmatites various quartzites,biotitegneissesandmica-gneiss- exposing itsQuartziticFormation (analternanceof Km 111.Lainici-P Stop 6.5: Berza etal.,1994). consider itaspartoftheDr chlorite-stilpnomelane-epidote mylonites. transformed intoquartz-albite-Kfeldspar-muscovite- 103.700, therocksbeingfoliatedandaltered, The first outcropsof diorites show apervasive Alpine mylonitization. tal EW-trending lineation.Dikes ofporphyriticmicro- may reach2cminlengthandshow astrong horizon- alternate withmicagneisses±sillimanite. The latter gioclase ±biotitemuscovite ±garnetdiopside ă iu ș Groupareexposed: quartzites±pla- ă iu ș ă Group,whileSavu etal.,(1984) iu Ș ș Group inthe u

ș i ţ ă a granitoidsbegin atkm g ă ă ș iu an Group(T. Berza,in: iu ș ș Formation (Lainici gneisses ă iu ș Group, in theXIV The churchofthe al., 1994). ates andarkosic sandstones(T. Berza,in:Berzaet The Mesozoiccover consistsofLiassic conglomer- tion ofchlorite,prehnite,epidote. Static retrogrademineralalterationsincludeforma- interstitial quartz,apatite. The fabric ismassive. brown hornblende,biotite,plagioclase(An40-50), are exposed, upriver consistingofclinopyroxene, Associated inthesamemagmaticsuitemeladiorites metric vein ofapliticrockscrossesthegranitoids. vicinity ofthehydroelectricadit. A subhorizontal cm. Equigranulargranodioritesalsocropoutinthe lengths of10cm;theplagioclasesdonotexceed 1 and accessories. The K-feldsparmegacrysts reach sist ofmicrocline,plagioclase(An30),quartz,biotite The porphyriticcoarse-grained Tismana granitescon- Tismana monastery. Tismana granite. Stop 6.8: mont. across theNeogeneformationsofGeticPied- After leaving theJiuGorges thefieldtrip proceeds of theSouthCarpathians(50kminlength). texture ismoreorlessmassive. Itisthelongestpluton biotite- hornblendegranodioritesandtonalites. The The Km 97. Stop 6.7: The deformationalhistoryincludestectonicshearing and argillaceous shales. crystalline schists,whilethematrixconsistsofsiltites include Mesozoicrocks,basalts,serpentinitesand a block-in-a-shearedmatrixtexture. The olistoliths of ahighlybroken sequenceofturbiditesshowing a UpperCretaceous Wildflysch formation,consisting uppermost termoftheLower Danubian cover, namely Between Brebinaand Titerle overlying theDanubian. de Aram Brebina valley atBratilovu, km48alongtheBaia Stop 6.9: much laterperiod. tion processes(T. Berza,in:Berzaetal.,1994). the Kfeldsparmegacrysts resistbettertothedeforma- and transformedintosericite-chlorite“orthoschists”; fected byaHercynian schistosity. They arelaminated Down totheRuncbrook,granitoidshave beenaf- Ș u ș Ș i ţ ă u a plutonconsistsofbiotitegranitesand -B th ș century;itsotherbuildings datefroma i ţ a granitoids. ă ile Herculane road. GeticNappe Tismana monastery

ș ti, theroadcrosses

was built 24-05-2004, 15:44:12 GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

Figure 12, 13 - Geological map and cross section-Danube Valley between Gura Văii and Orșova (V.Iancu, Fl.Marinescu, S.Năstăseanu, M.Conovici in Pop et al.,1997).

and gravitational mass transport. Shear-sense indica- Stop 6.10: tors suggest dextral shearing, connected to a major Obârșia Cloșani. Km 52-56. Severin Nappe. The EW -trending dextral strike-slip fault (8-10 km of Severin Nappe in this area is represented by the horizontal displacement). (A. Seghedi, in Berza et Obârșia Complex, a melange formation with ophio- al., 1994). lites and siliceous pelagic deposits (radiolarian cherts) Volume n° 1 - from PR01 to B15 n° 1 - from Volume In Bratilovu, the mylonitic rocks with western dips of assigned to the Upper Jurassic-Lower Cretaceous. the Lotru Group belonging to the Getic Nappe crop The ophiolitic rocks are basalts (in places with pil- out. low texture), dolerites, harzburgitic ultramafites and Across the villages of Mărășesti and Stănești, the minor gabbros, pervasively sheared and disrupted. road exposes outcrops of crystalline schists of the Geochemical features suggest MORB -tholeiites. The Getic Bahna outlier. rocks preserve fresh pyroxenes. Along the Brebina valley, spotted basalts show low-temperature meta-

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu foliation andaS Group, withsmallbodiesofsheareddiatexitic gran- Metamorphites ofthepreviously examined Lotru underlying Severin Nappe Lower Cretaceous turbidites(SinaiaBeds)ofthe the soleof viaduct (1.3kmwestwards). Tectonic contactat generations, S marble lenses. The outcropsdisplayuptothreefold amphibolites, quartz-feldspargneissesandscarce ceous paragneissesandmicaschistsassociatedwith Lotru Groupconsistsofmetaterrigeneousmica- Nappe, onwhichtheIronGateDamisbuilt. The The roadcrossestheIronGateoutlierofGetic Getic Nappe:LotruGroup. Pre-Alpine polymetamorphic basementofthe Scarpia (Padina Mic ruins canalsobevisited. A.D.), onepillarofwhichcanstillbeseen.Medieval emplacement of Trajan’s bridgeover theDanube(105 Drobeta -Turnu Severin. This town was built atthe The roadcontinuesacrossNeogeneformationstill Seghedi, inBerzaetal.,1994). rocks aretraversed byepidote-quartz-albiteveins (A. along thewesternborderofnappe.Shearedgreen lying bandedmylonitesdevelop onbasaltprotoliths S-C fabrics, withapenetrative scaly-cleavage. Flat elements oftheophiolitesconsistslickensides and epidote, albite,calciteandzeolites. The structural ondary mineralsoftheshearedrocksincludechlorite, morphism inprehnite-pumpellyitefacies. Othersec- Sl Stop 7.2: 3.5 kmwestofGura V Stop 7.1: Turnu Severin - Timi Pop etal.,1997). Danube southwards intoSerbia(Sip)(V. Iancu,in: The IronGatesoutlieroftheGeticNappecrosses ations liebetweenENEandESE. NE-SW attitude,whilethemineral(stretching)line- sure type. The dominantS2foliationhasageneral muscovite associationM2ofintermediatelow-pres- phism M1areoverprinted byasillimanite +biotite kyanite) characterizingafirst barrovian metamor- Relict mineralassemblages(biotite,garnet,staurolite, intersection lineations. ă tinicu Mare viaduct(km354)andOreva 1 layering,S

Getic Nappe(Bahnaoutlier)with 3 crenulationcleavage, mineraland DAY 7 ș ă oara ) andUngureanu viaducts. ă ii, km352,betweenthe 2 . dominanattransposition 1997). Seghedi,V. Iancu,in:Berzaetal.,1994;Pop formations, several metersaway fromthecontact(A. a steeplydippingshearbandfoliationoccursinboth phites reappearinthecoreofatightsynformalfold; viaduct, stronglyshearedandbrecciatedmetamor- across sedimentarydeposits.300meastoftheOreva build upthetopofhills,whileroadiscut where themetamorphicrocksofLotruGroup tion. The tectoniccontactcanbefollowed uphill, metamorphic rocksshow pervasive brittledeforma- the right-handbankofSl Getic NappeandtheSinaiaBedsareexposed on The relationshipsbetweentheLotruGroupof angle normalfaults. fanning infoldhinges. Younger structures arehigh beds. Sandstonebedsmayshow fracturecleavages Slaty cleavages areseldomvisibleinthepeliticinter- axial planessteeplydippingEor W arecommon. hinges. Various typesofkink-andchevron-folds with they areoftenpreserved asisolateddismemberedfold folds arestronglydisruptedbynormalfoldingand by steeplydippingnormalfolds(B2). The recumbent to isoclinalrecumbentfolds(B1)stronglyrefolded The structuralstyleoftheSinaiaBedsconsiststight nian- Lower Valanginian, accordingto age ofthesequenceisascribedtoUpper Titho- na isoftenpreserved insiltstonesandmudstones. The limestones formthininterbeds. Danubian tonic contactbetweentheSeverin Nappeandthe parison withtheCerna-Co to theUpperJurassic-Lower Cretaceous, bycom- places apseudobrecciaaspect. Their ageisascribed crossed bynumerouscalciteveinlets, exhibiting in are massive grey limestonesstronglyjointedand The oldestsedimentarydepositsexposed eastwards Group isexposed. At theconfluencewith Vodi vicinity oftheSl thicker sandstonebedsupto40-50cmoccurinthe The SinaiaBedsincludemostlydistalturbidites; naia Bedsareexposed. of theLotruGroup,whileonitswesternendSi- the viaduct,outcropconsistsofcrystallineschists large scaleopenantiformalfold.Ontheeasternendof ites, overlie theSinaiaBeds,lyingincoreofa Km 357, Vodi Stop 7.3: represent ahugeolistolithembeddedintoparatypi-

Domain. ţ a viaduct- Vârciorova viaduct. Tec- ă ˘tinicu Mareviaduct.Grey pelagic

ș u ș tea zone. These deposits ă tinic valley, wherethe Chondritid ţ a valley, theLotru Calpionellids ichnofau- 24-05-2004, 15:44:20 . GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

Figure 14 - Geological sketch of the Bârzava Valley (Moniom-Bocșa) (Iancu, Năstăseanu in Năstăseanu et al., 1981). 1, Quaternary; 2, Neogene; 3, Banatitic magmatites.Locva Unit:4, Upper Carboniferous and Lower Cretaceous; 5, Lower Carboniferous(Cârșie Formation); 6, Devonian, volcano-sedimentary formation:a, metapelites; b, metatuffs and metatuffites; 7, metamorphoseded igneous rocks; 8, Ordovician(?), Tâlva Mare Quartzites;Bocșa Unit: 9, Upper Carboniferous and Middle Jurassic-Lower Cretaceous; 10, Precambrian-Lower Cambrian,Bocșiţa-Drimoxa Formation; 11, Precambrian,Tâlva Drenii Formation. Reșiţa Nappe:12, Upper Carboniferous.

cal Wildflysch Lower Senonian Formation consisting road, the lower part of the nappe contained small of red and green marls, black shales and of a sequence exposures of ophiolites. known as Vârciorova Sandstone. The latter consists of A comparable succesion was described by Grubic´ massive calcareous sandstones, grading up to strati- (1992) in the Dzevrin hill in Serbia, south of the fied sandstones, with interbeds of conglomerates and Danube. microconglomerates, including unsorted lithoclasts of A vertical fault separates the Danubian from the gneisses, quartzites, micaschists and limestones. Bahna outlier of the Getic Nappe, the latter being Trace fossils occur within the pelitic terms, mainly prolonged south of the Danube into Serbia (Tekija). Chondritids. The major constituents of the sandstones Orșova is built upon a Miocene basin (V. Iancu, A. are plagioclase and quartz; detrital micas are musco- Seghedi, in: Pop et al., 1997). vite and partly chloritised biotite. The carbonate ce- ment is micritic to largely recrystallized. Stop 7.4: Walking eastwards the overlying Severin Nappe Bela Reka valley. Mehadia. Lower Lias. (known in Serbia as the Kosovica Nappe) consists At the southern entrance into Mehadia, on the left- of Azuga Beds = Kasajna Beds in Serbia (red and hand bank of the Bela Reka river, the Lower Lias is green shales, displaying sometimes a phyllitic aspect; exposed. It overlies transgressively the Permian, rep- PR01 to B15 n° 1 - from Volume red radiolaritic cherts, manganese cherts, sandy cal- resented by red conglomerates with argillitic matrix; carenites and sandstones), their age being ascribed to in the dominating Străjiuţul hill, Permian eruptive the Upper Jurassic, and by the previously examined rocks crop out. The Lower Lias consists of an alter- Sinaia Beds. nance of conglomerate banks, quartzitic breccia and The overthrust plane of the Severin nappe is marked sandstones, grey or blackish, with black gritty shales by mylonites. Before the construction of the new as intercalations (Codarcea et al., 1961).

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu et al.,1961). of theRe Leaving Moniom,the(Westphalian C.)DomanBeds Nappe andtheSuprageticMoniomNappe. and schists(S mandine, kyanite andstaurolitebearingmicagneisses thin PiatraScris quent. The topoftheformationisrepresentedby (Savu, 1970;S amphibole-gneisses, marblesandcalc-silicaterocks gneisses, quartz-feldsparamphibolitesand nodular sillimanite-bearingbiotitegneisses,pearl- The lowermost termoftheLotruSeriesconsists Armeni into theUpperLias,with paxillosus, Pholadomyasturi strained byfaunas with characteristic fortheGrestenfacies. Their ageiscon- gritty intercalationsoftheMiddleLiascropout, Upstream theBelaRekavalley, blackshaleswith Bela Rekavalley. MiddleLias. Stop 7.5: tonic line. The uppermost termoftheRe rocks oftheMoniomNappealongOravi Hill, wherethey areoverthrust bythemetamorphic Moniom. RelationsbetweentheGeticRe Stop 7.7: Timi Stop 7.6: represented bytheCarboniferousCâr character.Oravi The evidence itshighintensity(Rf>2,5)andplane of thepebbles. Analysis ofthefinite strainputin by theN30-40°E/10-30°NEtrendingelongations westwards. The stretchinglineationsarematerialized phyllites. Intheformer, thepebblesdecreaseinsize It consistsofmetaconglomerates,metasandstonesand The describedformationsexhibit subhorizontalini- intrusions. metatuffs alsobeingpresent,as well asmetagabbroic intercalations ofcarbonaticandgraphiticrocks,acid metatuffs, metatuffites and metaaglomerates,with quartz, sericite,calcite)representingmyloniticbasic sists ofchlorite-epidote-actinolite-albiteschists(± Valea SatuluiFormation oftheMoniomNappecon- Westwards alongtheBârzava river, theDevonian Dimitrescu, 2000). a simpleshearintheCarboniferousformations(M. Supragetic Nappedextral transcurrentfault, inducing ș valley between Teregova andSadova Veche. ș Formation oftheLotruSeries. ș i ţ a NappewillbecrosseduptotheCâr ă b ă ă b ă u, 1994). ă amphibolitelevel, overlain byal- u, 1994).Pegmatite veins arefre- ţ a tectoniclinerepresentspost- Ostrea cymbium Posidonia . Upwards they grade

bronni ș ie Formation. ș , i ţ

Belemnites a Nappeis (Codarcea ţ a tec- ș ș i ţ ie a Iancu, in:N tial stratification surfaces (S tion oftheBoc Nappe isoverthrust bytheBoc tunnel, the Valea SatuluiFormation oftheMoniom Along theBârzava valley, above theCol Moniom Nappe. Col Stop 7.8: Miss Delia-Georgeta Dumitra Dr. MihaelaDimitrescu,MissElenaNegulescu and The authorswould like toexpress theirgratitudeto Acknowledgements Bârzava valley -Boc Stop 7.9: the Le The Valea SatuluiFormation was parallelizedwith cleavages. (V. Iancu). with theLocva “Series”exposed alongtheDanube The Boc to theMiddle-UpperJurassic-Lower Cretaceous. represented bymarbles,theageofwhichisascribed The Mesozoiccover ofthebasement formations is 1981). orthoamphibolites (V. Iancu,in:N alternate withraremicroclineaugengneissesand with awestward dip. Westwards, theplagiogneisses tion folds,thelimbsofwhicharecutbyaS2foliation forest chalet. The rocksexhibit intrafolialtransposi- porphyroblasts); itcropsoutabout200mwestofthe otite andgarnetrelics(mainlyenclosedinplagioclase of muscovite-chlorite-albite plagiogneisses,withbi- - Senonian. are 87m.y. (B1)and80-81m.y. (B2)thatis,intra The respective K- Ar agesofthesuccesive intrusions N and hornblende(Russo-S plagioclase (20-35% An), microcline,quartz,biotite and granodioritesMediumUnitconsistsofzoned blende andbiotitephenocrysts. The monzogranites magmatic stage(Western Unit)containslarge horn- rocks. The micromonzodiorite porphyryoftheearly xenoliths ofbothcrystallineschistsanderuptive porphyry ispenetratedbyagranodiorite,carrying is exposed. A first intrusionofmicromonzodiorite and theintrudedSuprageticaugen-andplagiogneisses The contactzonebetweentheBoc ă st ţ an tunnel.Boc ă seanu etal.,1981). ș covi ș i ţ ţ ă a-Drimoxa Formation was parallelized a “Series”exposed alongtheDanube(V. st ș ă a Nappe. The latterformationconsists seanu etal.,1981). ș a Nappeoverthrust ontothe ș a Nou ă ndulescu etal.,1975;in 0 ) andalmostvertical S ș (GeologicalInstitute ă ș i . Banatiticmassif. ţ a-Drimoxa Forma- ș a banatiticpluton ă st ă seanu etal., ţ an railway 24-05-2004, 15:44:27 2

GEOLOGICAL STRUCTURE OF THE ROMANIAN CARPATHIANS B12

of Romania) for carefully editing the manuscript and ans (Mehedinţi-Banat Area). CBGA XII CONGR., B figures of this guide. 2, 100 p. Bucharest. Thanks are due to the Geological Institute of Roma- nia, Bucharest, for the facilities generously put at our Nedelcu, L., Hârtopanu, P., Szakacs, Al., Moga, C., disposal. Podașcă, I. IV Nat. Symp. Mineralogy (Iași), Field The authors acknowledge with thanks a Grant from Trip. Rom. Journ. Mineralogy, 78, suppl. 2, 40 p. the Romanian Academy (Nr. 94 / 2003) which ena- Bucharest. bled them to carry out the elaboration of this guide. Pop, Gr., Mărunţiu, M., Iancu, V., Seghedi, A., Berza, References cited T. (1997). Geology of the South Carpathians in the I Field-Guidebooks Danube Gorges (Romanian Bank). 28 p. Bucharest. Balintoni, I., Berza, T., Hann, H., Iancu,V., Kräutner, H.,Udubașa, G. (1989). Precambrian Metamorphics Săndulescu, M., Ștefănescu, M., Butac, A., Pătruţ, in the South Carpathians. 71 p. Bucharest. I., Zaharescu, P. (1981 a). Genetical and Structural Relations between Flysch and Molasse (The East Berza, T., Iancu, V., Seghedi, A., Nicolae, I., Balin- Carpathians Model). CBGA XII CONGR., A 5, 96 toni, I.,Ciulavu, D., Bertotti, G. (1994). ALCAPA II. p. Bucharest. Excursion to South Carpathians, Apuseni Mountains and Transylvania Basin: Description of stops. Rom. Săndulescu, M., Kräutner, H., Balintoni, I., Russo- Journ.Tect.Reg.Geol.75, suppl. 2, 105-149. Bucha- Săndulescu, D., Micu, M. (1981 b). The Structure of rest. the East Carpathians (Moldavia-Maramureș Area). CBGA XII CONGR., B 1, 92 p. Bucharest. Bleahu, M., Lupu, M., Patrulius, D., Bordea, S., Ștefan, A., Panin, S. (1981). The Structure of the Săndulescu, M., Borcoș, M., Bordea, S., Dimitrescu, Apuseni Mountains. CBGA XII CONGR., B3, 108 R., Ștefan, A. (1992). Les Carpates.Tectonique de p. Bucharest. Compression-Subduction-Magmatisme Connexe. Réun.extraord. SGF en Roumanie. Guide, 43 p. Bu- Borcoș, M., Peltz, S., Stan, N., Berbeleac, I. (1980). carest. Neogene and Permian volcanism in the Apuseni Mountains and the East Carpathians.136 p. Inst. Udubașa, G. (ed.) (2001). Geodynamics and Ore Geol., București. Deposit Evolution of the Alpine-Balkan-Carpathian- Dinaride Province. Rom. Journ. Min. Dep. 79, suppl. Cioflica, G., Savu, H., Nicolae, I., Lupu, M., Vlad, S. 2, 6-13. Bucharest. (1981). Alpine Ophiolitic Complexes in South Car- pathians and South Apuseni Mountains. CBGA XII II Geological maps of the Geological Institute of CONGR., A3, 80 p. Bucharest. Romania

Codarcea, Al., Bercia, I., Boldur, C., Constantinof, D., East Carpathians Maier, O., Marinescu, Fl., Mercus, D., Năstăseanu, S. 1:50000 (1968). Geological structure of the Southwestern Car- Bercia, I., Bercia , E., Săndulescu, M., Szasz, L. pathians. XXIII Intern. Geol. Congr. (Prague), Exc. (1975). Sheet Vatra Dornei. 49 A C, 50 p. Bucharest. Kräutner, H., Kräutner, Fl., Săndulescu, M., Bercia, Kräutner, H., Năstăseanu, S., Berza, T., Stănoiu, I., I., Bercia, E., Alexandrescu, Gr., Ștefănescu, M., Ion, Volume n° 1 - from PR01 to B15 n° 1 - from Volume Iancu, V. (1981). Metamorphosed Palaeozoic in the J. (1975). Sheet Pojorâta. South Carpathians and its relations with the pre-Pal- aeozoic Basement. CBGA XII CONGR., A 1, 116 p. Mureșan, M., Peltz, S., Seghedi, I., Szakacs, Al., Ban- Bucharest. drabur, T., Kräutner, H., Săndulescu, M., Mureșan, G., Peltz, M., Kräutner, Fl. (1986). Sheet Voșlăbeni. Năstăseanu, S., Bercia, I., Iancu, V., Vlad, S., Hârto- Săndulescu, M., Bandrabur, T., Mureșan, M., Vasi- panu, I. (1981). The Structure of the South Carpathi- lescu, Al. (1971). Sheet Miercurea Ciuc.

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu S Dimian, M.(1968).SheetR Joja, T., Alexandrescu, Gr., Bercia,I.,Mutihac, V., (1968). Sheet Topli Sheet Odorhei. M., Arghir-Dr Alexandrescu, Gr., Mure 1:200000 stantin, P. (1987).SheetCâmpulungMoldovenesc. S Sheet D Sheet Bra S I., S Berza, T., Seghedi, A., Pop,Gr., Szasz,L.,Hârtopanu, V., St South Carpathians Mantea, G.,Bo Borco 1:50000 Apuseni Mountains S (1973). SheetSânmartin. S Clo Bercia, I.,E.,N 1:50000 Bordea, S., Bordea, S.andBorco Lupu, M.,Kräutner, H., T¸icleanu, M.,Bo Avram Iancu. Dimitrescu, R.,Bleahu,M.,Lupu,M.(1977).Sheet Câmpeni. Dimitrescu, R.,Bordea,J.,S.(1974).Sheet Biharia. Bordea, J.,Bleahu,M.,Costea,C.(1989).Sheet Bordea, S.,Dimitrescu,R.,Mantea,G., Abrud. itrescu, R.(1967).Sheet Turda. Lupu, M.,Borco 1:200000 (1982). SheetDeva. Bandrabur, T., Kräutner, Fl.,Horvath, A., Nicolae,I. ă ă ă ă ă ndulescu, M., Vasilescu,Mure M., Popescu, A., ndulescu, Al., ndulescu, M.,Micu, Alexandrescu, Gr., Con- ndulescu, M.,Patrulius, D., ndulescu, M.,Mure ndulescu, M.,Bandrabur, T,Vasilescu, Al., Peltz,S. ș ani. ă ă b ș noiu, I.,Hârtopanu,I.(1977).SheetObâr , M.,Berbeleac,I.,Bordea,S.,J., ă ă u, G.,Moisescu, V., Popescu,Gh.(1986). muc. ș ov. Ș tefan, A., Borco tefan, A., ă ș gulescu, A., Bandrabur,T.(1968). gulescu, A., tinescu, S.(1981).SheetZlatna. ș , M.,Dimian,Lupu,D.,Dim- ţ a. ș , M.(1972).SheetBrad. ș ă an, M.,Mure st ă ș seanu, S.,Berza, T., Iancu, an, G.,S ă d ă Ș u tef ș ţ , M.(1979).Sheet i. ă nescu, M.(1972). ș ă an, G.(1975). ndulescu, M. ș Ș tinescu, S., tefan, A., ș an, ș ia Savu, H.,Pavelescu, M.,Stancu,J.,Lupu,D.(1968). Severin. Savu, H.,Ghenea,C., A. (1966).Sheet Turnu Re N (1968). SheetBaiade Aram N 1:200000 N., Schuster, A. (1972).SheetZ S St Savu, H.,Stan,N., N panu, I.(1975).Sheet Tismana. Pop, Gr., Berza, T., Marinescu,Fl.,St S N M., S topanu, P., Marinescu,Fl.,Dinic Hârtopanu, I.,Stan,N.,Iancu,V., N A., Rogge-T¸ Ghenea, C.,Russo-S Sheet Lupeni. dentale. chaines alpinessituéesautourdelaMerNoireocci- S Carpathians General Structure and Evolution oftheRomanian III References cited Sheet Or Geology. S Tehnic S and Tertiary Rom.Carpath.),Inst.Geol.Geofiz., European Micropal.Coll.” (Micropal. Guide.Mesoz. Antonescu, E.(1975).L’Anisien deCristian. Geological Structure oftheEastCarpathians 75, suppl.2,Bucharest. ă ă ă ă ă ă ă ă ă ndulescu, M.,Popescu,G.,S ndulescu, D.(1985).SheetRe ndulescu, M.(1980). Analyse géotectoniquedes ndulescu, M.(1994).Overview onRoumanian ndulescu, M.(1984).GeotectonicaRomâniei.Ed. ș st st st noiu, I.(1984).SheetSchela. i ţ ă ă ă a. ă seanu, S.,Stancu,J.,Ilie,S.(1968).Sheet seanu, S.,Bercia,I.,Bercia,E.,Bi seanu, S.,Iancu, V., Savu, H.,Russo- b ă ă , Bucure An. Inst. ăș In u, G.(1987).SheetOr tie. : “ ALCAPA II“, ă ranu, E.(1984).SheetBerzovia. ș

Geol. Geofiz ti. ă ndulescu, D.,Iancu, V., Ghenea, ă st ă seanu ,S.,Marinescu,Fl., ă . Rom. J. Tect. Reg . LVI, Bucure ă ș ă ndulescu, J.,Mih ova. ă ș rne i , I.,Bercia, Tatu, ţ ă a. st ș ă ti. ă noiu, I.,Hârto- seanu, S.,Hâr- ţ ș oianu, C. ti. In 24-05-2004, 15:44:30 . : “14 Geol ă il ă ., th ,

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București. Paleozoic Geodynamic domains and their alpidic evo- lution in the Tethys “. IGCP Project No. 276 (Papan- Antonescu, E., Ion, J., Alexandrescu, Gr. (1978). ikolaou , coord.). Ann. Géol. des Pays Helléniques, Nouvelles données biostratigraphiques concernant 37, p. 336 - 352, Athènes. les Schistes Noirs et les Argiles Bariolés des Car- pates Orientales. D. S. Inst. Geol. Geofiz. LIV / 4, Mutihac, V. and Bratu, E. (1965). Fazies und Alter București. der Ablagerungen aus dem nordlichen abschnitt des Ostkarpatischen Ausserrandmulde., Carp. Balk. Geol. Antonescu, E. and Săndulescu, M. (1985). Quelques Assoc., VII Congr., Sofia. données palynologiques concernant la Nappe du Flysch Courbicortical de la vallée du Trotuș (Car- Mutihac, V. and Ionesi, L. (1974). Geologia României. pathes Orientales). D. S. Inst. Geol. Geofiz. LXIX / Ed. Tehnică, București. 4, București. Săndulescu, M. (1973). Contribuţii la cunoașterea Antonescu, E., Bratu, E., Ion, J., Ionescu, A., Micu, structurii geologice a Sinclinalului Rarău (french ex- M., Săndulescu, M. (1989). Biostratigraphy of the tend. abstr. ). D. S. Inst. Geol. LIX / 5, București. Paleogene Flysch formations of the Roumanian Car- pathians. 14 th Congr. CBGA, Extended Abstr., Sofia. Săndulescu, M. (1975). Studiul geologic al părţii cen- Balintoni, I. (1985). Contributions to the knowledge trale și nordice a Sinclinalului Hăghimaș (french ex- of the metamorphic history of the Argestru Series tend. abstr.). An. Inst. Geol. Geofiz. XLV, Bucureși. rocks in the Puciosu brook (East Carpathians). D. S. Inst. Geol. 69 / 1, 247 - 255, București. Săndulescu, M. (1976). Contribuţii asupra strati- grafiei și a poziţiei tectonice a seriilor mesozoice din Balintoni, I. (1997). Geotectonica terenurilor meta- bazinul superior al văii Moldova (Carpaţii Orientali), morfice din România. Ed. Carpatica, 1-176, Cluj. (french extend. abstr. ), D. S. Inst. Geol. Geofiz. LXII Ion - Săndulescu, J. (1975). Microbiostratigraphie, / 5, București. associations et zones ? foraminifères du Crétacé du flysch externe des Carpathes Orientales (Roumanie). Săndulescu, M. (1988). Cainozoic Geotectonic His- Rev. Espan. Micropaleont., Madrid. tory of the Carpathians. Bull. AAPG 45, Tulsa.

Ion, J. (1978). Microbiostratigraphie des dépôts Săndulescu, M. (1990). Le flysch crétacé de la zone crétacés de la Nappe du Flysch Courbicortical. Ann. du Mont Ceahlău et du bassin du Bicaz. D. S. Inst. Soc. Géol. Pol. XLVIII / 2, Krakow. Geol. Geofiz. 74 / 4, București. Ionesi, L. (1971). Flișul Paleogen din bazinul văii Moldova (French abstr.). Ed. Acad. R. S. România, Săndulescu, M. and Russo - Săndulescu, D. (1981). București. The Ophiolites from the Rarău and Hăghimaș Syn- clines - Their Structural Position, Age and Geotec- Kräutner, H. G. (1980). Lithostratigraphic Correlation tonic Evolution. D. S. Inst. Geol. Geofiz. LXVI / 5, of Precambrian in the Romanian Carpathians. An. București. Inst. Geol. Geofiz. LVII, București. Săndulescu, M. and Micu, M. (1988). Oligocene Kräutner, H. G. (1983). Geotraverse H in the East Paleogeographiy of the East Carpathians. In: “Oli- Carpathians; Stratigraphic correlation forms. In: gocene from Transylvanian Basin”, Ed. Univ. Cluj. “Newsletter “ IGCP Project no. 5 (F. P. Sassi, F. Volume n° 1 - from PR01 to B15 n° 1 - from Volume Szederkenyi, Eds.), Padova. Săndulescu, M., Tomescu, C., Iva, M. (1976). Date noi cu privire la microfaciesurile și biostratigrafia Kräutner, H. G. (1988). East Carpathians. In: “Pre- formaţiunilor mezozoice din Sinclinalul Rarău cambrian in younger fold belts” (V. Zoubek, Ed.), pp. (french extend. abstr.). D. S. Inst. Geol. Geofiz. LXII 625 - 638. Wiley, Chichester. / 4, București.

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu pozitelor jurasice Econ. - Breaza(frenchextend. abstr.). Turcule Rev cal-tectonic context (EasternCarpathians,Romania). Cioflica, G.,Lupu,M.,Nicolae,I., Vlad, 44/10, 938-955, Winston &Son. “Al.I.Cuza” Ia iferi. Rezumatultezeidedoctorat,1-26,Universitatea Principi, G.,Saccani,E.(2002). Bortolotti, V., Marroni,M.,Nicolae,I.,Pandolfi, L., S est. paléogéographiques. ic evolution oftheH Stan, N., Tiepac, I.,Usc 76, Bucharest. Folded Area oftheEastCarpathians. (1995). Lower -MiddleMioceneFormations inthe CBGA, 12 the EastCarpathians(Moldavia -Maramure - S sice sicretacicedinparteavestic Bordea, S.(1992).Stratigrafia depozitelorneojura- S. Inst.Geol.Geof Apuseni Mountainsandassociatedmetallogenesis (1988). Evolution ofbanatiticmagmatisminthe Avram, S.,Laz Apuseni Mountains Prisaca. Contributions àla connaissancedel’âgeduGrès S Univ. Cluj. pathians. of theEoceneFlyschFormations oftheEastCar- S Geophys., Bucharest. A La NappedeMaclaentrelesvallées de T S ă ă ă ă ţ a (Montsde Tarc ndulescu, M.,M ndulescu, M., Antonescu, E.,Bratu,E.(1992). ndulescu, Micu,M.,Bratu,E.(1987).Stratigraphy ndulescu, M., Antonescu, E.,Platon,E.(1993). ă . ndulescu, D.,Micu,M.(1981). The Structureof Roum. Géol Ser. J,10,Bucure ţ Rom. J. Tect. Reg. Geol , I.(1971).Cercet In th : “Eocenefrom Transylvanian Basin”,Ed. Congr., GuidetoExcurs.,B1,Inst.Geol. ș i. ă . 44,31-50,Bucarest. r, C.,Berbeleac,I.,Uduba . 72-73/2,115-213.Bucure ș i eocretacicedincuveta Rar ă ă Rev. Roum.Géologie ă ghima u) -Corrélationsrégionales et run ă ș tescu, A. (2000).Petrogenet- ti. ţ eanu, M.,Popescu,Gh. ă ș ri geologiceasuprade-

granitoids ingeochemi- . 74,Bucharest. Inst. Geol.,St. Tehn. ă Intern.Geol. Review aMun Rom. J. Stratigr ţ 37,Bucar- ilor Metal- Ș ă . (1980). ș ș rcu Area). ti. ș a, G. ţ a et . D. ă u .

matism andmetallogenesis. Alpine ophiolitesofRomania:Tectonic setting,mag- 77. Bucure Petrology, geochemistryandoriginofmafic ophiolitic Savu, H.,Udrescu,C.,Neac from within the Apuseni Mountains,Romania:Evidence (1994). Variscan vs Alpine tectonothermalevolution Dallmeyer, R.,Neubauer, F., Pan 56,79-95. Bucure South and alkalinevolcanics. lites fromRomaniaandtheirassociatedcalc-alkaline Savu, H.(1980).Genesisofthe Alpine cycle ophio- and geochemicalevidence Ianovici, V.,Borco Romania). in theFene L, Sartori,F. (2002).Deformationandmetamorphism Ellero, A., Leoni,l.,Marroni,M.,Nicolae,I.,Pandolfi, St. cerc. geologie 40 metaconglomeratelor paleozoicedinBihoruldeSud Dimitrescu, M.(1995). Varia 75, suppl.2(ALCAPA II),65-76.Bucharest. Ianovici, V.,Giu Apuseni. Ed. Academiei, 1-632.Bucure Dimitrescu, R.,Savu, H.(1976).GeologiaMun rol Apuseni Mountains(Romania). associated toMiddleJurassicophiolitesintheSouth geochemistry oftheLateJurassiccalc-alkalineseries Nicolae, I.andSaccani,E.(2003).Petrology (Romania). Apuseni Mountainsandtheirgeologicimplications Ar agesofsomeophioliticrocksfromtheSouthern Nicolae, I.,Soroiu,M.,Bonhomme,M.(1992).K- 744. Bucure omagmatic settingoftheJurassicophiolitesfrom Saccani, E.,Nicolae,I., Tassinari, R.(2001).Tecton- geologic Lupu, M.,Bleahu,Savu, H.(1969)..Evolu . SMPM83,81-96. 40

Ar/ Apuseni Mountains(Romania):Petrological ă aMun 39 ș C. R.Géoscience Geol. Alpine ti. ș ș Ar mineralages ti. Nappe(southern Apuseni Mountains, ș ș ţ c ti. ilor Metaliferi.Ed. Academiei, 1- ă ș , D.,Ghi , 3-18.Bucure , M.,Patrulius, D.,Lupu,M., An. Inst.Geol.Geof 68,77-83.Grenoble. .Ofioliti ș 334,437-354.Paris. . Rom.J. Tect. Reg. Geol u, V., Stoian,M.(1986). ţ ulescu, T.,Borco An. Inst.Geol.Geof Swiss. Bull.Min.Pet- ţ ia formeigale 26/1,9-22. ș ti. ă , D.,Fritz,H. ș ti. . 56,55- 24-05-2004, 15:44:34 ș , M., ţ ţ ilor ilor ţ ia . . .

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rocks within the Obârșia Cloșani-Baia de Aramă re- J. (1998). Shoshonitic liquid line of descent from di- gion (Mehedinţi Plateau). D .S. Inst.Geol.Geof. 70- orite to granite:the Late Precambrian post-collisional 71/1, 183-20. București. Tismana pluton (South Carpathians, Romania). Lithos 45, 281-303. Elsevier. South Carpathians Antonescu, E. (1973). Asociaţii palinologice caracter- Grünenfelder, M., Popescu, G., Soroiu, M., Arsenes- istice unor formaţiuni cretacice din Munţii Metaliferi. cu, V., Berza, T. (1983). K-Ar dating of metamorphic D. S. Inst. geol. LIX / 4, 115-169. București. and associated rocks in the Central South Carpathi- ans. An. Inst. Geol. Geof. 61, 31-38. București Berza, T. and Seghedi, A. (1983). The crystalline basement of the Danubian Units in the Central South Iancu, V. (1982). Lower Supragetic nappes of the Ba- Carpathians: Constitution and metamorphic history. nat, Moniom-Dognecea zone. D. S. Inst. Geol. Geof. An. Inst. Geol. Geof. 61, 15-22. București. 69/5, 31-36. București.

Berza, T. and Iancu, V. (1994). Variscan events in the Iancu, V. (1986). Unités structurales supragétiques et basement of the Danubian nappes. Rom. J. Tect . Reg. infragétiques de la partie ouest des Carpates Méridi- Geol. 75, suppl. 2, ALCAPA II, 93-103. Bucharest. onales. D. S. Inst. Geol. Geof. 70-71/5, 109-127. București. Berza, T., Balintoni, I., Iancu, V., Seghedi, A., Hann, H. (1994). South Carpathians. Rom. J. Tect. Reg. Iancu, V. and Mărunţiu, M. (1994). Pre-Alpine litho- Geol. 75, suppl. 2, 37-49. Bucharest. tectonic units and related shear zones in the basement of the Getic-Supragetic nappes (South Carpathians). Berza, T., Constantinescu, E., Vlad, Ș. (1998).Upper Rom. J. Tect. & Reg. Geol. 75, suppl. 2 (ALCAPA II), Cretaceous magmatic series and associated miner- 87-92. Bucharest. alization in the Carpathian-Balkan fold belt. Journ. of Resource Geol. 48/4, 291-306. Tokyo. Kräutner, H., Berza, T., Dimitrescu, R. (1988) .South Carpathians. In: “Precambrian in younger fold belts” Berza, T., Kräutner, H., Dimitrescu, R. (1983). Nappe (V. Zoubek, Ed.), pp.639-664. Wiley, Chichester. structurein the danubian Window of the Central South Carpathians. An. Inst. Geol. Geof. 60, 31-39. Kräutner, H. and Krstic´, B. (2002). Alpine and pre- București. Alpine structural units within the Southern Carpathi- ans and the Eastern Balkanides. 27th Congr. CBGA, Codarcea, Al. (1940). Vues nouvelles sur la tectonique 1-8. Bratislava. du Banat méridional et du Plateau de Mehedinţi. An. Inst. Geol. 20, 1-74. București. Krstic´, B. and Karamata, S. (1992). Terranes of the Eastern Serbian Carpatho-Balkanides. C. R. D. S. Dallmeyer, R., Neubauer, F., Mocanu, V., Fritz, H. Soc. Serbe Géol., livre jubil. (1891-1991), 57-74. (1994). 40Ar/39Ar mineral age controls for the pre- Beograd. Alpine and Alpine tectonic evolution of nappe com- plexes in the Southern Carpathians. Rom. J. Tect. Reg. Liégeois, J., Berza, T., Tatu, M., Duchesne, J. (1996). Geol. 75, suppl. 2 (ALCAPA II ), 77-86. Bucharest. The Neoproterozoic Pan-African basement from the Alpine Lower Danubian nappe system (South Car- Volume n° 1 - from PR01 to B15 n° 1 - from Volume Dimitrescu, M. (200). Histoire déformationelle des pathians, Romania). Prec. Res. 80, 281-301. Elsevier. métamorphites carpatiques: Monts du T¸arcu et Col- Manolescu, G. (1937). Etude géologique et lines de Bocșa. An. Inst. Geol. Rom. 71, 105-106. pétrographique dans les Munţii Vulcan (Carpates București. Méridionales, Roumanie). An. Inst. Geol. 18, 79-112. București. Dimitrijevic´, M. (1997). Geology of Yugoslavia. Barex,1-188. Beograd. Pantic´, N. (1963). Fitostratigrafia devonovah I ka- mennougolnah otlojenii Karpato-Balkan (Vostocinaia Duchesne, J., Berza, T., Liégeois, J., Vander Auwera Serbia). CBGA, Congr. V (1961), Com. St. III / 2,

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Volume n° 1 - from PR01 to B15 B12 - B12 Leader: M.Sandulescu leul JiuluiîntreBumbe 107-115. Bucure (1964). Cercet Pavelescu, L.,Pavelescu, M.,Bercia,I.,E. (1986). Significance ofK-Arradiometricagesob- Russo-S sif. (1978). PetrologicalstudyoftheBoc Russo-S 50 /1,43-60.Bucure D. S.Inst.Geol.Geof ă ă ndulescu, D., Vâjdea, E., T ndulescu, D.,Berza, T., Bratosin,I.,Ianc,R. ă ri petrografice ș ti. ș ti. ș ti . 64/1,105-172.Bucure ș i Iscroni ș i structuraleîndefi- . D.S.Inst.Geol ș a banatiticmas- ă n ă sescu, A. ș ti. . Savu, H.(1970). Stratigrafia Inst. Geol.Geof tained inthebanatiticplutonicareaofBanat. morfism dinprovincia metamorfic Bucure din Mun 76, 119-128.Bucharest. early historyoftheGeticcrystalline. phic correlations:atentative way ofexploring the S ă b ă u, G.(1994).Lithostratigraphicandmetamor- ș ti. ţ ii Semenic . 70-71/1,405-417.Bucure . An. Inst. Geol Inst. . An. ș i izogradeledemeta- ă . 38,223-311. prebaikalian Rom. J. Petrol ș ti. 24-05-2004, 15:44:37 D. S. ă .

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