
ANDREJ SMUC 
JCRASSIC AND CRETACEOUS STRATIGRAPHY AND SEf)fMENTARY EVOLUTION OF THEJULIAN ALPS, NW SLOVENIA 


CIP - Kataložni zapis o publikaciji Narodna in univerzitetna knjižnica, Ljubljana 
551.762/.763(234.323.6)(0.034.2) 551.3.051(234.323.6)"615.2/.3"(0.034.2) 
ŠMUC, Andrej 
        Jurassic and cretaceous stratigraphy and sedimentary evolution of the Julian Alps, NW Slovenia [Elektronski vir] / Andrej Šmuc. - El. knjiga. - Ljubljana : Založba ZRC, ZRC SAZU, 2013 
ISBN 978-961-254-514-7 (pdf ) 
269353728 
JURASSIC AND CRETACEOUS 
STRATIGRAPHY AND 
SEDIMENTARY EVOLUTION 
OF THEJULIAN ALPS,
NWSLOVENlA 

v

ANDREJSMUC 
LJUBLJANA 2005 

CONTENTS 

Abstract.............................................................................................................................................................. 7 
Izvlecek .............................................................................................................................................................. 9 

1 	Introduction ................................................................................................................................................ I I 

1. 1 	Geological setting................................................................................................................................... II 

1.2 	Previous research ................................................................................................................................... 15 

I. Airns of vol urn e ....................................................................................................................................... 16 

1.4 	Definition ofpaleog-eog-raphic units ..................................................................................................... 16 

1. 4. 1 	Julian Carbonate Platform ................................................................................................................ 16 

1.4. 2 	Julian High ......................................................................................................................................... 17 

1. 4. Siovenian Basin: Tolmin Trough and Bovec Trough .......................... : ........................................... 17 
1..f) Methods of investigation ........................................................................................................................ 17 

2 	Geological maps of key-areas .................................................................................................................... 19 

2. 	I Geological map of the Triglav Lakes Valley ......................................................................................... 19 

2. 2 	Geological map of the Mt. Mangart Saddle.......................................................................................... 

3 	Stratigraphy................................................................................................................................................. 29 
I Jurassic formations ................................................................................................................................. 34 

1. 	1 Julian Carbonate Platform ................................................................................................................ 34 
Triglav Lakes Valley, Ravni and Luznica Lake .................................................. ............................ 35 
Mt. Mangart Saddle: Travnik structural unit........................................................................................ 36 
Mt. Mangart Saddle: Mangart structural unit....................................................................................... 37 

3. I. 2 	Julian High ......................................................................................................................................... 3H 
Prehodavci Formation ..................................................................................................................... ....... 3H 

LOWER MEMBER .................................................................................................................................... 40 
MIl)[)LE MEMBER ................................................................................................................................... 43 
IJpPI':R MEMIIER ..................................................................................................................................... 44 

3. 1. 3 Bovec Trough ..................................................................................................................................... 47 
Sedlo Formation ..................................................................................................................... ............... 47 
Skrile Formation ............................................. ....................................................................................... 51 
Travnik Formation ..... ........................................................................................................................... 52 
MEMBER 1 ............................................................................................................................................. 54 

MEMIIER 2 ............................................................................................................................................. 57 
MEMBER 3 ............................................................................................................................................. 5H 
MEMBER 4 ............................................................................................................................................. 60 

3. 2 	Cretaceous formations ........................................................................................................................... 62 

3. 2. 	1 Biancone limestone ........................................................................................................................... 62 

3.2.2 	Scaglia variegata ................................................................................................................................. 63 

3. 2. 	3 Scaglia rossa ........................................................................................................................................ 64 

3. 3 	Neptunian dykes ..................................................................................................................................... 66 

3. 3. 1 	Mangart structural unit ..................................................................................................................... 66 

3. 3. 2 	Ravni Laz ............................................................................................................................................ 69 

3. 3. 3 	Luznica Lake ...................................................................................................................................... 70 

3. 3. 4 Triglav Lakes Valley ........................................................................................................................... 70 

4 Jurassic to Cretaceous sedimentary and paleogeographic evolution of the Julian Alps ........................ 73 

4. 1 	Hettangian to Pliensbachian: Shallow-water sedimentation on the Julian Carbonate Platform ...... 73 
4.2 	Pliensbachian: Demise of theJulian Carbonate Platform and formation of the Bovee Troughand the Julian High................................................................................................................................ 73 
4. 3 	Late Pliensbachian to Toarcian: Sedimentation in the Bovee Trough............................................... 75 

4. 4 	Bajocian to Early Tithonian: Rapid Bajocian subsidence and sedimentation in the Bovee Trough and on theJulian High ................................................................................................. 79 
4. 5 	Late Tithonian to Early Aptian: Pelagic sedimentation of the Biancone limestone.......................... 82 

4. 6 Albian to Early Campanian: Deeper-water sedimentation of the Scaglia variegata and Scaglia rossa ............................................................................................................................................ 82 
I 

5 Correlation with neighboring areas ........................................................................................................... 85 

5. 1 	Correlation of the Bovee Trough with the Tolmin and Belluno basins in the Jurassic..................... 85 

5. 1. 	1 Correlation with the Tolmin Trough ............................................................................................... 85 

5. 1. 2 Correlation with the Belluno Basin .................................................................................................. 86 

5. 2 	Correlation of the Julian High with the Trento Plateau in the Jurassic ............................................. 86 

5. 3 	Correlation of Cretaceous deeper-water deposits with the Tolmin and Belluno basins and the Trento Plateau.......................................................................................................................... 87 
6 Conclusions ................................................................................................................................................. 89 

7 Acknowledgments....................................................................................................................................... 91 

8 References ................................................................................................................................................... 93 

Abstract 

The northwestern part of Slovenia includes the Julian Alps, which structurally belong to the Julian Nappe that forms the eastern continuation of the Southern Alps. What now form theJulian Alps were in theJurassic part of the southern Tethyan passivecontinental margin and at that time experiencedextensional faulting and differential subsidence related to rifting, whilst during the Cretaceous the area underwent the onset of a compressional regime.
The main purpose ofthis research is to present a detailed sedimentologic and biostratigraphic studyof the Jurassic and Cretaceous successions of the Julian Alps. Fourteen selected sections exposingLower Jurassic to Upper Cretaceous deposits are presented in detail. The Mt. Mangart area and the Triglav Lakes Valley are of key importance of this research. Other investigated regions include Cisti Vrh, Vas na Skali, Ravni Laz, and Luznica Lake. Eight lithostratigraphic units were described; four of them were formally described. 
Geological maps ofthe Triglav Lakes Valley and Mt. Mangart areas were made on a scale of I: 10 000 as well. The Triglav Lakes Valley area is composed of the Krn Nappe, overthrust by the Zlatna Nappe. The area is additionally disrupted by a large strike-slipfault forming a negative flower structure. Mappingthe Mt. Mangart area revealed a complex tectonic structure composed of the Mangart structural unit and the Travnik structural unit that are internallythrusted, folded and disrupted by faults. The Mangart structural unit is thus divided into the Mali Vrh, Rdeca Skala, Drn, and Mangart peak subunits. 
Three typical successions indicating three different paleogeographic domains are distinguished,and are as follows: 
The most complete succession is exposed in the Travnik structural unit. It starts with lower Lower Jurassic platform overlain by Pliensbachian deeper-shelf Iimestime of the Sedlo Formation, followed by the Toarcian Skrile Formation (blackshales with intercalated siliceous limestone). A stratigraphic gap, comprising at least the late Toarcian and Aalenian, separates the Skrile Formation from the overlying lower/middle to lower Tithonian Travnik Formation (cherts, siliceous limestone and carbonate gravity-flow deposits).The succession ends with the Biancone-type pelagiclimestone ofearly Cretaceous age. Paleogeographically the basinalJurassic deposits correspond to the Bovec Trough.
The succession in the Triglav Lakes Valleyconsists of Pliensbachian platform limestone overlain by the Bajocian to lower Tithonian Prehodavci Formation (condensed' limestone of Ammonitico Rosso type). The succession ends with a lower Cretaceous Biancone-type limestone. The Prehodavci Formation was also studied in Ravni Laz, Luznica Lake, C':isti Vrh, and at Vas na Skali. It is the most common formation of theJulian High.
The most reduced succession is characterized by numerous polyphaseJurassic neptunian dykes cut into the lower Lower Jurassic platform limestone. These deposits are unconformably overlain by the middle Cretaceous Scaglia variegata or Senonian Scaglia rossa formations. The succession is exposedin the Mangart structural unit. Neptunian dykesformed at the margins of theJulian High.
The main sedimentary evolutionary phases during the Jurassic and Cretaceous are: 1) During the early Early Jurassic, the Julian Carbonate Platform was active. 2) Due to extension and accelerated subsidence in the Pliensbachian, theJulian Carbonate Platform was dissected, forming two different paleogeographical domains: a deeper basin named the Bovec Trough and a pelagic plateau named the Julian High. Distal-shelf limestones of the Sedlo Formation were formed in the Bovec Trough, while blocks of the central part of the Julian High were probably emergent. In the marginal parts of the Julian High, neptunian dykes were formed at that time. 3) The latest Pliensbachian lowstand is represented by a Fe-Mn hardground on the top of the Sedlo Formation. 4) Black shales in the lower partof the Skrile Formation in the Bovec Trough were deposited during early Toarcian Oceanic Anoxic Event. The Skrile Formation records a Toarcian transgressive/regressive cycle. 5) A second pulse of accelerated subsidence in the Bajocian caused addi

Ahslmrl 
tional subsidence ofthe investigated area. The Bovec Trough at that time became part of a deeper basin recording the sedimentation ofcherts and siliceous limestones with radiolarians, and started to receive resedimented carbonates from the adjacent Dinaric Carbonate Platform. All the areas corresponding to the Julian High at that time were drowned and were characterized by condensed sedimentation of the Prehodavci Formation. 0) Breccias in the lower part of Member 3 of the Travnik Formation that represent the most proximal facies association of the formation in the basin and a Fe-Mn horizon on the plateau record an upper Bathonian lowstand. 7) A Kimmeridgian tectonic phase is marked by numerous neptunian dykes cut into the Prehodavci Formation and a level of breccias in the basin. R)At the early/late Tithonian boundary the siliceous pelagic sedimentation and Ammonitico Rosso type sedimentation was replaced by the carbonate background sedimentation of the Biancone limestone. This facies change is regional and synchronous throughout all the western Tethys. At that time Jurassic topography was predominantly flat. 9) A tectonic phase in the Albian caused renewed 
reorganization ofthe area and enabled the sedimentation ofthe Scaglia variegata formation. 10) After a tectonic pulse in the Late Cretaceous the depositionof the Scaglia rossa began.
The succession of the Bovec Trough is correlative with successions of the Tolmin and Belluno basins. The successions are generally similar, however some differences do exist, because the Tolmin and Belluno basins were already deep-water basins during the early part of the Early Jurassic whereas the area of the later Bovec Trough was a carbonate platform (the Julian Carbonate Platform) that was drowned no earlier than the Plienshachian. Furthermore, in the Middle and Late Jurassic, the Bovec Trough was located closer to the Dinaric Carbonate Platform than the Tolmin and Belluno hasins, as evidenced by the relatively late initial subsidence, conspicuous hiatuses and obvious sediment bypassin the Bovec Trough. The condensed successions of the Julian High are correlative with those of the Trento Plateau. They are the most similar to certain parts of the Trento Plateau, where the middle memher of the Ammonitico Rosso (RAM) did not develop. 


Izvlecek 

Preiskano obmocje se nahaja v Julijskih Alpah, ki so del strukturne enote J lIznih Alp ali natancnejepokrova. PaleogeografSkoje
Alp v juri pripadalo juznemu pasivnemukontinentalnemll robu Tetide inje bilo zaradi riftinga podvrzeno ekstenziji ter razkosano na bloke z razlicno hitrostjo V kredi paje obmocje v kompresivnem rezimu. 
Namen tega delaje sedimentoloska in biostratigrafska studijajurskih in krednih kamnin v J ulijskih Alpah. V ta narnen sem na obmocju Julijskih Alpdetajlno preiskal 14 izbranih profilov, v katerih iz
spodnjejurske do zgornjekredne kamnine. Obmocji Mangartskega sedla in Doline Triglavskihjezer predstavljata kljucni obmocji za razumevanjegeoloskega zahodnih Julijskih Alp vjuri in krecli. Kot dodatna obmocja sem prouCiI tudijllrskokredne profile v okolici (:istega vrha, Vasi na Skali, ter profila Ravni Laz inJezero v Luznici. 
Za obmocji Mangartskega sedla in Doline Triglavskih jezer scm izdelal tudi detajlni geoloskikarti v merilu I: 10000. Obmocje Doline Triglavskihjezer pripada Krnskemu pokrovu, na katerega jenarinjen Slatenski pokrovo Te starejse strukture so nato presekane z mocnim desnozmicnim preiomom.Obmocje Mangartskega sedla je strukturno zelo zapleteno zgrajeno. V splosnem ga gradita dve vecji enoti: Mangartska in Travniska strukturna enota. Mangartsko strukturno enoto nadalje sestavljajo stiri strukturne podenote: podenota Mali Vrh, Rdeca Skala, Drnska strukturna podenota in podenotaVrh Mangarta.
Na obmocjuJulijskih Alp sem odkril tri tipicnerazvoje, ki so znacilni za tri razlicne paleogeografske enote. 
Najbolj popolno zapmedje izdanja v Travniski strllkturni enoti in se zacne s plitvovodnimi spodnjeliasnimi apnenci, nad katerimi konkmdantno lezijopliensbachijski apnenci distalnega selfa Sedlske f()J'macije. Zaporedje se nadaljuje s toarcUskimi crnimi in rjavimi skrilavimi glinavci z vmesnimi plastmikremenastih apnencev, ki predstavljajo Skrilsko formacijo. Sledijo diskordantno odlozeni spodnje/srednje do spoclnje pelagiclli kremenasti sedimenti z vmesnimi karbonatnimi resedimenti Travniske formacije. Doigaska vrzel (zgomji in aalenij) loci Skrilsko od Travniske f()rmacije. Zaporedje se zakljuci s pelagicnimi apnenci tipa biancone zgornjetithonijskein spodnjekredne starosti. J urske globljevodne kamnine Travniskc strukturne cnote paleogeografskopripadajo Bovskemu jarhl.
Za zaporedje v Dolini Triglavskih jezerje zna-Cilno, da na spodnjejurske plitvovodne apnencediskordantno kondenzirani bajocijski do spodnjetithonijski apnenci tormacije Prehodavci (apnenci tipa ammonitico rosso). Nad njimi leZijozgornjetithonijski mikritni apnenci tipa biancone. Apnenci formacije Prehodavci so bili preuceni tudi v Ravnem Lazu,Jezeru v Luznici, Cistemu Vrhu in pri Vasi na skali. Predstavljajo tipicen razvqj Julijskega praga.
Najbolj kondcnzirano sedimentacijo odraza profil v Mangartski strukturni enoti. Tu nad plitvovodnimi zgornjetriasnimi in spodnjeliasnimiplitvovodnimi apnenci zjurskimi neptunskimi dajkineposredno leZijo aptijsko-albijske ali senonske globokovodne kamnine Scaglia variegata in Scaglia rossa. Neptunski dajki so nastajali v robnih delih J 1I1ijskega praga. 
na preiskanem ozem!ju odraZa vpliv ekstenzijske tektonike zaradi rifti nga v zahodni Tetidi, evstatitnih nihanj morske gladine in regionalnih sprememb. Glavne faze vjurskem do krednem razvojuJulijskega pokrova so 
1) V spodnjijurije na obmo(juJulijskegapokrova obstajalo plitvovodno obmocje, imenovano Julijska karbonatna platforllla. 2) Faza neenakc)mernega pogrezanja v pliensbachiju je povzrotilarazpad JlIlUske karbonatne platforme na bloke z razlicno hitrostjo pogrezanja. Nastali sta dye novi paleogeografski enoti: bo!j pogreznjeni bloki pripadajo Bovskemu jarku, relativno obmocja predstavljajoJulijski prag. V Bovskellljarku so se v pliensbachiju sedimentirali apnenci distalnega selfa Skrilske formacije, llledtem ko v centralnem 
praga ni bilo sedimentacije, ker jebilo obmocje ver:jetno na kopno. V robnih 

/zv[deh 
delihJulijskega praga so v tern casu neptunski dajki. 3) Na meji pliensbachij-toarcijje evstaticni padec morske gladine na bolj pogreznjenih blokih povecal intenziteto morskih tokov in stem ustvaril 
za nastanek zelezovih-manganovih gomoljev,ki so znaCilni za vrhnji del Sedlske formacije. 4) Spo
glinavci formacije Skrile predstavljajoznaCilen sediment globalnega anoksicnega dogodkain v spodnjem toarciju. 5) Druga faza pospeSenega pogrezanja v na ozemljuJulijskih Alp povzrocila dodatno poglobitev.Bovskegajarka postane del globljevodnega bazena,ki je neposredno povezan z Dinarsko karbonatno platformo, s katere material za karbonatne turbidite. ki predstavljajo Julijski prag,se v tern casu pray tako potopijo in na njih se zacne sedimentacija kondenziranih apnencev formacije Prehodavci (apnenci tipa ammonitico rosso).6) Zgornjebathonijski padec morske gladine se v bazenu odrazi s horizontom brec, ki predstavlj,yo
proksimalen turbiditni facies. Na podmorskiplanoti zaradi morskih tokov v tern casu nastajajo zelezo-manganovi gomoUi. 7) Tektonska faza v kimmeridgiju je povzroCila nastanek brec v bazenu, na podmorski planoti pa so nastali neptunski dajki. 8) Na spodnji/zgornji tithonij se pelagicna kremenasta sedimentacija v bazenih in sedimentacija apnencev tipa ammonitico rosso na podmorskih planotah preneha in zacnejo se sedimentirati pelagicni apnenci tipa biancone. Ta facialna sprememba je regionalna in istocasna v vseh bazenih v zahodni Tetidi. Globljevodnajurskatopografija je tako v spodnji kredi ze delno izenacena. 9) Nova tektonska faza v albiju je povzrocila ponovno reorganizacijo sedimentacijskega prostora in posledicno sedimentacijo formacije Scagliavariegata. 10) Po novi tektonski fazi v zgornji kredi (pred senonom) seje zacela sedimentacija formacijeScaglia rossa. 
Razvoje Bovskegajarka sem primerjal z razvoji v Tolminskem in Belluno bazenu. so si v splosnem podobni, vendar obstajajo pomembnerazlike. Obmocje Bovskegajarka se je potopilo sele v pliensbachiju, medtem ko sta Tolminski in Belluno bazen v tern casu ze globoka bazena. V srednjiin zgornji juri pa je bilo Bovskega bazena blize Dinarski karbonatni platformi kot omenjenabazena. RazvojiJulijskega praga pa so podobni razvojem na Trento V vecini preiskanih profilovJulijskega praga srednji clen Prehodavci ni razvit. Ti profili so podobni profilom v nekaterih delih Trento platoja, srednji kremenasti del formacije Ammonitico Rosso 

1 



INTRODUCTION 

During the Jurassic the Alpine-Mediterranean region ( outhern Alps and Dinarides) belonged to the southern passive continental margin of the Tethysand experienced extension due to rifting. The rifting re ulted in a brake up of preexi ting carbonate platforms, producing a complex pattern of pelagicbasins and escarpment-bounded pelagic platforms, which existed until Late Cretaceous. 
TheJulian Alps, as the eastern continuation of the Southern Alps, are typical example ofa Tethyanrifted margin, characterized by a thick pile of Upper Triassic to lower Jura sic platform limestones overlain by condensed and highly discontinuous Jura ic to Cretaceous deeper-water deposits that show drastic difference in thickness and abruptlateral facies changes. The study of these depositsand pre ent hiatuses enabled u to elucidate the complex vertical and lateral relationships that characterize the area and thus refine aJurassic to Cretaceous paleogeography, sedimentary evolution and rifting history of the outhalpine-Dinaric continental margin. 
1.1 GEOLOGICAL SETIING 
The study area is situated in NW Slovenia in the Julian Alp . The Julian Alps comprise the northwestern part of Slovenia and easternmost part of Italy (Fig. l.1). They extend from the Soca valleybetween Tolmin and Kobarid , Mt. Stol ridge between Kobarid and Gemona (Italy) in the outh, to the Kanal ka dolina (Val Canale, Italy) in the north and the Zgornja Savska dolina (the pper Sava Valley) in the east. 
The Julian Alps are a part ofa complex tructure of NW Slovenia, formed mostly in the Cretaceous and in the Tertiary during the Alpine orogeny(Doglion i & Bosellini 1987, Poli & Zanferrari 1995,Bresnan et al. 1998, Placer 1999). They structurally 

Fig. l .l Geographic localion of theJulian Alps (enlarged ector of the map ofSlovenia l: J.000.000, map courLesy of Anton Melik Geographical Institute). 



I Introductiun 
tributed approximately in N-S direction is similar to the pattern recognized westward, where in the E-W direction we observe the Dinaric (Friuli) Platform,BelluO() Basin, and Trento Plateau (Fig. 1.4) (Aubouin et al. 1965, Bosellini et al. 1981, Winterer & Bosellini 1981, Buser 1989,1996, Buser & DebeUak 1996, Placer 1999).
In northern Italy, the east-west arrangementof the Jurassic paleogeographic units was not significally changed by north-south shortening duringthe Alpine orogenesis. The units are still arrangedin their original order and allow a relatively clear paleogeographic reconstruction. The eastern partof the Southern Alps (northwestern Slovenia) was characterized by NW-SE striking normal faults in the Jurassic. Strong Tertiary polyphase thrusting first in Dinaric (NE-SW) and later in the South Alpine(N-S) directions thus completely obliterated the original Mesozoic paleogeography. Different paleogeographic units are thus only partly preserved and belong to different overlapping thrusts. In northwestern Slovenia facies belts are now primarily E-W oriented but the original geometry of the Mesozoic margin has notyet been reconstructed in detail. The reconstruction ofprimary Mesozoic spatial relationships is additionally hindered by the fact that in the Julian Nappe, upper Triassic shallow-water strata tend to be preserved whileJurassic and Cretaceous rocks are generally eroded. 
The Mesozoic succession in the Julian Nappeis characterized by a thick package of shallow-water Upper Triassic to lower Lower Jurassic limestones overlain by a condensed upper Lower Jurassic to Upper Cretaceous deeper-water deposits. Because of this stratigraphy, the inferred paleotopographicsetting of this area (Fig. 1.4) during the late Early to Late Jurassic was thought to be a pelagic submarine high (Julian High in Buser 1996). The Julian High, however, was not a uniform plateau but was dissected into differentially subsided blocks. Some of these blocks became isolated pelagic carbonate platforms (sensu Santantonio 1994), while other blocks formed deeper basins, which received gravity-displaced material from the adjacent shallow-water platforms (Cousin 1981, Smuc & Gorican 2005).
The similar spatial distribution of topographichighs and depressions in northern Italy and northwestern Slovenia (Fig. 1.4) also raised the questionof a possible deeper-water paleogeographic connection between the Belluno and Slovenian basins. Some authors (Aubouin et al. 1965, Cousin 1970, 1981, Buser 1996, Buser & DebeUak 1996) stated that the Belluno and the Slovenian Basin did not form a physiographically uniform basin but were both wedge-shaped and separated by a topographichigh, whereas others (Bosellini et al. 1981, Winterer & Bosellini 1981, Bellanca et al. 1999, Clari & Masetti 2002) suggest that they were connected directly. Our recent investigations (Smuc & Goriean 2005, this study) suggest that at least until the Pliensbachian, the Slovenian and Belluno basins were not continuous but separated by a topographic high, represented by the Travnik structural unit of the Mt. Mangart saddle. 
The Julian Alps are composed predominantlyof Upper Triassic shallow-water strata (DachsteinLimestone and Main Dolomite) and Jurassic and Cretaceous deposits are relatively rare (Fig. 1.5).They are restricted to relatively small areas and are usually fault-bounded. However, complete successions can be found in a few localities. The key-areasfor understanding theJurassic tectono-sedimentaryevolution of the Julian Alps are the Triglav Lakes Valley and Mt. Mangart saddle (localities 1 and 2 in Fig. 1.5). The Jurassic-Cretaceous successions in these areas are relatively well exposed. Additional areas where Jurassic and Cretaceous deposits were investigated are Ravni Laz, Luznica Lake, Vas na Skali, and Cisti Vrh (localities 3 to 6 in Fig. 1.5). In these localities, the successions are smaller and less well-exposed, so that only one section could be studied from each locality. 

1.2 PREVIOUS RESEARCH 
Stur (1858, ref. in Diener 1884, p.686) was the first to recognize the Jurassic beds in the TriglavLakes Valley. TheJurassic age of the beds was later confirmed by Kossmat (1913). Salopek (1933) first described the Jurassic and Cretaceous beds in the Triglav Lakes Valley. Ramovs (1975) dated red nodular limestones of the Triglav Lakes Valley as Oxfordian and Kimmeridgian.
Winkler (1920a, 1920b) and Winkler-Hermaden (1936) investigated the coarse-grainedJurassic Krn breccia at Luznica Lake and interpreted them as transgressive deposits following the MiddleJurassic orogenic phase. This interpretation was later refuted by Babic (1981) who found out that this "Krn breccia" represents fillings ofneptunian dykes provokedby the repeatedJurassic extensional fracturing ofa submarine topographic high.
Selli (1963) constructed the first viable geological (I: 1000(0) and tectonic (1 :250 (00) map ofthe Julian Alps. 

1 Intmdllrti(J1I 
Cousin (1981) investigated western Slovenia together with northeastern Italy. Within his studyhe includedJurassic and Cretaceous localities in the Julian Alps: the Mt. Mangart saddle, Bavsica, Bovec, Na Skali, Vrsnik, Triglav Lakes Valley and the Mt. Krn area. Cousin (1981) mapped some of the areas and compiled composite stratigraphic sections ofthe exposedJurassic and Cretaceous formations. In the Julian Alps he recognized two parallel N-S oriented basins: "Sillon de Bovec" and "Si1lon de Bled", separated by a submarine topographic high (in the Komna area). To the south, these two mergewith the E-W oriented "Sillon the Tolmin". 
TheJulian Alps were also mapped for the Basic Geological Map ofYugoslavia, at a scale of1:100 000 by Buser (1986) (the Tolmin and Videm sheet, 1: 100 
(00) andJurkovsek (1986) (the Be!jak and Ponteba sheet, 1:100(00). Both authors concluded that the Jurassic and Cretaceous strata are restricted to a few square kilometers and that they are predominantlyfault-bounded. Furthermore, in the explanatory notes of the maps, the authors described the condensed Jurassic and lower Cretaceous rocks. 
Jenkyns (1988) focused on a horizon oforganic-rich shales with siliceous-limestone intercalations that occur at the Mt. Mangart saddle, interpretingthese deposits as a product ofthe Toarcian Oceanic Anoxic Event (OAE). Recently, the Toarcian ageof these deposits was confirmed using well-preserved and diverse radiolarian faunas (Gorican et al. 2(03).
Jurkovsek & Kolar:Jurkovsek (1988) described the crinoids from the Tithonian-Valanginian beds east of Vrsnik. Lower Cretaceous nannoplanktonand radiolarians from Vrsnik were described byPavsic & Gorican (1987).
Buser (1989, 1996) studied the geolob'Y and paleogeographic evolution ofwestern Slovenia. He determined that the area of theJulian Alps in Late Triassic and earliestJurassic belonged to a shallow-water carbonate platform, called theJulian Carbonate Platform. During the earlyJurassic, this platform was drowned and became a pelagic submarine high,named the Julian High.
The most extensive research on Jurassic and Cretaceous deeper-water deposits was publishedby Jurkovsek et al. (1990), focusing on the pelagicbeds at Mt. Mangart saddle, Pldivec, Bavsica, Vrsnik, and at C:rni Vrh. They mapped and constructed composite stratigraphic sections of the UpperTriassic to Cretaceous formations. Jurkovsek et al. (1990) concluded that until the late EarlyJurassic, the sedimentary environment of the rocks forming the Julian Alps was characterized by shallow-water sedimentation on Julian Carbonate Platform that was, in the late EarlyJurassic, dissected into differentially subsiding blocks characterized by deeper-watersedimentation. 
In the late 1990s we initiated the systematicstratigraphic and sedimentologic research and detailed mapping of the Mt. Mangan saddle and Triglav Lakes Valley. The sedimentary evolution and radiolarian dating of the Travnik section (in this book this section is named MAl) and MA6 section have been published (Gorican et al. 2003, Goriean & Smuc 2004, Smuc & Gorican 20(5). Herein I describe the Iithostratigrapy of these sections and I correlate them with other sections. 

1.3 AIMS OF VOLUME 
The aims of this volume are to present a detailed sedimentologic and biostratigraphic study of the Jurassic to Cretaceous successions oftheJulian Alps,including formal definitions ofthe lithostratigraphicunits, the interpretation of sedimentary environments and discussion ofeustatic vs. tectonic factors that controlled the observed depositional pattern.We compare the Jurassic sedimentary evolution of the Julian Alps area to the coeval evolution of the Belluno and Slovenian basins, and Trento Plateau. 
1.4 	DEFINITION OF THE PALEOGEOGRAPHIC UNITS 
The Julian Alps record the rifting and platformdrowning and differential subsidence and thus formation of differ'ent paleogeographic units in theJurassic. Because the nomenclature consideringthese units is not consistently used in the publishedliterature, definitions applied herein are given. 
1.4.1 JULIAN CARBONATE PLATFORM 
TheJulian Carbonate Platform, as defined by Buser (1989), was a Late Triassic to EarlyJurassic shallow water platform that was located northward from the Tolmin Troug-h (see below). TheJulian Carbonate Platform deposits are now exposed in the Southern Karavanke Mountains, Julian Alps, and Kamnik-Savinja Alps. According to Buser (1989) the Julian Carbonate Platform formed in the early Carnian (Cordevolian). The platform ceased to exist in the 

1 Inlrotil1rlion 
middle to late Early Jurassic when it was dissected into blocks with different subsidence rates (Buser1989) . 
l.4.2 	JULIAN HIGH 

The term Julian High was introduced by Buser (1996) to denote the entire drowned Julian Carbonate Platform that in late Early Jurassic became an isolated submarine high with condensed sedimentation, which lasted until the early Cretaceous. However, in the Middle Jurassic, some drowned blocks of the former Julian Carbonate Platform became deeper basins receiving gravity-displacedmaterial from the adjacent shallow-water platform
(e.g. Mt. Mangart, see Cousin 1981,Jurkovseketal. 1990, Smuc & Gorican 2005, this volume) and thus not submarine highs. Therefore, in this volume the tenn Julian High refers only to those subsided blocks, which were in the Middle and LateJurassic characterized by condensed sedimentation of Ammonitico Rosso-type limestone that is typical of a submarine plateau (e.g., Triglav Lakes Valley). The blocks where the Pliensbachian to Tithonian pelagicdeposits are preserved only as neptunian dyke fills also correspond to the Julian High (e.g., the Mangan structural unit). All succes-sions of the Julian High are now exposed on theJulian Nappe. 
1.4.3 	SLOVEN IAN BASIN: TaLMIN TROUGH AND BOVEe TROUGH 

The term Siovenian Basin is used in Siovenian geological literature as both a paleogeographic and a structural term. As a paleogeographic unit it was introduced by Cousin (1970) who defined the term "Sillon Slovene" for the area extending from Kobarid to Tolmin and further east, with deeper-watersedimentation essentially from the Late Triassic to Late Cretaceous. Buser (1989,1996) used the name Siovenian Basin for a wider area. With it, he marked the approximately east-west directed narrow facies belt extending throughout the entirety of Slovenia in which Triassic to Cretaceous deeper-water strata crop out. Recently, Smuc & (;ar (2002) remarked that the term Siovenian Basin is actually used for two temporally different paleogeographic units, because it comprises the Middle Triassic basin and the basin that developed later in the Latest Triassic and Jurassic. Smuc & (:ar (2002) pointed out that Middle Triassic tectonic activity ceased during the 
Carnian; at that time, carbonate platforms prograded quickly into surrounding basins and tilled them almost completely. So by Norian-Rhaetian time, western Slovenia constituted an area with minimal topographic relief (Buser 1989, Ogorelec & Rothe 
Larger regional Middle Triassic events do not seem to be directly related to the Late Triassic-earlyJUI'assic rifting events that led to the Jurassic-EarlyCretaceous ocean spreading (see Winterer & Boseilini 1981, Doglioni 1987, Bertotti According to Smuc & (;ar (2002) the Middle Triassic basin and Late Triassic to Jurassic basin share the same name (Slovenian Basin) but belong to two different stages in the paleogeographic evolution of western Slovenia. Herein I propose that the name Siovenian Basin should be limited in time to the Late Triassic and younger basin. 
The Tolmin Trough as defined by Cousin (198 I) constitutes a part of the Siovenian Basin. It comprises the east-west directed facies belt between Kobarid and Cerkno with deeper-water sedimentation from the Jurassic to latest Cretaceous. 
The Bovec Trough was defined by Cousin ( 1981) to denote the N-S trending small transverse basin with less marked basinal characteristics than the Tolmin Trough. According to Cousin (1981)the Bovec Trough comprises the Mt. Mangan saddle (Travnik hill) and Bavsica area. Herein the subdivision of Cousin (1981) is followed. Structurally, the successions of the Tolmin Trough form the Tolmin Nappe, whereas the successions of the Bovee Trough belong to the Julian Nappe (sensuPlacer 1999). Herein the terril Bovec Trough is used for the Pliensbachian to lower Cretaceous deeper-water deposits that crop out in the Travnik structuI'al unit. 
l.5 METHODS OF INVESTIGATION 
Detailed mapping-was carried out for the Mt. Mangart saddle and Triglav Lakes Valley areas on a 
I: 10 000 scale in order to separate structural units that differ in thcir stratigraphic evolution. 
Sedimentological field observations included the detailed measurement and sampling of 14 sections. The stratigraphic logs were measured in the 
1: 100 scale for basinal successions, and in 1: 50 scale for condensed successions. More than 1100 thin sections were prepared for microfacies and biostratigraphic analyses. The successions were dated with foraminifers and calpionellids found in thin sections. Radiolarians were used to datc the 

1 Introduction 
basinal deposits ofMt. Mangart (Goriean et al. 2003, Goriean & Smuc 2004, Smuc & Goriean 20(5).
Resedimented limestones of the Travnik Formation were classified according to the classification scheme of turbidite facies of Mutti (1992), which consists of nine main facies types (Fl to F9). For studied sections, local transgressive-regressive cycles were determined and correlated with the Tethyantransgressive-regressive cycles as described in Graciansky et al. (199H), Jacquin & Graciansky (1998),andJacquin et al. (199H). 
Rock samples, thin sections, and radiolarian residues are stored at the Ivan Rakovec Institute of Paleontology, ZRC SAZU, ldubljana. 

2 





GEOLOGICAL MAPS OF KEY-AREAS 

The Julian Alps are characterized by strong end Cretaceous to Tertiary polyphase thrusting and strike-slip displacement. Thus the different paleogeographic units today belong to different thrust sheets in addition deformed along strike-slip faults. In order to delimit these different structural and therefore different paleogeographic unit'i, the detailed mapping ofthe key areas Triglav Lakes Valleyand Mt. Mangart saddle was necessary. 
2.1 GEOLOGICAL MAP OF THE TRIGLAV LAKES VALLEY 

Geological map of the Triglav Lakes Valley and main cross-sections are illustrated in Figs. 2.1, and 2.2. 
In general the Julian Alps are part of the Julian Nappe, which is internally thrusted and faulted. In the Triglav Lakes Valley area, two of these smaller-scale nappes are present. The Krn Nappe is situated in the central and western partof the valley (see Fig. 2.1) and is composed of bedded Upper Triassic to lowermostJurassic platformlimestones, unconformably overlain by Jurassic and Cretaceous deeper-water deposits (Buser 1986,1987, this study). The Krn Nappe is overthrust by the Zlatna structural unit that is composed of white, massive Upper Triassic limestones (Buser1986, 1987). The thrust plane is clearly visible in the northeast-ernmost part ofthe valley (east ofthe Prehodavci cottage) and in the southernmost partof the valley (see Fig. 2.1) whereas in the main partof the valley the thrust plane is covered by scree and was located on the basis of different lithologyof the overlying nappe.
Both structural units are additionally cut by a large, dextral strike-slip fault in the 20-200° direction. This fault is probably part ofa fault called the Vrata fault byJurkovsek (1986). In the northern (upper) part ofthe valley, the fault branches, (Figs. 2.1, 2.2, cross section A, B, C) extending southward trough the entire valley. The eastward branch of the Vrata fault is called Spicje fault and the west one is Zelnarice fault. The Triglav Lakes Valley is a topographic depression located between these divergent faults and is characterized by normal faults extending mainly in the NW-SE and SW-NE direction (Fig. 2.1). These normal faults cut the valley into blocks with different subsidence rates and rotations (Figs. 2.1, 2.2 (cross section D), 2.3a,b, 2.4a,b), indicating an extensional regime between the faults. These blocks are recognizable because ofthe spatial occurrence oftheJurassic Prehodavci Formation (condensed limestones of the Ammonitico Rosso type) (Fig. 2.1). In the northernmost part ofthe valley, the Prehodavci Formation occurs at the 2050 m ofaltitude while towards the southern part of the valley, the altitude of the Prehodavci outcrops decreases, so in the southernmost part of the valley the Prehodavci Formation crops out at an altitude of 1650 m (Figs. 2.1, 2.2 (cross section D)). The different rotation of the blocks is clearlyevident by the different dips ofbedding within each block (Fig. 2.1). 
On the basis ofthese data we concluded that the structure ofthe Triglav Lakes Valley formed during two different tectonic phases. Overthrusting of the Zlatna Nappe on the Krn Nappe represents the first phase. During the second phase this older structure was cut by the larger dextral strike-slip Vrata fault. In the northern part of the valley the fault parts in branches forming a negative flower structure extending southward trough the valley. The TriglavLakes Valley thus is an extensional wedge between these branches (Fig. 2.5) as evidenced by different the subsidence and rotation of the blocks in the valley. 
















3 Stratigraphy 
stratigraphic range was determined on the basis of the tratigraphic position and pre nce of bivalve Lithiotis pmblematica (Gumbel), alga Palaeodasycladus medilerraneus (Pia), and foraminifer Agerina martana (Farinacci) by (Cousin 1981 , Buser 1986, Buser & Debelja k 1996,jurkovSek 1986,jurkov"ek etal. 1990, "muc & Goriean 2005).
A r gional discontinuity surface mark the topof the Lower jurassic platform limestone, which i cut by numerous neptunia n dyk and/ or overlain by more or less condensed dee per-water trata. 
In this study the LowerJurassic platform limesto ne were studied in th e Triglav Lakes Valley (sections TVl and TV4, Fig. 3.1), at Ravni Laz (section Rl, Fig. 3.2) and Luznica Lake ( ection Ll, Fig. 3.2), and at Mt. Ma ngart (section MAl, Fig. 3.3, ection MA7, Fig. 3.6). Only the top few meter below the discontinuity urface were investiga ted in detail. 
TRiGLA V LAKES VALLEY, RA VNI LAZ, AND LUZNJCA LAKE: SECTIO S TV1, TV4, R1, L1 (Figs. 3.1, 3.2) 

Description offacies.-Lower jura sic platform limestones conformably overlie pper Triassic Dachstein Lime tone. They consist of up to 1.8 m thick beds of homogenous mudstone to wackestone with pellets that alternate with thinn r beds (l0-50 cm) of packsto ne to wackestone with peloids and fenestral limestone. 
The homogenous mudstone (Fig. 3.7) to wa kes tone is light brown. At place it exhibits stromatactis and shelter cavitie , bird -eye textures,geopetal infillings and also fene tral porosity. The grains are ra re peloids, 0 tracods, foraminifer (Textulariidae, Valvulinidae), algae, and fragments of bivalve , ga tropods and bryozoans. At placespellets are abundant, forming a packstone fabric and repre ent majority of grains. The limestone is fr que ntly bioturbated. 
The inter tratified wacke ton e to packstone, in place a grain tone (Fig. 3.8, 3.9), con i ts ofpeloids, ooids, bioclasts and intraclasts ofmudstones, fenestral limestones and, grainstones with peloids. Bioclasts are foraminifers (Textulariidae, Valvulinidae), fragments ofbivalve ,0 tracods, brachiopods, gastropods and algae (Palaeodasycladus p.). Fragments ofechinoderms are rare. At Ravni Laz these lime tone also contains lumachelle with the following bivalves: Geroilleiopema? p., Mytilopema? sp., and Pseudopachymytilus? sp.(Fig. 3.10, determin ed by I. Debeljak). 
In the grainstones, grain are cemented fir t by fin e-grained mosaic cement, syntaxial cement and then by coarse r sparite and neomorphic micrite. 
Fenestral limestones are thin-bedded (in some place bed thickness reach s 30 cm), laminated and exhibit birds-eyes, laminoid fe nestrae, helter cavitie ,and geopetal infilling (Fig. 3.11). They are characterized by the alternation of up to 0.2 mm thick micritic laminae with up to 0.6 mm thick laminae compo ed of microsparite (Fig. 3.12). Grains are rare 0 tracods and pellets.
Age.-The age of this lim estone is not well constrained due to the absence ofdiagnostic fossils. However on the basis of the stratigraphic position, local pre ence oflarge bivalves (see above), and correlation with similar beds in the Dinaric Carbonate Platform (Buser & De be ljak 1996) , Trento Plateau (Clari & Masetti 2002, and refer nc s within) and lower jurassic hallow-water deposits from Alge ria (Elmi et al. 2003) and Morocco (Elmi et al. 1999) an earlyPliensbachian age is suggested for th e d posits. 

Fig.3.8 Platform lim eSLOnes: limeSLOne wilh peloids, ooids,Fig.3.7 Platform limeslones: mud LOnewilh mall bel1lhic echinoderm fragments, fragments of bivalves and bel1lhic foraminifers (seclion TV J). foraminifers (seClion TV4). Scale bar is J mm long. 
3 Stratigraphy 
Fig. 3.9 Platform limestones: grainstone with algae, intraclasts , peloids, be nthic foraminifer and fragments of bivalves (section Rl) . Scale bar is 1 mm long. 
Fig.3.10 Platfonn limes tone : lumachelle of bivalve (seclion Rl, ee Fig. 3.2). 
Depositional environment.-The micritic lime-
tones were formed in a low-energy ubtidal re
tricted lagoonal environment. edimentary characteri tic of the inter tratified fenestral lime tone indicate deposition in ubtidal-intertidal environment. Peloidal limestones with variou grains were deposited in a high-e nergy ubtidal environment affected by currents. The grains, in particular bivalves were formed on inner parts of the platformand were later transported to th e margins. Vertical facie changes observed in all ection reflect change of the environment, probably due to the high frequency sea-level oscillations (see discussion in chapter 4.1). 
Fig. 3. 11 Platform limesto nes: limestone with fenestral porosity (section 1Vl). cale bar is 1 mm long. 
Fig. 3. 12 Platform limestones: la minated limestone (section 1Vl). 
MT MANCART SADDLE -TRA VNIK STRUCTURAL UNIT SECTIO MAl (Fig. 3.3) 
Description.-The dominant lithofacie i a lightgray, massive, medium to well-sorted grainstonecomposed of non-skeletal and skeletal grains (Fig. 
3.1 3). on-skel tal grains are mainly intraclasts of peloidal wackestone/ pack tone and mudstones,peloids, micritized ooids and oncoids. The skeletal component con i t of echinoderm fragment,gastropods, bivalves, spongiomorphids, fragmentsof algae and foraminifer. Grain are cemented first by bladed and syntaxial cements and th e n by coar er sparite. 

3 Straligm/Jh), 
Fig. 3.13 Platform limesLOne : grai nstone with peloid ,intraclasts of mudstones, and oncoids (s ction MAl ).Scale bar is 1 mm long. 
Fig. 3. 14 Platform limestone: packstone with peloids,illlraclasts of mudsto nes, belllhic foramini fe rs ( ection MA l). Scale bar is 1 mm long. 
In the uppermost pa rt of shallow wate r limestones, up to 1 m thick b d s of the above d escribed grainsto ne alte rna te with up to 30 cm thi ck bed s o f a fin e r-grain ed wackesto ne / packsto ne (Fig. 3. 14). Grains a re pelo ids, rare oo id , be nthic fo raminife rs (T extula riidae, Val vulinidae, L enliculina sp. , a nd Agerina marlana (Fa rin acci», ra re echinoderms, and bivalves. 
Age.-In th e uppe r pa rt o f th e lim e to ne the prese nce ofAgerina manana (Fa rinacci ) (accordingto th e bi ozonal sc he me o f Chiocchini e t al. (1994) 

uggests a Plie nsbac hi a n age. In th e lowe r pa rt o f the ectio n A. martana is not pres nt 0 a Sinemul;an agefo r this lower pa rt i possibl e, but no t confirmed . Depositional environment.-Gra insto nes o f the lowe r part we r d e posited in a high-e ne rgy ubtidal 
e nvironment, mos t pro bably a sand belt in a mar-g in al pa rt of a sha llow-wa te r carbonate pl a tform (cf. Di Stefano et al. 2002 ) . The maj o ri ty of grain 
orig ina ted from a subtidal lagoonal e nviro nment in the platform in te rior and wa later tra nsported to the platform ma rgi n . The fin e r-grained peloidal wacke to nes/ pac ksto nes inte rcala ted in th e uppe r pa rt were d e po ited in hydrod ynami cally quie ter e nvironment locate d bas inwa rd o f the ma rg in a l 
andbelt The deepe r d epositio nal e nvironme nt is indicated by ope n marine ele me n ts (Lenliculina sp. ) . 
MT. MANGART SADDLE: MANGART STR UCTURAL UNIT: SECTIO MA7 (Fig. 3.6) 
Description.-The uppermost Trias ic to LowerJurassic platform limesto ne o f the Ma nga rt structural unitwas tudied at sectio n MA7 (Fig. 3.6). Itis represented by a light gray mass ive bo und tone. On th e hand-specime n and thin ectio n scale it is grain tone with corals, po nges, calca reous algae, a nd fragme nts ofbivalves, ga tropod , brachiopod and echinoderms (Fi g. 
3.15). Pe lo id and foraminife r (Involutinidae, 0d o a ridae, Agerina manana (Fa rin acci» a re pre e nt but no t freque nt. In places, in traclas ts composed of g ra instones with ooids are also p rese nt. Gra ins a re ce mented with spa ritic ce me nt. 
Age.-In the pl a tform limesto ne of the Ma ngart structura l unit Jurkovsek e t al. (1990 ) fo und the fo llowing fo ra minife rs: Galeanella panlicae (Za ninetti & Bronnimann) and Triasina hantkei (Maj zon ), and d e te rmined a Rh aetia n age for th ese d e posits. H oweve r, from th e a rticl e ofJurkovsek e t al. (1990) it is no t cI a r from which pa rt (uppe r o r lowe r) 
Fig.3. 15 Platfo.-m limestones: grainstone with corals and 
tro mato poroid frag ments (Mali Vrh structura l subuni t,Mangan saddle). cale bar is J mm long 

the samples were taken. In our study we found, in the uppermost part of these limestones, Agerina marlar/a (Farinacci) suggesting a Pliensbachian age(according to the biozonal scheme of Chiocchini et al. (1994». On the basis of these data the most probable age range is Rhaetian to Pliensbachian. 
Depositional environment.-The Lower Jurassic platform limestone of the Mangart structUl'al unit is a part of a small patch-reef. The presence of intraclasts of grainstones with ooids suggests that the patch recfwas located within an oolitic sand belt in the marginal part of the carbonate platform. 
JULIAN HIGH 

The julian High represents an isolated pelagicplatform (sensu Santantonio 1994) that was formed after the drowning oftheJulian Carbonate Platform. The distinctive characteristic of the Julian High is that Pliensbachian platform limestones oftheJulian Carbonate Platform are unconformably overlain by Bajocian to lower Tithonian highly condensed limestones ofthe Prehodavci Formation. In the most condensed sections, the Lower Jurassic platformlimestones are penetrated by polyphase jurassicneptunian dykes and unconformably overlain bymiddle Cretaceous Scaglia variegata or Senonian Scaglia rossa. The successions oftheJulian High are preserved in the Triglav Lakes Valley, at Ravni Laz, Luznica Lake, and in the Mangart structural unit. At C':isti Vrh and Vas na Skali, only parts of the Prehodavci Formation crop out, and the contact with the underlying platform limestones can not be seen. 
PRA'lfOf)Avel FORMATION 

Type section.-TVI (Fig. 3.1, for location see Fig. 2.1).The formation is named after Prehodavci saddle in the Triglav Lakes Valley, situated 1.2 km northward of the type section. The Prehodavci Formation was investigated in the Triglav Lakes Valley (sectionsTVI to TV5, Fig. 3.1), at Ravni Laz (section Rl, Fig.3.2), near the Luznica Lake (section Ll, Fig. 3.2), at Cisti Vrh, and at Vas na Skali. The best-preservedsections occur in the Triglav Lakes Valley where Jurassic strata crop out all along the valley (see geological map Fig. 2.1).
Short definition.-The Prehodavci Formation is composed ofcondensed limestones ofAmmonitico Rosso type and is subdivided into three members. The Lower Member consists ofcondensed, red, bedded bioclastic limestones with Fe-Mn nodules that 
gradually pass into light gray, indistinctly nodular limestones. The Middle Member is composed of thin-bedded micritic limestones. The Upper Member unconformably overlies the Lower or Middle Member. It is represented by red nodular limestone, and by red marly limestones with abundant Saccocoma sp.
The Prehodavci Formation unconformablyoverlies the Upper Triassic to Lower Jurassic platform limestone of the Julian Carbonate Platform. The contact is marked by a highly irregular unconformity surface. This surface is marked with up to 3 m deep and up to 10m wide oval depressions cut into the Lowerjurassic platform limestones that are filled with limestones of the Prehodavci Formation (Figs. 3.16, 3.17, 3.IR).
The Prehodavci Formation is overlain by the upper Tithonian pelagic Biancone limestone. The formation reaches a maximum thickness of about 15 m. 
Note.-In the following facies description we are using term "nodules" as defined by Martire (1996):nodules are all the parts ofthe rock ofvariable shape(ellipsoidal to very irregular but normally rounded)and size (from few mm to several em) limited bytransitional or sharp boundaries with the surrounding matrix from which they are distinguished by a marked contrast in texture, color, and compactionalfabric. 
Age.-The Bajocian to early Tithonian age ofthe formation is determined on the basis of the ammonites found by Ramovs (1975), planktic foraminifers, Saccocoma sp., and the stratigraphic correlation with the Rosso Ammonitico Formation. A more precise age assignment is discussed for each member individually, below. 
Previous work.-The Jurassic beds were first mentioned by Stur (IH5H, ref. in Diener 1884, p.686). He found ammonites in the bedded limestone and assumed that they were Jurassic in age. Later, the./urassic age of the limestones was confirmed byKossmat (1913), who found that they overlie the Dachstein Limestone and are overthrust by a massive reeflimestone ofthe Ziatna Nappe. Seidl (1929) first gave a schematic cross-section ofJurassic beds in the Triglav Lakes Valley. Salopek (1933) provided the first general description ofJurassic and lower Cretaceous beds in the Triglav Lakes Valley, finding the following ammonites in theJurassic beds: Phyllo(;ems sp., lIolcophyllo(;rms?sp., and Perist,hinctessp. Ramovs (1975) dated the red nodular limestones in TriglavLakes Valley as Oxfordian and Kimmeridgian on the basis of the following ammonites: HnastJirio(:(:ms 


3 Stratigraphy 
sp., Greg(Jryceras sp., Lytoceras sp., Paraspidoceras sp.,and owerbyceras sp.. The area of the Triglav Lake Valley was mapped for the Basic Geological Map of Yugoslavia 1: 100000, by Buser (1986) andJurkovSek (1986). 
LOWER MEMBER OF THE PREHODAVCI 
FORMATION 

The Lower Member of the Prehodavci Formation wa investigated at Triglav Lake Valley (sections TVI-TV5, Fig. 3.1), Ravni Laz ( ection Rl, Fig. 3.2), and Luznica Lake (section L1 , Fig. 3.2) and consists of biocla tic limestone with Fe-Mn nodules, limestone with ooids th at occur only locally, and light gray nodular limestone. The Lower Member is dis-conformably overlain by either the Middle or UpperMember ofthe Prehodavci Formation. Both contacts are sharp erosional urfaces. The erosional surface between Lower and Middle Member is straight,while the contact of Lower and Upper Member is irregular and cuts up to 1 m deep into white nodular limestone of the Lower Member. 
Age.-The common pre ence of the plankticforaminifers , protoglobigerinid , in the bioclastic limestone with Fe-Mn nodule suggests a Middle Jura ic age, most probably Bajocian to Bathonian (cf. Caron & Homewood 1983, Tappan & Loeblich 1988, Da rling et al. 1997) for the lower part of the Lower Member. The bioclastic limestone is conformably overlain by white nodular limestone, thus according to the stratigraphic po ition, a Callovian age is a sumed for the white nodular limestone. At Ravni Laz ( ection Rl , Fig. 3.2) oolitic limestone is intercalated between bioclastic lim stone and white nodular limestone. This facie i most probably latest Bathonian and l or early Callovian. 
Bioclastic limestone with Fe-Mn nodules. 

The bioclastic limestone with Fe-M n nodule makes up th lowermost part ofthe Lower Member and is present in all of the inve tigated ections,with the exception of section TV5 in Triglav Lake Valley. Bioclastic limestone unconformably overlie an irregular di continuity surface developed on topofearly Lower Jurassic platform limestone (see Figs. 3.16, 3.17,3.18) and displays significant thickness variations, from few dm to a maximum of 3 m a t places. 
Facies description.-The lower pa rt of the me mber is represented by red , bedded (up to 10 cm),at place nodular wackestone to packstone (lal-ely grainstone) that exhibits paralle l a nd indistinct cros -lamination (Fig. 3.19). 
Fig. 3.19 Lower Member of the Pre h odavci Formation: red bioclastic limestone with Fe-Mn nodules. Triglav Lakes Valley, section TV4. 
Be dding surfaces a re at places marked by Fe-Mn oxides and represent di continuity urfaces. The limestone is composed ofvarious bioclasts and intraclasts (Fig. 3.20). 
, 
'-t> .,. 
... , G' J 
.. .
! 
... 
:,.,. 
-i> 
'f • 
-' " .. , ,'... t 
\.. "-_ ... 
... ---.., 
-. '." 
J-. -, .. 





-'.-.... .; 
.. .'--. 
Fig. 3.20 Lower Member of th e Prehodavc i Formation: bioclastic lime tone with echinoderm rragments, gastropods and filam e nts (section TV4) . Scale bar is I mm long. 
Bioclasts are fragments of echinoderms, be nthic foraminifers (Lenticuiina sp.), ga tropod protoconchs,juvenile ammonites, disarticulated valves of thin-shelled bivalves, and algae fragments. Planktic foraminifers (protoglobigerinids) OCCllr in th e mid-dl pa rt of the bioclastic faci s (Fig. 3.21). 
lntracla ts a re fragments of limestones composed exclusively of sparite crystals a nd fragmentsof biocla tic limestones with the same compo ition as the host rock. In places, the limestone is com

3 Stratigraphy 
Fig. 3.21 Lower Member of the Pr hodavci Formation: bioclastic limestone with echinoderm fragments and planktic foraminifers (section R1 ). ca le bar is 1 mm long. 
posed excl usively of bored echinoderm fragments cemented by yn taxial cement (Fig. 3.22) . 
Fig. 3.22 Lower Member of the Prehodavci Formation: grainstone with echinoderm fragments and a completely Fe-Mn incrusted intraclasts (section TV). cale bar is 1 mm long. 
The distinct feature of the bioclastic limestone is a high abundance of Fe-Mn oxide that occur in different forms: 
• 	
as cryptocrystaJlin e aggregate forming irregular patche within the micritic matrix, 

• 	
as coatings of bioclasts a nd fragments of spariti c limesto ne . ually F -Mn oxides occur on the bored urface of bioclasts and fragmentswhere they represent fillings of very small, straight and branching microboring , usually 


attributed to th e cyanobacteria and fungi (cf.Bogg 1992, Martire 1996). At place al 0 the interior of the biocla ts is thoroughly mineralized (Fig. 3.23) . 
• 	
as individual Fe-Mn nodules (up to 10 cm in the diameter) (Fig. 3.24) 

• 	
individual thin crusts within bioclastic limestones (Fig. 3.25) 

• 	
as dis olution residues along stylo lite 


Fig. 3.23 Lower Member of the Prehodavci Formation: Fe-Mn in cru ted echinoderm fragments (section TV).Scale bar is 0,5 mm long. 
Fig. 3.24 Fe-Mn nodules in the Lower Member of the Prehodavci Formation, Triglav Lakes Valley. Photo Rafae l Marn. 
p-section the wackestone-packstone grades into thi k (up to 40 cm) bedded light r d wackestone. Generally thi lime tone i similar in composition to the limestone of the lower part of the Lower Member, but pelagic foraminifers, filaments and calcined radiolarians are more abundant, is devoid ofFe-Mn oxides, and contains pyrite grains as well. 
t Ravni Laz (section Rl , Fig. 3.2) the lower part of the Lower Member ends with a 40 cm thick 

3 Stratigraphy 
Fig. 3.25 Lowe r Me mb r of the Pre hodavci Formation: Fe-Mn crUSl wilhin the bioclas tic lime tone with echinoderm fragments, gaslropods and benthic foraminifer (seclion TV4). cale bar i 1 mm long. 
package composed of pack tone to wackestone with echinoderm fragments, belemnites, and rare planktic foraminifers, calcified radiolarians and filaments. 
Depositional environment.-The red nodular bioclastic lime tone is a typical de posit of an isolated pelagic plateau (cf. Martire 1992, 1996). odula r bedding, parallel , indistinct cross-lamination, and composition of the lime tone indicate a depositionin a pelagic high-energy environment. Abundant Fe-Mn oxide pre ent in this facies suggest extremelyreduced edimentation rates due to the trong bottom-curents that were sweeping ocean floor and thus prevented high sediment accumulation (Martire1992, 1996) . The sedimentation reached minimum with the formation ofthe di tinct level with concentrated Fe-Mn nodules. 
Oolitic limestone 

Oolitic limestone i only present at the Ravni Laz (section Rl , Fig. 3.2) where it conformablyoverlie th red bioclastic limestone with Fe-Mn nodules. 
Facies description.-This facies consists of three,10 to 30 cm thick, horizontally laminated beds of grainstone and packstone composed almo t exclu
ively of partly or completely micritized ooid (Fig.3.26) . Other grains are echinoderm fragment,bivalve fragments, and be nthic foraminifer. The uppermost bed of th e ooliti c facies represents transitional facies into overlying light gray white nodular limestone d escribed b low. In the upper part ofthi bed the filaments predominate while ooids become scarce and finall y absent. 
Fig. 3.26 Lower Member of the Prehodavci Formation : packsto ne with ooids a nd p loids ( ection Rl ). Scale bar is 1 mm long. 
Depositional environment.-Beds of oolitic limestone occur within a typical condensed pelagic platform facies a nd are allochthonous gravity di placeddeposits ( ee discu ion in chapter 4.4). 

Light gray nodular limestone 
A light gray nodular limestone is present in the Triglav Lakes Valley (sections TVI-TV5, Fig. 3.1), at Ravni Laz ( ection Rl , Fig. 3.2), and at Cisti Vrh. 
In the Triglav Lakes Valley the gray nodular limestone conformably overlies red bioclastic limestones with Fe-Mn nodules. The lower boundary is gradual while the upper boundary of this facies is sharp and irregular and ma rked by an erosional surface. The thickness ofgray limestone varie from 6 to 10 m. At Ravni Laz, the light gray nodular limestone conformably overlies oolitic limestone . Here the nodular lime tone is only I m thick. 
Facies description.-The facies is characterized by a light gray packstone (rarely wackestone) and exhibits indi tinct nodular bedding. At places, the nodular bedding is clearly visible (Fig. 3.27). 
Bedding surfaces are marked by thin greenclay films. Bed thickness is 3 to 5 cm rarely 10 cm. The packstone i compo ed mainly ofdisarticulated valves of thi n-shelled bivalves (Bositra sp.) a nd calcifi ed radiolaria ns (Fig. 3.28). Othe r grains a re aptychi, benthic foraminifers, echinoderm fragments,juvenile ammonites, gastropod protoconchs and pellets. In the lower part of the limestone protoglobigerinid a re prese nt. At places al 0 ammonite moulds are present, howeve r, they are poorly pre
erved and do not aid in age determination. Rarely,nodules ofwackestone composed exclusively ofcalci

3 StraligmIJ/t), 
Fig. 3 .27 Lower Me mber of the Pre h o d avc i Fo rmatio n : li gh t gray nodular limestone . T ri g lav La kes Va ll ey. Ph oto Rafae l Ma rn. 

£led radio larians occur. They show ellipsoidal hape and sha rp a nd a t pl aces also tra nsiti o nal bo undari es with th e ma tri x. The very distin ct features of th ese facies a re up to few cm thick concentratio ns of pyrite (Fig. 3.29). 
Depositional environment.-The no dula r graylime to ne re prese n ts typi cal d e posit of a n isolated pelagic plateau as evide nced by pre e nce of mainly pelagic bioclasts (radio la rians, ammonites, fil am e n ts and pl a nktic fo ra minife rs) a nd be n thos (fo raminife rs a nd echino d e rms) whil e ha llow-wate r e le me nts a re comple te ly mi ss in g . The indistin c t nodula r bedding and abse nce ofFe-Mn oxides suggest lowe re ne rgy current regimes compared to th e underlyi ng bi oclastic limestone with Fe-Mn no dules. The ho ri-
Fig. 3.28 Lowe r Me mber of th e Preh odavci Fo rmatio n : light gray nodular lim esto ne with ca lcified radi o laria n moulds a nd filaments (sectio n TV2). cale ba r i 1 mm lo ng. 
Fig. 3.29 Lower Mem ber of th e Prehodavci Formation: pyri te concre tio ns in the lig h t nodular limesto ne (sectio n TV2). Scale ba r i 1 mm lo ng. 
zon with we ll-d evelo ped nodular be dding sugges t th at pulsa ting curre nts allowed micrite accumulatio n fo llowed by re peated phases of ceme n ta tio n , bio turbatio n a nd curren t reworkjng (Ma rtire 1996) . The distinct, up to few cm la rge concentratio ns o f pyrite indicate reducin g e nviro nment during earlydiagene is. 
MIDDLE MEMBER OF THE PREHODAVCI FORMATIO 
The Middle Me mbe r of t he P reho d avc i Fo rma ti o n i pre e nt o nl y in the Luznica La ke (sec ti o n L1,Fig. 3.2). It i a be dde d red ma rl y mudsto ne that disco n fo rma bl y ove rli es the red bi o cl as ti c limesto ne with Fe-Mn no dules o f t he Lowe r Me mbe r. 

3 SlratigralJhy 
The marly limestone is overlain di conformably by Kimmeridgia n red nodular lime tone ofthe UpperMember of the Prehodavci Formation. 
Description offacies.-The red ma rly mudstone (rarely wackestone) is thin, evenly-bedded (bed thickness is up to 7 em), composed of pl a nktic foraminifers (protoglobigerinids), calcified radiolarians, be nthic foraminifers, and echinoderm fragments (Fig. 3.30). The matrix is micrite with a small amount of terrigenous silt-sized micas. 
Fig. 3.30 Middle Member of the Prehodavci Formation: mudstone with calcifi ed radiolarian moulds (sectio n Ll ).Scale bar is 1 mm long. 
Age.-On the basis of the stratigraphic position only a gene ral age assignment, between the Callovian to the Kimme ridgia n, i po ible. 
Depositional enmronment.-The ma rly mud tone was de posited in a lower hydrodynamic current regime, which permitted depositi o n ofeve nly bedded mud-supported sedime n ts. Absence ofcementation, and he nce offirm ground burrowi ng, hinde red formation of nodular tructure (cf. Martire 1996). The pre e nce ofth e ilt-sized micas indicate a n increased input of terrigenous material at that time . 
UPPER MEMBER OF THE PREHODAVCl FORMATION 
The Upper Member of the Pr h d avc i Formation was investigated in the Triglav La kes Valley (sections TV1, 2, 3, 5, Fig. 3.1), at Ravni Laz (sectio n R1, Fig. 3.2), Luznica La ke ( ection Ll, Fig. 3.2) a nd at Cisti Vrh a nd Va na Skali. The pp r Me mbe r unconformably overlies the Lower or Middle Me mbe r of the Prehodavci Formation (Fig. 3.31). The contact i irregular and cuts up to 1 m deep into the Lower Member. 
The Upper Member i a red nodular limesto ne of Ammonitico Rosso type. The exact thickness of this member could not be d etermined since the upper boundary is not visible in the outcrops, but can be e timated to a t least 2.5 m at Triglav La kes Valley, 3.5 m at Ravni Laz, and at least 6 m at Luznica La ke. 
Facies description and lateral variations.-This facies is characterized by red olor and a marked nodular a pect in outcrop because ofthe color contrast betwee n the pink nodules and darker matrix (Figs. 3.32, 3.33). odules a re up to 10 em large and are mai nly intraclasts, ammonite moulds, a nd early diagenetic nodules. 
Fig. 3.31 Irregu lar contact (arrow) be lween Lower and 
pper Member of the Prehodavci Formation (Triglav Lakes Valley, seclion TV 1) . Photo Rafael Ma rn. 

3 Stratigraphy 
Fig. 3.32 Upper Member of the Prehodavci Formation: red nodular limeston e: (Triglav Lake Valley, ection TVl). Photo Rafael Marn. 
Fig. 3.33 Upper Member of the Prehodavci Formation: red nodular limeston e: (Triglav La ke Valley sectio n TV 1). Photo Rafael Marn. 

The intraclasts consist of wacke tone to pack-stone with disarticulated valve of thin-shelled bivalve (Bo ilra sp.), calcified radiolarians, fragme nts of ammonite shell , echinoderm fragments,juvenile ammonites, gastropod protoconch , benthic foraminifers (LenlicuLina p.), and planktic foramini£ rs (protoglobigerinids) (Fig. 3.34). The intraclasts show sharp boundaries with the surrounding matrix. In the upper part of the me mbe r, they are also bored , borings are coated with the Fe-Mn cru t (Fig. 3.35). 
Fig. 3.34 Upper Member of the Prehodavci Formation: Fig. 3.35 pper Member of the Pre hodavci Formation: nodules of wackestone with filaments and calcified ra-Fe-Mn incru ted intraclasts in a filament-rich pack tone diolarian moulds embedded in a filament-rich packstone matrix ( ction TV). Scale bar i 1 mm long.( eClionTVl ) . Scale bar is J mm long. 
3 Stml igraphy 
Fig.3.36 Upper Memberofthe Prehodavci Formation: ammonite mould in the red nodular limesLOne: (Triglav Lakes Valley, seClion TVl) . Photo Rafael Marn. 

The ammonite moulds are frequent and are generally coated with Fe-Mn oxide. Usually they are broken and abraded, and intact specimens are rare (Fig. 3.36). 
The early diagenetic nodules have the same composition as intraclasts but show transitional boundaries with the surrounding matrix. 
The described nodules are embedded in a darker, at places, more clay-rich matrix. The matrix consists of packstone with fragment of bivalves (Bosilra p.) and rare echinoderm fragments. Bivalve fragments are flat, aligned parallel to the edge of nodule, and form fitted fabric (Fig. 3.37). 
Fig. 3.37 pper Member of the Pre hodavci Formation: nodules ofwackestones with liIaments and calcified radiolarian moulds embedded in a filament-rich matrix forming filled rabric ( ection TV1) . Scale bar is 1 mm long. 
Stylolite are common. They occur within the matrix and at the boundary between ma trix and nodules. In Ravni Laz ( ectionRl, Fig. 3.2) a 70 em thick package of packstone with bioclasts is present in the upper part ofthe section. Packsto ne contains abundant Saccocoma sp. , bele mnites, echinoderm fragments, aptychi, calcified radiolarians, and intraclasts (Fig. 3.38) . 
Fig. 3.38 Upper Member of the Prehodavci Formation: pack tone with Sa ccocorna fragments and aptychi (Vas na 
kali area). ale bar is I mm long. 
At Cisti Vrh a nd Vas na Skali Upper M mber of the Prehodavci Formation is composed of nodules that are wackestones with abundant Saccoco'l1la sp. fragments, aptychi , a nd calcified radiolarians. 

3 Straligra/Jhy 
Rarely, fragments ofechinode rms and detritic grain ofqua rtz are pre e nt. These nodules are embedded in a clay rich pa kstone matrix with abundant Saeeoeomas p . (Fig. 3.39), and rare calcified radiolarians and oth r echinoderm fragme nts. 
Fig. 3.39 pper Member of the Prehodavci Formation: clay-rich limestone with Saccoc01na (Vas na kali). Scale bar is J mm long. 
Age.-The ammonite moulds a re quite frequent 111 thi facies, howeve r they a re u ually not well-pre erved a nd very ha rd to extract from the rock. 

alope k (1933) found the followin g a mmonites: Phylloeeras sp. , H oleoj)hylloeeras? sp., a nd Perisphineles sp. a nd de termined a La te Jurassic age for the red nodular limestones. This age a ignment was late r improv d by Ra movs (1975) who fo und th e follow-in g ammonites: EnasjJidoceras sp., Gregoryeeras sp., Lytoeems sp., Paraspidoeeras sp., a nd Sowerbyeeras sp., and de termined a n Oxfordia n a nd Kimme ridgian age. On the basic geological map ofYugo lavia, these red lime tone were broadly as ign ed to th e Late Jura sic (Bu er 1986) . According to the tratigraphic correlation with the Ro 0 Ammonitico Formation in the Trento Plateau, th e pper Member of the Prehodavc i Formation corresponds to the Kim-m ridgian to Tithonian Upper Membe r ofthe Ro 0 Ammonitico Formation. 
A Late Kimme ridgia n to Ear!>' Tithonian agefor the nodular limestones of the i ti Vrh and Vas na Skali was assumed on the basi of pre ence of Saeeocoma sp. (according to artorio & Venturini 1988) . 
The Kimme ridgia n to early Tithonia n age of th e pper Me mbe r of the Prehodavci Forma tion is thu mo t probable. 
Depositional environment.-The red nodular limestone of Ammonitico Ro " o type represents 
conde n ed edimentation and is typi cal of sedime ntation o n isolated p elagic pl ateaus. Various nodules (intracl asts, earl y diagenetic nodules and ammonite moulds) indicate the influe nce of pul ating bo ttom-currents that allowed micrite accumulation, followed by long and re peated phases of ce me nta tion , bioturbation and current reworking (Martire 1996) . The highe r clay content in the matrix i most probably a s condary enrichment due to the pressure dissolutio n of micrite (cf. Clari & Ma rtire 1996). 
3.l.3 BOVEe TROUGH 
The Bovec Trough was a -S trending small tra nsve rse Jura sic basin located in th we te rn pa rt of the Julian appe (for d e finition see ch a pte r 1.4.3). It comprises the a rea of Mt. Ma ngart saddle (Travnik tructural unit) a nd Bav"ica a rea (Cousin 1981). The Bovec Troug h formed afte r the di sintegration and drowning of the Julia n Carbonate Platform. The di stinct feature of the Bovec Troug h i that sedimentation was basinal from the Middle Jurassic. Th Lowe rJurassic platform lime tone of the Julia n Carbonate Pla tform are overlain by la te Plie nsbachia n distal shelflimestones (Sedlo Formation) foil wed by the de position of th black hales (Skri le Fo rmatio n). The Middle a nd pperJurassic de po its of the Bovec Troug h are cha racte ri zed by pelagic iliceou edimentation a nd abundant carbonate g ravity-flow de posits (Travnik Formation).The be t-exposed sections of the Bovec Trough crop o ut in the Travnik structural unit o n the Mt. Ma ngart saddle (see Figs. 2.7,2.8) where 5 section s (MAl to 5) (Figs. 3.3, 3.4) were inves tigated . The most compl te ection is the MAl section (Fig. 3.3) , recording the evolution from the Early Jurassic to the Early retaceous. The MAl section ha alread y been d esc ribed (Sm uc & Gorican 2005), under the n a me Ma ngart sectio n . In this volume the litho tratigraphic units are fo rmally de cribed a nd detailed facie description a re also g iven. 
SEDLO FORMA TION 
Typesection.-MAl (Fig. 3.3, for location see Fig. 2.7) . The Sedlo Formation is nam ed after th Mt. Ma ngart saddle (sedlo is th e Slovenian word for saddle). The Sedlo Formation was inves tigated in both the MAl and MA2 sections (Fig. 3.3) . In th e MAl section , the Sedlo Formation is completely accessible while in the 

3 StratigmlJhy 
MA2 section only the upper part ofthe formation is vi ible. The Sedlo Formation corresponds to Unit 2 of Smuc & Gorican (2005). The development of the Sedlo Formation in the MA2 section is newly explained here. 
Short Definition.-The Sedlo Formation lithology ranges from wackestone to packstone rich in echinoderms,juvenile ammonite, sponge spicules and foraminifers. In the upper part ofthe formation rudstone i intercalated with packstone containing echinode rms. The thickne ofthe edlo Formation at the type locality is 27 m. 
The S dlo Formation conformably overlies the Lower Jurassic platform limestone. The boundary he re is sharp and well disce rnible upon clo e inspection, because of the facie change, but indistinct in field morphology. However, the limestones of the Sedlo Formation a re clearly distinguishedfrom the underlying shallow water grain tones and wackestones (see chapter 3.1.1) due to the marked difD re nce in the texture of limestone (they are much more fine-grained). The Sedlo Formation i unconformably overlain by the lower (to middle?)Toarcian Skrile Forma tion. This discontinuity surface is marked with a Fe-Mn hardground on the top of the Sedlo Formation. The Pliensbachian ageof thi formation is constrained by foraminifers,combined with radiolarian da ting from overlying
trata. 

Prevwuswork.-The bioclastic lime tone ofMali Mangart was first described by Cou in (1981). He found that the shallow-water lower LowerJurassic " p eudo-oolitic" limestones are overlain by 20 m 
Fig. 3.40 Sedlo Formation: massive and indi tinctly bedded bioclastic lim e LOne (Travnik structural unit of the Ml. Man gan saddle, ection MAl). The section is in overturned position. Line in the upper left corner of the photo is j m lo ng. Photo Rafae l Marn. 
of biomicritic lime tones with numerou spongespicule, foraminifers (Agerina marlana (Farinacci)(by ou in (1981) determined a Vidalina martana (Farinacci», Nodosariasp.), echinoderm debri ,andjuvenile ammonites. In the upper part ofthis uccession he found calcareous microbreccias composedofabundant echinoderm fragments and foraminifer (Agerina marlana (Farinacci), Involutina liassica Oones), Nodosariasp ., Lenticulinasp.). According to this association he dated thi limestone a middle Lia sic.Jurkovsek eta!' (1990) de cribed the uppermo t pa rt of this lime tone; they found foraminifer (Age-rina martana (Farinacci) (by Jurkovsek et a!. (1990) determined as Ophthalmidium leischneri (Kristian-Tollmann», radiolarian moulds, spongespicules, echinoderm fragments and juvenile ammonite . On the ba is of the presence of Agerina martana (Farinacci) they assigned a Liassic age to this limestone. 
Facies description.-The lower part of the formation con i t of light browni h-gray, massive to in-di tinctly bedded (Fig. 3.40), and at place nodular,biocla tic wackestone to packstone . Bed thickness is up to 10 cm. 
The limestone is composed ofsponge spicules,echinoderm fragments, locally abundant juvenileammonites, and benthic foraminifers (Textulariidae, Lenticulina sp., Agerina martana (Farinacci»(Fig. 3.41) . Ostracod and brachiopod shells are rare. Glauconite is present as infilling in chambers offoraminifers or a small individual grain . Pellet are abundant in place. 

3 Stratigraphy 
Fig. 3.41 Se dlo Formation: bioclastic limestone with juvenile ammonites, sponge spicules, and echinoderm 
fragm e nts (section MAl). Scale bar is 1 mm long. 
The upper part of the formation is characterized by a distinctive greenish rudstone-packstoneand red siliceous limestone (Fig. 3.42). 
In the MAl section (Fig. 3.3) this level is characterized by 1 to 1.8 m thick rudstone-packstonepackage that is overlain by red siliceous packstone/wackestone, while at the MA2 section (Fig. 3.3),the rudstone package is thicker (up to 10 m) and alternates with red siliceous packstone/ wackestone. The upper part ofthe formation is more argillaceousand darker in color than the lower part, and can therefore be readily distinguished in the field. 
The rudstone and packstone are thin-bedded, poorly sorted, moderately to densely packed, and normally graded. Elongate grains are oriented parallel to the bedding. The prevalent grain are fragments of echinoderms and diverse intraclasts. Echinoderm grains show evidence of mechanical breakage and abrasion. Intraclasts are fragmentsof underlying lithologies represented by clasts of biocla tic wackestones with benthic foraminifers (Agmna manana), sponge spicules,juvenile ammonites, and rare echinoderms, clasts of well-sorted grain tones with peloids, micritized ooids, and fragments of bivalves, and al 0 clasts of mudstones,and peloidal mudstones (Fig. 3.43). Other grainsinclude foraminifers (Lenticuiinasp. , Agmna manana (Farinacci)), bivalve and brachiopod fragmen ts,and peloids. The matrix is micrite and microsparite.Glauconite, chlorite and pyrite grains also occur within the matrix. 

Fig. 3.42 Upper pan of the Sedlo Formation: greenishrudstone -packstone and red siliceous limestone (Travnikstructural unit of th e Mt. Mangan saddle, section MAl).Section is in overturned po ition . Scale bar is 1 m long. Photo Rafael Marn. 
Fig. 3.43 Sedlo Formation: rudstone with echinoderm fragments, and intraclasts of pe loidal pac kSlones, and mudstones (section MAl). 
The red siliceous pack tone/ wackestone is bedded, with beds of up to 10 cm thick and slightly 

3 SlraligratJiI), 
nodular. It consists of abunda n t, pa rtly calcified , spo nge spi cules and radiolaria ns (Fig. 3.44). 
Fig. 3.44 Sedlo Formatio n: uppermost siliceous limesto ne with sponge spicules and radio larian m o ulds (sec tion MA l ). Scale ba r is I mm long. 
Othe r grains include ra re echinode rm fragme nts that are no t pre e nt in the topmost beds oftile fo rmatio n. The matrix is partially impregnated by Fe-Mn oxides. T he siliceous packstone/ wackestone contai ns Fe-Mn nodules up to 3cm in size. T hey occur th rougho ut th e uppermost l.5 m ofth e fo rmatio n. At the type sectio n , MAl (Fig. 3.3) the fo rmatio n is capped by a 25 cm thick bed composed exclusively of Fe-Mn nodules (Fig. 3.45). The nodules consist main ly ofquartz and pyrolusite, with minor amo unts ofcrypto melane, todorokite a nd goethite; th e MnO content reaches 55 % (Jurkovsek et al. 1990). This bed is no t prese nt in tile MA2 sectio n. 
Age.-The commo n presence ofAgerina mariana (Farinacci) (according to the biozonal sche me of Chiocchini et al. (1994» in th e lower part of th e forma tio n suggests a Pli e nsbachia n age. Because the ove rlying Skril e Formatio n is early T oarcia n in age (Co ri can e t al. 2003), the Fe-Mn hardground at the to p ofth e Sedl o Formatio n approximately correspo nds to th e Plie nsbac hia n/ T oarcia n bo undary.
Depositional enmronment.-The lower pa rt of th e forma tio n i con tructed of bioclastic wackesto ne and packsto nes that were de posited in a low e ne rgy e nviro nme n t. The prese nce of o pe n-ma rin e bi ota (spo nge picul es a nd juvenil e ammonite) and the abse nce of shallow-wa te r ele me n ts suggest a d eeper d epositi o nal e nviro nme n t, most probably th a t of a distal shelf (cf. Elmi 1990 ). 
Rudstones a nd packs to nes in th e uppe r part of th e fo rmatio n exhibit no rma] g rading, relatively de nse packing a nd pa rallel o rie n tatio n of the elo n-gate grains a nd are interpre ted as gravity-flow de po its. T he pre e nce of completely lithified lithoclasts of olde r trata indicates exhumatio n of unde rlyi ng litho logies by syn sedimentary exte nsio nal tecto ni cs tha t p roduced unstable lo pe, uncove red older rocks a nd e nabled e ro io n. The exhumed rocks were additionally erod ed due to mechanical abra io n by the grain-loaded tu rbule n t wa ter (cf. Di Stefano & Mindsze n ty 2000, Di Stefano e t al. 2002). 
In the wackestone a nd packstones with ferroma n gan e e n o dules a bove the resedime n ted limesto nes, spo nge spicules and radiola ria ns prevai l and be nthic calca reous o rganisms become scarce to abse nt. Fe rro-m a ngan e e nodules provide evide nce fo r extrem ely reduced sedime n tatio n rates 
Fig. 3.45 Sedlo Formatio n : Fe-Mn nodules in th e uppermo t part of formation. Section is in overturned posi tio n (Travn ik structura l u n it of th e Mt. Ma n gan saddle, section MA l ). 

3 SlraligralJhy 
of this pelagic limesto ne. The edime n tatio n rate reached its minimum with th e fo rmatio n of th e Fe-Mn ha rdg ro und. 
SKRlLE FORMATIO 

Type sectWn.-MAl (Fig. 3.3 fo r locatio n ee Fig. 2.7). The Skril e Fo rmatio n is na med after the old name tha t local people used fo r the locality of the lower pa rt of th e MA 1 sectio n (skrile is the old Slove nian word for hale). An additio nal ectio n whe re thi form atio n cro ps o ut is the MA2 ectio n (Fig. 3.3). However th e o utcro p is mostly covered and o nly th e lowe rmost part ofthe fo rm atio n can be studied . The Skrile Forma tio n correspo nds to nit 3 of Smuc & Go riea n (2005).
Short Definition. -T he Skrile Fo rmation is a 
27.5 m thick succession of organic a nd ma nganeserich calcareous sha les with interbedded dark g ray 
Fig. 3.46 Skrile Formalion (arrow) (Travn ik lructu ral u n il of th e Ml. Mangan saddle, section MA l ). ectio n i in ove nurned posilio n . T h e visible o Ulcrop of the Skri le Formation is approximately 20 m lo n g. Ph oto Rafael Marn . 
iliceou lime to ne. It unconformably ove rlie the Sedlo Fo rma tio n, a nd i unconfo rmably ove rlain by the Travnik Fo rmatio n (Fig. 3.46). The earl y and possibly middle Toarcia n age of this fo rmatio n wa constrained with radiola ri a ns (Go riean et al. 2003).
Previous work.-Cousin (1981) first me ntioned bl ack calcareous shales and brown ma rls with rare inte rcala tio ns of gray limes to n s with radiolaria ns a t Mt. Ma ngart addle. This a utho r estima ted 10 m of thickne s fo r these de posits. J e nkyns (1988) provided a m o re d etaile d d escriptio n o f black shale . H e de cribed 26.5 m of o rgani c-ri ch bl ack la mina ted calca reous hales, m a nganife rrou a t the ba e, and brown ma rls ri ch in polle n , that are in te rb dded with limes to ne Witll radio la ria ns. In shales, J nkyns (1988) ide ntified quartz, smectite, illite, and d e te rmined tha t o rganic-ca rbon values ra ng betw e n 0.48 a nd 1.7 %.J e nkyns (1988) inter-pre ted these de posits as a product of th e T oarcian Oceanic Anoxic Event. Later these d e posits were al 0 investigated by Jurkovse k et al. (1990), who ide n tified qua rtz, calcite, illi te a nd pyrolusite in th e ma nganife rrous shales. 
Facies description.-The fo rmatio n starts with a 40 cm thick bed of da rk gray organic-ri ch , wackestone/ packsto ne with echinode rms, calcifi ed radi olaria n , and spo nge spicule. The ma trix is mi crosparite. 
This wackes to ne / packsto ne is ove rlain by a 10 cm thick bed ofvery poorly-sorted rudsto ne. ormal grading is o bserved within this bed . The rudsto ne is composed mainly of echinode rm fragme n ts and intraclasts. In traclasts a re mudstone and peloidal packsto ne. Rare fo raminife rs, fragme n ts of bivalves and gastropods, glauconite, and phospha te g rain s are al 0 prese n t. The rudsto ne is ceme n ted by drusy and yntaxial ce me nt. 
Above the rudstone, black la mina ted calca reous o rganic-rich h a les with interbedded bl ack siliceous limestone a re present (Fig. 3.47). In the uppe r pa rt of the fo rma tio n, the hale a re brown. The ha le contain quartz, mectite a nd illite, a nd Mn oxide Oe nkyns 1988, Jurkov· e k et al. 1990).The TOC va lue ra nge be twee n 0.48 a nd 1.7 %, and ma nganese content is hig h (up to 9.27 %) in the basal po rtio n a nd decreases (1.12 % o r less) upsectio n Oe nkyns 1988). 
The sili ceous limes to n e inte rcala ted within th e shales varies fro m packstone to mudsto ne. Bed thickn e s is up to 15 cm. In the lowe r pa rt of the fo rm atio n, beds a re abundant and a re mainly packsto nes a nd wac ke to nes, whil t upward, the beds become rare and are p redo minan tly wacke to nes to 

3 Straligra/Jhy 
mudstones. In the lower part of the formation, the siliceous limestone shows both normal and inverse grading, parallel and ripple cross-lamination (Ta-dBouma seq uences), while up ection, only indi tinct parallel lamination is present (Td Bouma equence).The grai n-ta-matrix ratio and the mean size of radiolarian decrea e upward. In the uppermost lime-
tone beds, the grain-ta-matrix proportion is againhigh (packstone/ wackestone laminae). The limestone is composed mainly of radiolarians, spongespicules (only in the lowermo t part of the formation), intraclasts oflime mudstone (in the lowermost part of the formation only), and phosphate grains(Fig. 3.48) . Authigenic quartz and pyrite occur and are especially abundant in wackestone, while they are less common in the pack tone beds. The matrix is micrite with a high organic matter conte nt. 
Fig. 3.4 Skrile Formation: normally graded siliceous limestone with radiolarian and mudchip ( eClion MAl).Scale bar is 1 mm long. 
Fig. 3.47 Skrile Formation : shales with interbedded black 
iliceous limestone. Section is in overturned position(Travn i k structu ral unit ofthe Mt. Mangan sadd le, section MAl). Photo Rafael Marn. 
The formation ends with 0.90 m oflight green,thinly-bedded, laminated, mudstone with Mn dendrites. Echinod rms, ostracods, foraminifers and calcified radiolarians are very rare. Pyrite, limonite, quartz and glauconite are present. The limestone i bored. 
DepositUmalerwironment. -The Skrile Formation records a high input of terrigenous clayey material. Black organic-rich shales in the lower part of the formation were depo ited during the early Toarcian Oceanic Anoxic Event, as suggested by Jenkyns(1988) and confirmed with radiolarian dating(Corican et al 2003). 
The limestone in the lowermost part of the formation is interpreted as hemipelagic limestone and indicates an increa e in edimentation rate following the formation of the Fe-Mn crust. Sedimentary
tructures and the composition ofthe rud tone bed are very imilar to that in the rudstone beds of the upper part of the Sedlo Formation and suggest a deposition by a high-density gravity-flow. 
The edimentary tructure found in the siliceous limestone intercalated within shales are typicalof low -density turbidites (e.g. Piper & Stow 1991). The nature of re edimented grain (only pelagicfauna) indicate redepo ition ofmaterial only within the sedimentary basin. 
TRAVNIK FORMATIO 
Type sernon.-MAl (Fig.3.3, for location see Fig. 2.7) . The Travnik Formation is named after Travnik hill where the type ection i located. Additional ection where thi formation was tudied are the MA3 and MA4 sections (Figs. 3.4, 3.49). The Travnik For


3 Slraligra/Jhy 
matio n orre po nds to nit 4 of Smuc & Corica n (2005). The de criptio n of th e Travnik Fo rmatio n in th e MA3 a nd MA4 sectio ns is newly pre e nted h reo 
Definition.-The Travnik Fo rm a tio n is a 77 to 120 m thi ck succe io n ofche rts, he rty limesto nes and carbo na te gravity-flo w de posits. On the basis 
o f diffe re nt lithology, structur and compositio n of resedimented carbo na tes, th e T ravnik Fo rmation is subdivided in to 4 me mbers. The Travnik Fo rmatio n unconformably ove rli es the krile Fo rmation. The base o f the fo rmatio n i diachronuo us. t th e MAl s ctio n (Fig. 3.3), th e ba e of the for ma tio n is late Baj ocia n o r early Batho ni an ('muc & Corica n 2005), whil e at th e MA3 a nd MA4 ectio n (Fig. 3.4),th e lowe r part ofth e form ation is arly-middle Baj o-cia n in age. The Travnik Fo rm atio n is confo rm ably overlain by pelagic, Bia ncone-typ e lime to ne. T he maximum range o f this fo rmatio n is thus lowe r-middl e Baj ocia n to lower Titho nia n. T he ages of individual me mbe r are given below in th e d esc ripti o n of the member o f the Travnik Fo rmatio n. 
PreviOllS research.-Resedime n ted limes to n s and sili ceou rocks a t Mt. Ma ngart saddle were recogni zed by Cousin (1 981) a nd Ju rkovse k e t al. (1990). From the T ravnik hill Cousin (1981) described he te rogeneous upper Dogger to MaIm deposits. According to Cousin (1981), th ese de posits consist of radi ola ria n cherts, bi o micritic limesto nes with radi olaria ns and spo nge spi cul ,calca re nites and carbo na te breccias . Calca re nites a nd b reccias con ta in abunda n t ooid , in traclas ts, echinod erm de b ris, foraminife r (P rotopeneroplis striata Weynsche nk, Endothyra sp., ummolocolina sp., Trocholina ? sp., Meyendorfina p. ) a nd fila me n ts. The upper part con tain s red radi olaria n ch erts tha t alternate with red n odular limes to nes with SaccocO'lna, and white calcareous b reccias (Cousin 1981). Jurkovsek and co-authors (1990) de cribed thin-bedded a nd silicified limesto ne with ooids and interpreted th e m a carbo nate g ravity-flow de posits. Jurkovse k a nd co-autho rs (1990) assumed th ese limesto nes were MaIm in age. 
MEMBER 1 
The Me mber 1 ofth e Travnik Form a tio n rep re e n ts the base of th e fo rmation. T he bas ofMember 1 is la terally di achronuo us a nd variably develo ped . At the MAl sec tio n (Fig. 3.3, th e base of Me mber 1 i defin ed by a package ofglauconitic breccia ove rlyi ng th e di continuity surface, whil e a t the MA3 a nd MA4 sectio n (Fig. 3.4), the lowe r part of Me mbe r 1 is a ho mogeno us mudsto ne with cherts, but the contact with the Skrile Fo rmatio n is not visibl e. Because of this d iffere n ce we described separately th e d epo its of M mber I for the MAl ectio n ver u th e MA3 and MA4 sectio ns. 


Member I at MAl section 
Facies description.-At the MAl sectio n (Fig. 3.3),Me mbe r 1 begins with a 1.3 m thi ck package o f green, up to 25 cm thick beds offin e-grained , poorly-to medium-sorted clast-suppo rted breccia (Fig. 3.50) tha t grad es into a thin-to medium-bedded , coar e to medium-grained calcareni te. 
T he b reccia consists offilame n ts, echinode rms,biva lve fragme nts, foraminifer (Textulariid ae, L enticulina p.), radiolaria n , po nge p icule and 
Fig. 3.50 Member 1 of t h e Travnik Formation: basal breccia (Travnik struClu ra l uni t o f the Ml. Mangan addle, section MA l ). Photo Rafae l Marn. 

3 SlraligmIJ/t), 
Fig. 3.51 Member 1 of the Travnik Formation: breccia with echinoderm fragments, glauconite and abundant li thoclasts of th e bioclastic limestone of the Sedlo Formation, mudstone lilhoclasts and li thocla ts of iliceous limestones of the Skrile Formation ( ection MAl). Scale bar is 1 mm long. 
various lithoclasts (Fig. 3.51). The lithocla ts are the bioclastic wackestone/ mudstone of the underlying
edlo Formation, as well as the light gray mud tone and siliceous packstone/ wacke tone of the Skrile Formation. Glauconite is abundant. The calcarenite exhibits parallel lamination, and elongate grains are aligned parallel to bedding. Ithas the same bioclasts as breccias, but contains more highly evolved glauconite grains (determined according to classification ofOdin & Fullagar 1988) (Fig. 3.52) and it i devoid of lithoclasts. Some of the glauconite grains have a fractured grain surface. 
Fig. 3.52 Me mber 1ofthe Travnik Formation: calcarenite with abundant glauconite grains, radiolarians, phosphategrains and filaments (section MAl). cale bar i 1 mm long. 
The breccia and calcarenite are overlain by thin-bedded gray iliceous pack tone/ wacke tone and dark gray la minated cherts that alternate with medium-bedded ligh t gray homogenous wackestones that contain lenses of chert. The iliceou packstone/wackestone shows parallel, low-angle cro s lamination and wispy, convoluted lamination (Tb-d Bouma sequenc s). Grains are partly calcified radiolarians and rare fragmen ts ofechinoderm ,and phosphate grains. The intercalated wackestone is compo ed of completely calcified radiolarians and rare filaments. Rare, up to 30 cm thick, ooid bearing, beds are inter-bedded in the upper part of the member. 
Age.-On tile basis of radiolarians found in the chert overlying basal glauconitic breccia, Smuc & Goriean (2005) determined the age to be late Bajocian or arly Bathonian. 
Depositional environment.-Sedimentary structures of the basal breccias suggest deposition by gravelly high-density turbidity currents. Different lithoclasts of the Sedlo and Skrile Formations indicate exhumation and partial erosion of underlyingdeposits. The presence ofevolved to highly evolved glauconite in the breccia and calcarenite is indicative oflong-term sediment starvation in the provenance area (Odin & Fullagar 1988, Amorosi 1995). The breccia corresponds to the F5 facies type. The overlying coar e to medium-grained calcarenite were deposited by andy high-density turbidity currents and represents the F7 facies type. Siliceous limestones at the top of the unit were deposited by low-density fine-grained turbidity currents and represent Tb-d Bouma divisions of F9a facies type. 
Member 1 at MA3 and MA4 sections 
Facies description and lateral variation.-Member 1 of the Travnik Formation in the MA3 and MA4 sections (Fig. 3.4) starts with bedded (bed thickness from 5 to 70 cm) homogenous mudstone/wackestone with lense and bed of black replacement chert (Fig. 3.53). 
The lime tone is compo ed of calcified radiolarians, filaments, pyrite, and authigenic quartz(Fig. 3.54). In place the calcified radiolarians predominate.
Beds of medium-grained calcarenite are intercalated. alcarenites are composed of filaments,echinoderm fragments, intraclasts ofmudstone with radiolarian moulds, and glauconite grains. Glauconite occurs as individual grains or impregnates the echinoderm fragments. Phosphate grains, authigenic quartz and benthic foraminifera (Lenliculina
p.) are rare. 

3 StratigmfJlt)1 
Fig. 3.54 Member 1 of th e Travnik Formation: micritic limesto ne with calcified rad iolarian moulds (section MA4). Scale bar is I mm long. 
In th e middle pa rt of th e Me mbe r 1 at th e MA4 sectio n the siliceous pac kstone/ wac kes to ne, ooidal calcare nites, and calca re nites with echinode rm fragme n ts begin to occur. 
The siliceous packsto ne/ wackestone exhibits horizon tal, rippl e-cross la minatio n , a nd convolute laminatio ns (Tb-d Bo uma seque nces), and rarely no rmal grading (Ta Bo uma divisio n ). It is composed of pa rti a lly calcifi ed ra di ola ri a ns, fila me nts a nd rare ly spo nge spi cul es, echinod erm fragme n ts and mud-chips. In pl aces phospha te and pyrite grains a re al 0 prese nt. 
The medium to fin e-grain ed calcare nites are bedded (bed thickn es up to 20 cm ) a nd ma inl y 
Fig. 3.53 Me mber 1 of the Travnik Formation: bedded li mestone with chen (Travni k structu ra l unit of the Mt. Mangan saddl e, section MA4). 
exhibit ho ri zon tal laminatio n (Tb Bo uma divisio n ) while no rmal grading a nd ripple-cross laminatio n occurs rarely (Ta-c Bo uma seque nce). La minatio n is de fin ed by a lte rnatio n of thicke r packsto ne la minae composed mostly of ooids and thinne r la minae where fil a m e n ts p red o mina te. Other grain are pe lo ids, echinod erm frag me n ts, be n thi c fo raminifers (T extula ridae, Lenticu lina sp.), phospha te, and glauconite grains. 
T h e echinode rm calcare nites a re bedded (bed thi ckn ess up to 10 cm ) a nd consist o f g ra instones composed p red o mina n tly o f echino d e rm fragme n ts and ra re gla uconitic a nd phosphate gra in s, and mud-chips (Fig. 3.55) . In places ooids a re also pre e n t. Gra in a re ceme n ted by yn taxial ceme nt. 
The upper pa rt of Me mbe r I is characteri zed by I m thick medium-to fin e-gra ined poorly so rted breccia that grade into a coarse-grai ned calcareni te. Gra ins are lithoclasts of wackestone of th e Sedl o Fo rmatio n , siliceous packsto ne/ wackestone of the Skrile Forma tio n , and clasts of mudsto ne fro m th e lowe rmost pa rt of the Me mbe r 1. O the r grains a re echinode rm fragme n ts, gastropod a nd bivalve fragme n ts and small gla uconitic grains. The matrix of the breccia is packstone to wackestone with ooids and small echinode rm fragme n ts. In the calca re nites ove rlying b reccia lithoclast becom e scarce and ooids tart to pred o minate. Other grains are echinode rm fragme n ts, spo nge spicule a nd be nthic foraminifers . Thi breccia i correla tive with the basal breccia a nd calca re nite a t th e MA l sectio n (Fig. 3.49). 

J Siraligra/Jhy 
Fig. 3.55 Me mbe r 1 o f the Trav nik Fo rma ti o n : ca lcarenites with ec hi noderm fragm e n ts, pho pha te a nd gla uconite gra in s ce me nted by yn tax ial ce me nt (sectio n MA4).Scale bar is 1 m m lo ng. 
Me mber 1 of th e Travnik Formatio n e nds with alte rna tion o f 1 m thick package of previo usly described medium-grai ned calcare nite with ooids a nd up to 2.5 m thick package of siliceous limestone with radiol aria ns. 
Age.-Th early-middle Baj ocia n age (UAZ 3 in Baumgartne r e t al. 1995 a) is constrained by the foll owin g radi ola ria n associa tio n (d e termined by 
S. Go ri ean ): Bernoullius rectispinus Kito, De Weve r, Dan lian & Co rdey, Hexasaturnalis suboblongus (Yao),H suurn rnalsuokai lsozaki & Matsuda, Pamsaturnalis dil)locyclis (Yao), Stichornitm (?) takanoensi Aita, a nd Strialojaponocapsa plicarum (Yao). The radiola ria n 
Fig. 3.56 Me m ber 2 o f the Travnik Fo nnatio n: limc tone I11 cgabed s (arrow). The sectio n is in overturned positi on (Travnik structu ra l unit o f th e Mt. Ma ngan sa d d le , sectio n MA l ). 
ample was fo und 9. 20 m above th e base of the MA4 sectio n (Fig. 3.4). 
Depositional environment.-The ho mogeno us lim to ne with calcified radi ola ria ns is interpreted to be pe ripl atform ooze de posits. iliceous lime-
tones of the middle part o f the m e mbe r were d e po ited by low-d e n sity turbidity c urrents a nd a re Ta-d Bouma seque n ce o f F9a facies typ e. Calc a re nites in whic h ooid a nd echino d e rm predo minate were depo ited from sandy turbidite curre nt and re pr sent F8 a nd F9a fac ies types. The prese nce of gla uconite g rain in calca re nite with echinoderms indicates lo ng-term sediment ta rvation in the provena nce a rea (Odin &Fullagar 1988, Amoro i 1995). 
MEMB ER 2 
Me mbe r 2 i pr s nt in all the inves tiga ted ctio n almost without la te ral varia tio ns in thickn e sand compo itio n (Fig. 3.3, 3.4, 3.49). 
Facies description.-Me mber 2 is cha racterized by 0.3-5 m thick b ds (Fig. 3.56) o f light gray oolitic packsto ne a nd g rain tone. 
Thicker b d are tr uctureless, whereas thinne r (less tha n 0.5 m) beds a t places show g rading, pa rallel, a nd rarely ripple cross la mina tio n (Ta-c Bo uma 
eque nces). Th limesto ne a re compo ed primarilyofooid while o ther g rain (echinode rm , pelo id , foraminifers (Textula riid ae, Involutinidae, Lituolid ae), a nd micriti c intraclasts) a re ra re (Fig. 3.57). Black che rt nodules are prese nt in so me bed . 

3 SImI igmphy 
Fig.3.57 Member 2 of the Travnik Formation: packstonewith ooids, peloids, benthic foraminifer (section MAl).Scale bar is I mm long. 
Age.-In th MAl section (Fig. 3.3) the underlying Member 1 is dated as latest Bajocian-early Bathonian (sample MM 30.60 in Smuc & Corican 2005, for the po ition of the sample see Fig. 3.3). Smuc & Corican (2005) gave a broad age a signment of latest Bajocian-early Bathonian to late Bathonian-earlyCallovian for the overlying Member 3 (sample M8 38.40, for the po ition of the sample ee Fig. 3.3). Thu , according to the stratigraphic po ition of Member 2, a Bathonian age was determined. 
Depositional environment.-Thinner beds were depo ited from sandy turbidity currents and are F8 and F9a facies types. Thicker, structureless beds most probably were deep-water massive sand bodie (according to Stow & Johansson 2000) and were deposited by highly concentrated sandy turbidity currents. Their thickness is constant in all of the investigated ections thus indicating sedimentation on the basin plain. 
MEMBER 3 

Deposits of the Member 3 are investigated at the MAl and MA 3 sections (Figs. 3.3, 3.4, 3.49). 
Facies description.-Member 3 starts with several, up to 2.60 m thick, carbonate breccia beds, each of them capped by fine-grained parallelly laminated packstone/wacke tone (Fig. 3.58). The lowermost breccia bed is channeled into underlying Member 
2. At places only the amalgamated breccia beds are present while fine-grained calcarenite are missing.Breccias are grain-supported, graded and composed 
Fig.3.58 Base ofMember 3 ofthe Travnik Formation: erosional contact between breccias and fine-grained calcarenites (arrow) (Travnik structural unit of the Ml. Mangansaddle, section MAl). Photo Rafael Marn. 
of up to 5 cm large lithoclasts of underlying lithologies of Members 1, and 2, and the Sedlo Formation (Fig. 3.59). Other clasts are composed ofabundant fragments of echinoderms, fragments of stromatoporoids, coral and foraminifers (Textulariidae,Involutinidae, Lituolidae). Individual breccia beds al 0 occurin the middle part ofMember 3. The overlying laminated fine-grained packstone/ wacke tone i composed of filaments, mall echinoderm fragments and micritized ooid (Fig. 3.60). 
This package is overlain by thin-to medium-bedded, coar e-to fine-grained limestones showinggrading, parallel and wavy lamination (Ta-Tc Bouma divisions) . They have a similar composition to limestones of Member 2, but contain fewer ooids. 
Thin-bedded, parallelly laminated radiolarianbearing cherty lime tone characterizes the middle part of Member 3. 

3 Straligra/Jily 
Me mber 3 e nds with a 3 m thick bed compo ed of 30 cm thi ck breccia at th e base, which abruptly pa e into massive fin e-grained indistin ctly la minated packstone / wacke t ne with chert nodul es (Fig. 3.61). The breccia ha the arne composition as th e breccias in the lowe r pa rt of Member 3. The packstone / wackestone with che rt nodules is composed of fila me nts, echinoderm fragments, rare ooids, phospha te grains a nd pyrite. 
Age.-On the ba i of the radiolarian in the che rty limesto ne in the middl e pa rt of Me mber 3 Smuc & Gorican (2005) (sample M8 38.40, for the po ition of th e sa mple see Fig. 3.3) d e termined a broad age a sign me n t oflatest Bajocia n-early Bathonian to late Bathonian-arly Callovian ( AZ 5-7 in Ba umgartner e t al. 1995a). On the basi ofcorrelation with the T ethyan tran gre ive/ regre sive cycle ofJ acquin e t al. (1998) the breccias ofthe lowe rmost part of th e Me mber 3 mo t probably correspo nd to the late Batho nia n lowsta nd. 
Depositional environment.-The base of Me mber 3 i cha racteri zed by a malgama ted breccia bed representing the F3 facies type that were de po ited by d ebri fl ows. Individual breccia beds are directly overlain by fin e-grain d calcarenites in terpreted to be th e dilute "tail" of the ame gravity flow that produced each breccia bed , thus indi catin g ubstantial sediment by-pass (cf. Mutti 1992). Two br ccia beds in tl1e middle part of th e me mber were d eposited by gravelly high-de n ity turbidity currents and represents F4/ ?F5 facies type. oar e-to fine-grained calcare nites from middle pa rt of M3 me mbe r were de posited fro m a sa ndy turbidity currents and rep-re e nt top-cu t-off Bo uma s que nce ofF8/ 9 and F9a fac ies type. Th iliceou limesto nes were de posited by low-de nsity turbidity currents and represent Tb 
Fig.3.6J Upper panofthe Membe r 3 of th e Travnik Formation: massive pack tone -wac kesto ne with che rt nodules. Section is in overturned po ition (Travn ik structural unit of the Ml. Mangansaddle, section MAJ). Ph oto Rafae l Marn. 
Fig. 3.59 Membe r 3 of the Travnik Formation: carbonate breccia with lithoclasLS of Member J and 2 of the Travni k Formation, Sedlo Formation and fragme nts of stromat
o poroids (section MAl). cale bar is 1 mm lo ng. 
Fig. 3.60 Member 3 of the Travnik Formation: wacke
tone/ packs tone wi th filaments and mall echinoderm fragments (sect ion MAl). 

3 Siraligra/)hy 
Bouma sequences of F9a fac i s typ . The massive breccia bed that grades to a fine-grained limestone with chert nodules in the uppermost part of the member wa depo ited from highly concentrated turbidity current and b longs to a F3 / 4 facies type. 
MEMBER 4 

Member 4 wa inve tigated in the MAl section (Fig.3.3). M mber 4 contain cherty limestones, cherts and iliceous mudstones with intercalation offine to very coarse-grained calcarenites. Carbonate breccia is present in the uppermo t part of the member. 
Facies descnption.-The lower 15 m of Member 4 are characterized by thin-bedded laminated (Td)black ch ert and ch erty limestones ( ame composition as cherty lime tones of Member 3) with intercalated thin-bedded, fine to coarse-grainedcalcar nites. Calcarenite h ow Ta-b and Tb-d Bouma divisions and are pack tone composed of filaments, peloids, echinoderm fragments, foraminifer (Textulariidae, Involutinidae, Lituolidae) and phosphate grain . Ooids are rare. In coarse-grainedfacies, reworked lithoclasts of Member 1, 2, and 3 occur. In the middle part of Member 4, thin beds of orange replacement chert are present.
The upper part ofMember 4 tarts with red radjolarian cherts with intercalated coarse to very coarse-grained calcarenites (Ta Bouma division) (Fig. 3.62), and continues with a 2.5 m thick, clay-rich packagecontaining intercalations ofred calcareou clay-richchert and coarse-grained calcarenites. 
The uppermo t part of Member 4 is compo ed of red laminated and, at places, graded radiolarianrich marls (Fig. 3.63) with intercalations ofa carbonate breccia and coarse-grained calcarenites. 
Fig. 3.63 Member 4 of the Travnik Formation: laminated,radiolarian-rich marl (se ction MAl). cale bar is I mm long. 
The intercalated coarse-grained calcarenites are packstones to grainstones compo ed ofpeloids,echinoderm grains, foraminifers (Textulariidae,Involutinidae), rare mall ooids and mudstone clasts. In the uppermost part of Member 4, the calcarenites are composed exclusively of echinoderm fragments.
The breccia bed (30 cm thick) in the upper part ofMember 4 (Fig. 3.64) is coarse-grained (clasts are up to 10 cm), grajn-supported and composedmainly of large lithoclasts of underlying litho logies 
Fig. 3.62 Member 4 of the Travnik Formation: red radiolarian chen, with intercalated coarse-grained calcarenites. ection is in overturned position (Travnikstructural unit of the Ml. Mangartsaddle, section MAl). Photo Rafael Marn. 

3 Stratigraphy 
Fig. 3.64 Upper part of the Member 4 of the Travnik Formation : breccia (Travnik structural unit of the Ml. Mangan saddle, section MAl).Photo Rafael Marn. 
Fig.3.65 Member 4 ofthe Travnik Formation: carbonate breccia with lithoc1asts of the Members 1,2,3 of the Travnik Formation, belemnites and peloids (section MAl). Scale bar is 1 mm long. 

of the Travnik Formation (Fig. 3.65). Other grains are echinoderms, belemnites, peloids, foraminifer (Textulariidae, Valvulinidae), fragments of algaeand corals. Important constituents are rare but large(up to 2 mm) euhedral delritic grains ofbytowniteanorthite feldspars (Fig. 3.66). 
Age.-Based on the stratigraphic position and radiolarians found in the siliceous limestones late Bathonian/ Callovian to early Tithonian age was determined for these deposits by Smuc & Corican (2005). The authors determined the following ages (for the position of the samples see Fig. 3.3): samples MS 33.30, and MS 21.90 corresponds to AZs 6 to 7 (middle Bathonian to late Bathonian-early 
Fig. 3.66 Member 4 of the Travnik Formation: breccia with echinoderms and euhedral detritic grain of bytownite-anorthite feldspar (section MAl) . Scale bar i I mm long. 
Callovian), samples MS 14.30, and MS 10.90 are a ignable to the middle-late Oxfordian (UAZ 9) , sample MS 6.S0 is not younger than late Oxfordianearly Kimmeridgian (UAZ 10?) (for the position of the samples see Fig. 3.3). 
Depositional environment.-Cherts, calcareous clayey cherts and marls of Member 4 represent the background pelagic edimentation. The carbonate admixture in these beds can be either of pelagic or platform origin. Lamination and, at place, grading suggest hydrodynamic sorting. The fine-to medium-grained calcarenites were deposited bylow-to medium-density turbidity currents and are ba e-missing Bouma sequences and correspond 

3 Stratigraphy 
to the F9a fac ies type. Coarse-gra in d calcarenites belong to the Ta-b Bouma divisio ns ofF8/ 9a facie and were d e posited by sandy, hig h-de nsity turbidity curre n ts. The breccia bed in the uppermost part of the me mber is a d ebris-flow a nd corresponds to the F3 facies type. 

3.2 CRETACEOUS FORMATIONS 

The Cretaceous formation a re uniformly d eveloped over the entireJulian appe. H owever, the outcropsof the Cretaceous formation a re rare in the Julian 
appe a nd no section with continuous Cretaceous d evelopment has been found. 
3.2.1 BIANCONE LIMESTONE 

The Biancone limestone i a bedded pelagic limestone containing che rt. It conformably overlies the Prehodavci Formation and the Travnik Formation. The exact thickne s of thi unit in the investiga ted 
ctions is not known since th e upper boundary i never exposed , but the thickness can be estimated to be at least 10m. In the literature the following localities have thus far been reported to have exposuresof the pe lagic Bia ncone lime tone: Mt. Mangart saddle, Pleiiivec, Cisti Vrh, Logj e in the Bavsica valley, Vas na Skali, Luznica Lake, and Triglav Lakes Valley (Cousin 1981 , Buse r 1986, Jurkovsek 1987, Jurkovse k e t al. 1990) . In thi tudy th e Biancone limestone was investigated in the Travnik tructural unitofMt. Mangartsaddle ( ection MAl, and MAS, Figs. 3.3, 3.4), Triglav Lake Valley, Cisti Vrh, and at Vas na Skali. 
Facies description and lateral variations.-In the Triglav La kes Valley and at Cisti Vrh the direct contact of the Bia ncone limestone a nd the unde rlyingPrehodavci Fo rmation is covered. The Biancone limestone is re presented by up to 10 cm thick bed of mudstone to wackestone with up to few cm-thick chert bed and nodules. It i compo ed of calcified radiolarians, ap tyc hi a nd calpio ne llids (Calpionellaalp'ina (Loren z), Remaniella catalanOl? (Pop)). Extremely rare echinoderm fragm nts are also present. In the upper part of this unit Calpionella eliiptica ( adi ch ) is present as well. 
At Vas na Skali, the previo usly d escribed Biancone limestone passes upward into a matrix supported , medium-grained chaotic conglomerate. Clasts a re composed exclusive ly of Biancone limestone (Fig. 3.67) that at places show plastic deformation. 
The matrix of the conglom rate is wackestone composed mainly of radiolarian moulds and rare Calpionella eliitJtica (Cadi ch ). At place the matrix is completely sili cifi ed. 
Fig. 3.67 Bia n cone limeston e: conglo merate with clasts of Biancone lim estone embedded in a radio larian-rich matrix. (Vas na Skali ) . Scale bar i 1 mm long. 
The pelagic limestone at Mt. Mangartsaddle was investigated in th e Travnik structu ral unit (section MAl and MAS, Figs. 3.3, 3.4). The lower part consists of red nodular (bed thickness is up to 5 cm) (Fig. 3.68) mud tone to wackestone compo ed mainly of calpionellids, ap tychi , and calcified radiolarians. 
Fig. 3.6 Bian one limestone: nodular lim e LOne with chert beds (Travnik structural unit of the ML Manganaddle, se tion MAS). 

3 Stra l igrajJhy 
Fig. 3.69 Biancone limestone: lectonized lighl gray limestone with chert nodul es (Travnik slruclu ralunil of the Ml. Mangan saddle, section MA5) . 

Echinoderm fragm e n ts and be nthic fora minife rs a re extremely rare. Up to few ce ntime te rs-thick beds of red re place me nt che rt occur within nodula r lime to nes. In th e MAS sectio n , a few beds of calca re nite co mposed exclusively of echinod e rm fragme n ts a re inte rcala ted in the lowermost part. In th e lowe rmost pa rt Crassicollaria sp . a nd Calpionella alpina (Lo re nz) a re present, while in th e middle pa rt Ca lpionella eliilJlica (Cadisch ) occurs. The uppe r part (exposed only at section MA5) is a strongly tectonized light g ray wackes tone / mudstone with che rt nodules (Fig. 3.69) composed exclusively of calcified radiola rian moulds. 
Age.-In the Triglav Lakes Valley, Cisti Vrh and Vas na Skali areas the La te Tithonia n to middle Be rriasian age of th e exposed Bia ncone limestone was de te rmined o n th e basis of th e Calpionella alpina (Lo re nz), R entaniella catalanoz? (Po p) and Calpionella eliilJlica (Cadisch) (according to Re mane 1985 and Crlin & Blau 1997). The a me age wa de te rmined fo r th e red nodula r limesto nes in the lowe r pa rt of th e MAl and MA5 sectio ns a t the Mt. Ma ngart sad-dl e. The light gray limesto nes with che rt nodules in the uppe r pa rt of the MA5 ection in th e Mt. Ma nga rt saddle a re da ted with radiola ria ns. A la te Vala ngi ni an-early Ha uterivian age ( AZ 17-1 8 of Ba umgartne r e t al. 1995a) was de te rmined o n th e bas is of th e radiolarians (Corica n & Smuc 2004, p.35).
Depositional environment.-The Biancone limesto ne was de pos ited by no rmal pelagic sedime ntatio n in a d eepe r-wate r e nviro nme nt. At pl ace nodula r bedding suggests the influe nce of sea-bo t-tom curre n ts tha t caused slower sedime n tatio n rates and early selective ceme n tation. At Vas na Skali,the Biancone limestone passes upward into chaotic conglome ra te . These d e posits are interpre ted as debri flow de po its tha t fo rmed due to th e local loss of shear stre ng th ofth e pa rtIy consolidated ma terial in a slope e nvironme nt. 


3.2.2 SCAGLIA VARIEGATA 
In theJulia n Alps, exposures of the Scaglia variegata a re very ra re. Only five localities have thus far been re ported in the lite ra ture. These are: Logje in the Bavsica valley, Vas na Skali, Slatenek creek, Luzni ca La ke, a nd Mt. Ma nga rt (Cousin 1981, Buse r 1986, Jurkovse k 1987, Jurkovse k e t al. 1990, Pavsic 1994, Corica n & Smuc 2005) . In these a reas green a nd gray marls, shales, calca re nites, a nd che rts, ma ke up th e Scaglia variegata de posits. At Mt. Mangart,th e Scaglia va riegata crops o ut in the Drn structural subunit. This outcrop was da ted by Corica n &Smuc (2004) , and is d escribed below. 
Descnption.-The succession at section MA6 (Fig.3.5a, b ) starts with lowe r Lowe r Jurassic pla tform limes tone cut by Jura sic neptunia n d ykes ( ee cha pte r 3.3.1 ) that are unconformably ove rlain by 20 m of middle Cretaceous Scaglia variegata. The Scaglia variegata sta rts with 0.5 m of bedded (bed thickness up to 20 em ) medium-grained breccia that grades into medium-grained calca re nite. The la rgest clasts in breccia a re 3 em , are de nsely packed , and elo ngated cl as ts a re alig ned pa rallel to the 

3 Stratigraphy 
bedding. Clasts are composed of echinoderm fragments, lithocla ts of gray, black and orange cherts,and lithocla t ofradiolarian-bearing wackestone to packstone (Fig. 3.70). Glauconite and chlorite are also present. Grains are cemented by blocky sparitethat i , in places, completely ilicified. 
Fig.3.70 caglia variegata: basal breccias with lithoclasts ofcherts, and siliceous lime tone with radiolarians (section MA6). Scale bar is 1 mm long. 
The breccia and calcarenite are followed by 16 m of gray, thin-bedded siliceous limestone that alternates with gray to green marl and chert. Marls are common in the lower part while upwards limestones and cherts predominate.
The upp rmo t five meters ofthe succession are composed of0.5 m ofnodularly-bedded black cherts with manganese, 2 m of red bedded chert, and a 2 m ofred thin-b dded marly packstone composed almostexclusivelyofplankticforaminifers (Fig. 3.71). The matrix of lime tone is microsparite, at places 
Fig.3.71 Scaglia variegata: limestone with small keel-less globular foraminifers (seClion MA6). 
completely replaced with Fe-Mn oxides. The most abundant foraminifer are small keel-less globularforaminifers. However, in the uppermost part ofthe 
ection very rare globotruncanids with developedsingle keel al 0 occur. 
Age.-Ba ed on the radiolarians from the siliceous lime tones 4 m above the base of the succession, an early or ear!>' middle Albian age was determined (Gorican & muc 2004). In the uppermost part of the succession, globotruncanids with a developed single keel occur. The e can be used as a biostratigraphic marker, as the first occurrence of keel in globotruncanids is in the Rotalipora subticinensis Zone, i.e. in the late middle Albian (Caron1985).
Depositional environment.-The ba al medium-grained breccia and coarse-grained calcarenite were deposited by a high-de nsity turbidity current. The completely lithified clasts ofcherts indicate the erosion of older strata. Glauconite grains indicate sediment starvation in the provenance area (Odin& Fullagar 1988, Amorosi 1995). The marls in the lower part indicate higher input of clay in into basin . Siliceous limestones, cherts and limestones with pelagic foraminifers represent deeper-water pelagic sedimentation. 


3.2.3 SCAGLIA ROSSA 
In theJulian Alps, the exposures ofthe Scaglia rossa are more common than those of the Scaglia variegata. The Scaglia ro sa deposits occur as smaller erosional remnants on an older (uppermost Triassic to lower jurassic) platform and deeper-waterdeposits. sually the contact of the Scaglia rossa with older trata repre ents a dis ontinuity urface,rarely the Scaglia ro sa i in fault contact with urrounding rocks (Cousin 19 1, Bu er 1986,jurkov-ek 1987, Radoicic & Buser 2004). The Scaglia rossa in thejulian Alps was described by Cousin (1981) , Buser (1986) , jurkovse k (1987), jurkov-ek et al. (1990) and Radoicic & Bu er (2004). Scaglia ross a is characterized by red, rarely gray, thin-bedded limestone and marly limestone with abundant globotruncanids. On the basis of the globotruncanidsthe caglia rossa ranges from th e upper Turonian to th lower Maastrichtia n (Cousin 1981) , however in the Bovec area the caglia Rossa is conformablyoverlain by Campanian fly ch depo its (Buser 1987, jurkov-ek 1987, RadoiCi c & Bu er 2004) . The thickness of the Scaglia ros a in the julian Alps ranges from few meters to approximately 100 m . 

3 Stratig raphy 
Fig. 3.72 cag lia rossa: thin bedded limesto ne, overlain by coarse-grain ed b reccia (Ma li Vrh structural subunit ofthe Mt. Manga n saddle, ection MA7) . Photo Rafael Marn . 

In this study the Scaglia rossa was studied at Mt. Mangart saddle, section MA 7 (Fig. 3.5). The Scaglia ros a of th e Mt. Ma ngartsaddle was previously investigated by Cousin (1981) a ndJurkovsek etal. (1990) and assig ned to the Turo nia n and Se no nia n on the basis ofthe globo truncanids. My study revealed tha t at Mt Ma ngart saddle Scaglia ross a cro ps o ut o nly in Mali Vrh and Rdeca skala subunits of the Ma ngart structural unit ( ee Figs. 2.6, 2. 7). In th e Mali Vrh subunit, th e Scaglia ro a unconfo rmably overli es Uppe r Triassic to lowe r Lowe r Jurassic pl atform limesto ne cut by large ne ptunia n dyke , while the structural subunit Rdeca skala consists o nly of comple tely tecto nized Scaglia rossa. The investigated sectio n MA 7 (Fig. 3.6) is a pa rt of the Mali Vrh subunit,however due to th e poor exposure, its direct con tact with the unde rl ying uppe r Triassic-lowe r Lower 
Jurassic pla tform limeston e is not recorded. 

Facies description. -The succe io n is composed of thin-bedded (bed thickn ess is 2-5 cm ) red a nd subordina tely gray wackestone (ra rely packstone and mudsto ne) (Fig. 3.72) tha t exhibits horizo n tal lamina tion a nd, at place , normal a nd inve rse grading and ripple cross-laminatio n (Ta, Ta-c Bouma divisio ns) . 
T he lime to n e is compo ed mainly of small keelless globula r foraminifer and glo botruncanids with a d evelo ped single keel (Fig. 3. 73). Spo ngespicules, calcified radiola ri a n , echinoderm fragme n ts, small spari tic g rains, phosphate, glauconite and qua rtz grain are rare. Within these limesto nes, medium-grain ed calcarenite and coarse-grained breccia occur. The calca re ni tey bed is 10 cm thick 
Fig. 3.73 Scaglia ro sa: packstone with abundant globotruncanids ( ection MA7) . Scale bar is 1 mm long. 
and norm ally grad ed , a nd th e base i e rosio nal. T he calca re nite consists oflithoclasts a nd bioclasts. Lithoclasts include previously d escribed limesto nes with pla nktic foraminife rs a nd mudsto nes, la minated and graded siliceous limesto nes with radiolarian , shallow water pelo idal grai nstones, and che rts. Bioclasts are fragme n ts of I noceramus sp., fragme n ts of echinoderms, and be nthic fo raminife rs (Len ticu lina sp. and Textula ridae) (Fig. 3.74) . Other grains a re glauconite, pho phate and quartz grai ns. Grai ns are ceme nted by gra nular sparitic ceme nt a nd yntaxial ceme n t around echinoderm grai ns. 
A breccia bed is presen t in the uppe r part ofthe inves tigated sectio n (Fig. 3.72). It is poorly-sorted, normally graded and clast uppo rted . Clasts are upto 1 m and include : 

3 Stratigraphy 
• 	
limestones with globotruncanids,


• 	
wacke tone to mud tone with calcified sponge spicules, 

• 	
normally grad ed a nd horizo n tally laminated red siliceous limes tones with radiolarian, 

• 	
red cherts,


• 	
red la minated ma rly wackestones to packstones with abundant Saccocoma, fragments ofechinode rms, aptychi a nd be nthic foraminifers, 

• 	
pelle toidal limestone,


• 	
light gray packstone to grainstone composed of peloids, fragments of limestone with fenestral porosity, algae fragments, be nthic foraminife rs, and echinoderm fragments,

• 	
la mina ted a nd normally grad ed wackestone with pellets a nd foraminifers,

• 	
light gray shallow water limestones with ne ptunia n dykes. 


Fig. 3.74 Scaglia rossa: calcarenite with mudstone lithoclasts, Inoceramussp., and fragments ofechinoderms (section MA7). Scale bar is 1 mm lo ng. 
The matrix of the breccia is a wackestone with planktic fo ra minifers, described in the lower part of the successio n. 
Age.-The inves tigated section MA7 corresponds to the Unit 2 of the Rdeca skala of Cousin (1981, 
ee p. 440, a nd 441) . Cousin (1981) d ated this unit on the basis of the glo bo truncanid as uppe r Senonian. 
Depositional environment. -The Scaglia ross a represent typical d eepe r-wate r sedime n ts in the Uppe r Cretaceous. The thin-bedded wackestone with normal a nd inverse grading, ho rizon tal and ripple-crosslaminatio n were d eposited by low-d e nsity turbidity curre nts (cf. Pipe r & Stow 1991, Shanmugam 2000) . The normally g raded calcarenite bed representstop-cut-off Bo uma seque nce (Ta) and was deposited by medium-grained turbidity curre n ts. The coarse-grained breccia is here considered to be the product ofa hyperconcentrated gravity flow (cE. Mutti 1992). The presence ofvarious clasts of olde r strata in the calcarenite and breccia indicates exhumation ofund e rlyi ng lithologies by synsedime n tary extensio nal tectonics and e rosio n at least down to UpperJurassic d e posits ( clasts of red ma rl y wackestones with abundant Saccocoma). Prese nce of Inoceramus sp. , fragments ofechinoderms, and benthic foraminifers indica tes input from shallow-water areas. 


3.3 NEPTUNIAN DYKES 
eptunia n d ykes are present o nly in the drowning successions of the Julia n High , a nd th ey are comple tely abse nt in the investigated Bovec Troughsections. 

3.3.1 	NEPTUNIAN DYKES OF THE MANGART STRUCTURAL UNIT 
eptunia n dykes are present in the Mali Vrh , Mangart Peak, a nd Drn subunits, where they pe netrate uppermost Triassic a nd Lower Jurassic pl atform limesto nes. 
The structural subunit Mali Vrh is ma rked by numerous neptunia n dykes. They were studied in the MA7 section (Fig. 3.6) a nd also at roadside outcrops o n the road to Mt. Mangart saddle (forlocation see Fig. 2.7). Two distinct generatio ns of ne ptunia n d ykes were differentiated o n the base of their geometry a nd sediment infilling. 
The first gene ra tion is represented by two major types ofneptunian d yke: dykes with irregular-undulate and concave walls a nd dykes with straig ht walls exhibitin g a jigsaw structure. The former are characterized by up to 20 cm thick oval cavities with smooth and undula te surfaces (Fig. 3.75). Cavity wall are rimed by fibrous ce me nt (Fig. 3.76). The re maining space was filled with red mudsto ne with fragme nts of 0 tracods, echinode rms, ammonites,spo nge spicul es a nd be nthic foraminifers includingAgerinamartana (Farinacci) (Fig. 3.77). Thin Fe-Mn crusts are present within th e mud tone (Fig. 3.78) . Ra rely the remaining space is fill ed with wackestone with echinoderm fragments, be nthic foraminifers and mudstone lithoclasts. The second type is cha r-acterized by straightwalls exhibitingjigsaw structure. These fissures are filled by the previou ly mentioned red mudsto ne with Agerina manana (Farinacci). On 

3 Stratigrap hy 
Fi g . 3. 75 eptunia n d ykes Wilh irregula r-undula le wa ll (Ma li Vrh slruclura l subunit 
o f th e Ml. Ma ngan addle).Ph OlO Ale nka Eva e rn e . 
Fig. 3.76 eplunian dyke: fibrous ce me nt rim a round cavity wa lls. ppe r part of the photograph i mudstone 

(1. gene ra lion of ne plunia n dyke infill of Mali Vrh struclura l ubunil). Scale bar is I mm long. 
Fig. 3.77 eplllnia n dykes: mud to ne with Agerina mar-Iana (Fa rinacci) (1. gene ra lion o f the ne plllnia n d yke infill of Mali VI'h struClura l subunil). Scale bar is I mm long. 
Fig. 3.78 Ne ptunian dykes: lowe r part of the photographis mudslones wilh Fe-Mn crusts. In th e uppe r pan of th e photograph wacke LOne with echinod e rm fragme n ts and mud to ne intraclas ts are pre e nl. (I. ge ne ra tio n o f the ne ptunian dyke infill of Mali Vrh struclllral subunil).
ca le bar i I mm lon g. 

3 Stmligmplty 
th ba i of th e prese nce of A. mariana the age of the fo rma tio n of the oldes t infilling of ne ptunia n dyke is Plie nsbachia n (thi infilling is coeval with the dl o Fo rmatio n of Bovec Trough, see cha pte r 
3.1. 3). The caviti es with irr gul ar undula te walls were formed by dissolutio n , howeve r at places it is clearly vi ibl e th a t dissolution r sha p d fractures with straig ht walls (ern e 2004). Dykes with straight walls were formed by mecha ni cal deformatio n of th e host rock due to the exte nsion al tectonic move-me n ts in the Plie nsbachia n. Thejigsaw tructure was form ed due to th e seismi c shocks a nd injectio n o f unlithifi ed pIa tic edime nt. Alte rnatio n ofceme nts, sedime nts, a nd cru t i indicative of breaks during sediment infiltration. 
The second gene ra tio n of ne ptunia n dyke is the most prominent gene ra tion of fractures. It occurs in Mali Vrh a nd Ma ngart peak subunits a nd 
Fig. 3.79 La rger chaotic breccia -n e pwnia n d yke filling (Mali Vr h structural subunit of th e Ml. Mangan sad d le) . 
i m a rked by two different types: la rger chaotic breccia bodies a nd smaller fra tures with smooth and straight wall . Chaotic breccias (Fig. 3.79) a re up to few te n of me te r la rge, laterally confined breccia bodies with mostl y uneve n walls. Only in pl aces is sha rp contact with the host rock o bserved. Jigsaw structure in the breccia is a lso pre e nt (Fig. 3.80a,b). Clas ts of breccia a re a ng ul a r a nd u ually not orie nted . Clas ts can be up to 1 min size and a re omposed of massive lime to ne with coral and smaller fragme nts ofshallow-wate r grain tone (Fig. 3.81). Some clasts ofhost rock include evide nce ofthe first generation of ne ptunia n dyke . The first gene ratio n of fillin g is a l 0 pre e nt a cia ts. The ma trix i red a nd g ray micro pa rite with fragmentsof po nge a nd echinode rms, and gla uconite g ra ins. In the uppermost part, the breccia body cl asts a re smalle r a nd the ma tri x i at plac s la mina ted. The 

Fig. 3. Oa Neptunian dyke with j igsaw truclUre (Mali Vrh Fig. 3. Ob ketch of th e neptunian dyke on the phostructural subunit of the Ml. Man gan addle). tograph 3. Oa White color represent Lower J urass ic platform li mesLOne. 
3 Stratigraphy 

3.3.2 NE PTUNIAN DYKES AT RAVNI LAZ 

SECTION 


Fig. 3.81 eptu n ia n d ykes: cia t of mudsLOne e mbedded in ma lrix wilh pa rite grains a nd echinod erm fragme n ts. 
(2. ge neratio n o f Lhe n e p tunian d yke inlill of Ma li Vrh 'l ructu ra l sub unit). Scale bar is 1 mm lo ng. 
econd ty p e o f ne ptunia n d yke i ch aracte ri zed by subvertical a nd bedding-parallel fractures with 
mooth and straight walls. The fractures a re up to 40 cm wide, with a pe netratio n de pth of a few meter . T he e fractu res are fi lled by the previo usly me ntio ned breccia, a nd diffe r o nly in having a smaller g rai n ize. The age ofthe second gene ratio n ofneptunia n dykes is poorly constrained due to lack of age-diagnostic fossils. On the basis of the crosscutting rela ti o nship with the firs t gene ra tio n of ne ptunia n d ykes, the econd ge n ratio n po td a tes the Plie n bachia n. The fo rmatio n of chaotic breccia bodies a nd fractures with straight wa lls i ascribed to the extensio nal tectonic pulse that caused brittle deformatio n of host rock, producing wide cracks that were quickly fill ed a ev ide nced by the lack of ce ment o n the walls (erne 2004). 
Th n e ptunia n d ykes of the Drn structural subunit (loca tio n Fig. 2. 7, tratig ra phic po itio n Fig. 3.5a,b ) a re larger blocky breccia bodies within the lower Lowe r Jurassic pl atform lime to n es. T he breccia bodi e are la terally confi ned to a few te n of meters, sh owing sha rp contact with th e h ost rock. T he b reccia is clasts-supported and con ists ofcobbles and, mo re commo nly, up to meter-sized bo ulde rs of ho t rock e mbedded in a red ma trix. Bo ulders ofthe lowe r Lower Jura ic limesto nes also contain olde r ge ne ratio n of the neptunia n dykes, d e cribed above . The matrix is red microsparitic lime to ne with a ptyc hi , fragme n ts of echinode rms and fragme nts ofpelagic crinoid Saccocomas p. Based 
o n SaccocO'llW p. the most pro bable age of the matrix i la te Kimme ridgia n to early Ti tho nia n (e.g. Sartorio & Ve nturini 1988) . 
At Ravni Laz (sectio n R1 , Fig. 3.2), ne ptunia n d ykes occur thro ugho ut the Preh odavci Fo rmatio n , but were not recorded in th e Lower Jura ic pl atfo rm limestones. He re, neptunian dyke are subparallel to th e bedding a nd are up to 10 cm thick oval cavities fill ed with younger sedime n ts. In the lowe r part of th e Lower Membe r of the Pre hodavci Formatio n, the nep tunian dykes are filled with Kimmeridgian to lower Berria ia n limesto ne. The ba e of ne ptunia n dykes is characte rized by laminated and graded packsto ne to mudstone. Fragments of accocomaare by far the prevailing grains. The upper pa rt of the d yke is fi ll d with th e mi crosparitic-g raded limesto nes composed of echinod erm fragme n ts, calpio nellids (Ca ltJionelia alpina (Lo re n z», and in tracl asts of pack tones with Saccocoma. 
The fo llowing ne ptunia n dyke fill consists of lower Berriasia n fi ne-grained breccias. T his breccia fill cavities of up to a few te n of c n timeters . T he breccia is clast supported and compo ed of lithoclasts of wackestones to m udstones with echinoderm fragmen ts, be nthic fora mini f< r (Lenticulina sp. , Textularidae) and Calp ionella elliptica (Cadisch ) (Fig. 3.82). Othe r g rains are individual echinode rm fragme n ts and Fe-Mn e ncrusted bi ocla ts. 
Fi g. 3. 2 epLUnian d ykes: br ccia with echinoderm fragments and lilh oclasts ofwackeSLO ne with echinodeml fragme n ts (neptu n ia n dyke in fi ll al Ravn i Laz, eClio n Rl ).Scale bar i ] m m lo ng. 
The yo unge t ne ptunia n d yke infillings a re late retaceous in age and occu r in th Pre hodavci Fo rmation . The ne ptunia n dyke a re up to 10 cm wide bed-pa rallel caviti es. In the lower part of the dyke, th e fill is wacke to nes with pla nktic glo bula r 

3 SI raligralJiI), 
Fig. 3.83 Neptunian dykes: packstone with globotrunca n ids and ra re echin ode rm frag me nts (uppe rm os t ne ptunian dyke infill at Ravni Laz, ection RI ). Scale bar is 1 mm long. 
fo ra minife rs, glo bo truncanids a nd ra re echinod e rm fragme n ts (Fig. 3.83). In th e uppe r pa rt of the fill s, th e limes to n es becom e la mina ted. The la minatio ns a re a n alternatio n of up to 5 mm thi c k packsto ne la minae a nd thinne r mudsto n e. Packsto n es a re composed exclusively of fragm e n ts of glo bo truncanids. 

3.3.3 	NEPTU NIAN DYKES AT LUZNICA LAKE SECTION 

At Luzni ca La ke (sectio n Ll, Fig. 3.2) the n e p tunian dykes occur in Lowe r Jurassic platform lim esto nes and in the Pre h o d avci Fo rmation. 
In th e Lowe r Jurass ic platform lime tone, the ne ptunia n dykes a re e lo ngated , subve rtical or bed-pa rallel cavi ties fill ed with younger limes to n e . The fill is gene rally wac kes to ne with sm all spa rite grains overlain by wac kesto n with pl a nktic fo ra minife rs (pro toglo bigerinids), bele mnites, echinod e rm fragm e n ts, fila me n ts, a nd ra rely be nthic fo ra minife rs (Fig. 3.84) . The m a tri x is micrite to mic ro pa rite. On th e bas is o f th e pre e nce of pl a nkti c fo ra mini f-e rs (p rotoglobi gerinids) this ne ptunia n dyke fill is Baj ocia n o r younger. In places, th e re m aining po re space is fill ed by uppe r Titho nia n mudsto nes with Caipionella ai/lina (Lo re nz). 
T he ne ptunian dykes in the Pre h od avci Form atio n occ ur in th e bioclas tic facie ofboth th e Lowe r Me mbe r a nd in th e U ppe r Me mbe r. In bo th ca e the ne ptunia n dykes a re re p rese nted by subve rtical and bed-pa ralle l caviti es up to few dm in dia m e te r. 
Fig. 3.84 Neptunian dyke: in the lower pa rt of the photo wackestone with ec hi noderm fragments and protoglobigerinids. ppe r part of the ph otogra ph i younger mudstone with Cal1Jionr4la alpina (neptunian dyke infill at Luznica Lake, section Ll ). Scale bar is I mm long. 
In the bi o cl astic facies, the n e ptunia n d yke a re fi lled with packsto ne composed ma inly of fila me n ts and e nc ruste d intraclas ts of bi ocl a tic limes to n e . Othe r grain s include echinod e rm fragm e n ts and ga tro po d protoconc hs. In th e pper Me mbe r of th e Pre h od avci Fo rmatio n the fill is ch a racte rized by a n upper Kimme ridg ia n to lower Titho ni a n pac k ton e composed ofSaccocornas p . frag m e n ts and in traclasts ofh ost rock. In th e uppermo t pa rt of the Upper m e mber th e subve rti cal ne ptunia n dykes a re fill ed with mudsto ne with calpi o nellids (Caipioneila aipina (Lo re nz)). 


3.3.4 	NEPTU NIAN DYKES IN TRIGLA V LAKES VALLEY 
Neptunia n d ykes in the Triglav La kes Va lley a re d evelo ped o nly in the uppermost pa rt of the Pre h o-d avci Fo rmatio n ( ectio n TVl, Fig. 3.1 ) as bed-crossin g, up to 50 cm d eep a nd 10 cm wid e fractures wi th a p referential SE-NW orie n ta tio n (Fig. 3.85) th a t are fill e d wi th two differe nt gen e ra tio ns of breccia. At places ne ptunia n dykes exhibitjigsaw structure . The walls of th e fractures a re usua lly e nc rusted with Fe-Mn oxides. The fir t generatio n of breccia consists of fragm e nts of ammonite m o ulds a nd c m-sized Iith o clasts of red wac kes to n es to pac ksto nes with disartic ula ted valves ofthin-she lled bivalves, calcified radio la ria ns of th e red n odula r facies. The m atrix of breccia is packsto ne with fila me n ts, ra re echin od e rm frag me n ts, be le mnites a nd fo ra minife rs ( L enlicuiina sp .) (Fig. 3.86). The second gene ra tio n of breccia 

3 Siratigraphy 
Fig. 3.85 eptunia n d yke with j igsaw structu re (Triglav Lakes Valley, sectio n TV] ). Host rock is limestone of the Prehodavci Formation. Photo Rafae l Marn . 

i composed of euhedral grains of d e tritic quartz,litho clasts of red nodula r limesto ne, pack to ne with calcified radiol arian moulds, a nd wackestone with aptychi . Th matrix of the breccia i wacke tone with echinod e rm fragm e n ts, o paque mine rals a nd Fe-Mn incru ted bioclasts. 
The tra igh t a nd smoo th walls ofth e ne ptuniandyk s suggest brittle fracturing of a we ll-lithifie d host rock. The opening of these fractures was due to th e exte nsional tecto nic move me nts, afte r the d e po ili o n o f Kimme ridgia n ppe r Me mbe r of the Prehodavci Formatio n . 
Fig. 3.86 eptunian dyke: breccia wi th lithoclasts of wackestone with filaments embedded in a wackestone/ packstone with filaments, and rare echinoderm fragments (neptunian dyke infill at Triglav Lake Valley, ection TVl ). Scale bar is 1 mm long. 
Summary.-Ne ptunia n dykes in the investigated a rea a r interpre ted to be the product of tecto nic exte n ion that produced o pe n crack that we re late r fill ed with younger sedime nt. Acco rding to the ageofth host rock a nd ne ptunia n dyke infillings, fo ur m a in pha e of ne ptunia n d yke fo rma tio n in the a rea of the Julia n appe a re recog ni zed : 
1) Plie nsbachia n tectonic phase: 
eptunia n d ykes in the Pli e nsbachia n pla tfo rm limes to nes o f the Ma ngart structural unit. These ne ptunia n d yke infillings ra nge from the Plie nsbachia n to the Kimmeridg ia n-early Tithonia n . 
2) Baj ocia n tecto nic phase: 
Neptunian dykes in the Plie nsbachian pla tform limesto nes with Baj ocia n to la te Tithonia n infillings. 
3) Kimmeridgia n tectonic phase 
eptunia n dykes in the Pre ho d avci Fo rmatio n tha t a re fill ed with the upper Kimme ridgia n to Be r-ria ia n d e posits 
4) La te Cretaceous tecto nic phase (pre-Se nonian ): 
Neptunia n d ykes in the Pre h od avci Formation th a t a re fill ed with U ppe r C re taceous limestones with globotruncanids. 


4 

JURASSIC AND CRETACEOUS SEDIMENTARY AND 
PALEOGEOGRAPHIC EVOLUTION 
OF THEJULIAN ALPS 

The Julian Alps experienced an extension related to the formation of the south Tethyan continental margin that started in the latest Triassic and continued into the Jurassic (see Bertotti et a1. 1993). The Jurassic successions in the Julian Alps aIlow us to decipher the disintegration oftheJulian Carbonate Platform, formation of the deeper Bovec Troughand Julian High, to reconstruct the depositionalhistOlY ofthe trough and the plateau, and to discuss the main mechanisms controIling the sedimentation on theJurassic south Tethyan margin.
Correlation of the two most representative sections of the Bovec Trough (MAl) and Julian High(TV1) with Tethyan transgressive/regressive cyclesis presented in Fig. 4.1. Correlation among all investigated sections is shown in Fig. 4.2. The time spanof formations and stratigraphic gaps is graphicallypresented in Fig. 4.3. 

4.1 HETTANGIAN TO EARLY PLIENSBACHIAN: SHALLOWWATER SEDIMENTATION ON THE JULIAN CARBONATE PLATFORM 
Lower Jurassic platform limestones of the Julian Carbonate Platform represent a continuation of shallow-water sedimentation from the Late Triassic. Facies associations ofthe investigated LowerJurassic sections is representative of a shallow carbonate platform with a variety ofhydrodynamic conditions. The peloidal, ooidal grainstones to packstones of the Travnik structural unit (section MAl, see Fig.3.3) represent the high-energy subtidal sand belt environment in a marginal sector of the carbonate platform. The majority of grains originated from a subtidal lagoonal environment in the internal partof the platform and was later transported to the platform margin. The Triglav Lakes Valley (sectionsTVl, TV4, Fig. 3.1), Ravni Laz (section Rl, Fig. 3.2),and Luznica Lake (section Ll, Fig. 3.2) sections represent more protected inner-platform areas. In these sections, tidal flat deposits are represented by laminated limestone exhibiting birds-eyes, laminoid fenestrae, shelter cavities, and geopetal infillings.They are present only in the lower part of the sections. Upwards, the sections consist ofalternating lagoonal micritic limestones and higher-energy peloidal limestones with a variety of grains. In the Ravni Laz section (RI, Fig. 3.2) lumachelle of bivalves is present. This facies association most probably represents an inner-outer platform transitional zone (cf. Rey 1997, Ruiz-Ortiz et a1. 2004). The vertical alternation of the quiet-water lagoonal limestones and high-eneq.,'Y peloidal limestones, thus suggestchanges from an inner to outer platform environment. This alternation was most probably caused byhigh frequency sea-level oscillations. An additional hypothesis is that the juxtaposition of the higherand lower-energy may have been trough tidal channels (cf. Ruiz-Ortiz et a1. 2004).
In the marginal parts ofthe platform (Mangartstructural unit of the Mangart saddle) small patchreefs thrived as well. 


4.2 PLIENSBACHIAN: DEMISE OF THE JULIAN CARBONATE PLATFORM AND FORMATION OF THE BOVEC TROUGH AND THEJULIAN HIGH 
Shallow-water sedimentation oftheJulian Carbonate Platform halted in the Pliensbachian. In all investigated sections the platform limestones of theJulian Carbonate Platform are conformably or unconformably overlain by deeper-water deposits, thus markingplatform drowning (Figs. 4.1, 4.2, 4.3).
In the Travnik structural unit (section MA 1) the drowning succession is gradual and the transitional facies is present below the drowning unconformity.The transitional succession consists ofshallow-water' grainstones with intercalations of finer-grainedpeloidal wackestones/packstones. These finer-grained limestones formed in a hydrodynamicallyquieter environment and contain open marine elements (Lenticulina) thus indicating a deepening of 


4 Jurassir and C'"f'tarrous sediment",) and evolution oj t"eJulian Alps 
the environment. However, at this stage carbonate production on the platform still managed to keep pace with increased subsidence. The intercalated peloidal wackestone/packstones are thus interpreted as markers ofincipient drowning. Continuouslyincreasing subsidence rates probably coupled with carbonate productivity decrease due to eutrophication (d. Dromart et al. 1996, Mallarino et al. 2002)in the Pliensbachian caused the complete drowningofthe platform, allowing distal shelflimestones with sponge spicules andjuvenile ammonites ofthe Sedlo Formation to accumulate. 
In the Mangart structural unit (MA6, MA7 sections, Figs. 3.5a,b, 3.6), numerous neptunian dykeswith the oldest infilling dated as Pliensbachian penetrate the Lower Jurassic platform limestones. Facies ofthe Pliensbachian infillings are equivalent to that of the Sedlo Formation. 
In the Triglav Lakes Valley (TV1, 4), Ravni Laz (Rl), Luznica Lake (Ll) sections (Figs. 3.1,3.2) the LowerJurassic platform limestones are unconfi.)rmably overlain by the Bajocian to lower Tithonian condensed limestones of the Prehodavci Formation, demonstrating a stratigraphic gap comprising at least the Toarcian and Aalenian. The drowningunconformity is expressed by up to 3 m deep and 10 m wide oval cavities cut into the lower Jurassic platform limestones that are filled with limestones of the Prehodavci Formation. The morpholoh'J' of this surface suggests formation mainly by chemical erosion most probably due to a subaerial exposure.
The causes fi.Jr platfi.xm drowning may include rapid sea-level rise from tectonic or glacio-eustacy,and environmental changes that reduced benthic carbonate production (Schlager 1981,1989, 1992, Dromart et al. 1996, Ruiz-Ortiz & Castro 1998, Mallarino et al. 2002, Morettini et al. 2002). In the Julian Alps, however, the tectonically induced subsidence as a main factor controlling the platformdrowning is directly evidenced by the presence of Pliensbachian neptunian dykes in the uppermost part ofthe LowerJurassic shallow water limestones. Additionally, the differential tectonic movement of isolated blocks is clearly recorded by different manifestations of the drowning unconformity over very short distances: a probable uplift into subaerial environment (Triglav Lakes Valley, Ravni Laz, Luznica Lake areas), formation of neptuniandykes (Mangart structural unit), and synchronousdeepening-upward facies trend in the drowningsuccession of the Travnik structural unit. 
Our data thus indicate that shallow-water sedi
mentation on theJulian Carbonate Platform ended 
in the Pliensbachian due to an extensional tectonic phase. At that time the platform was dissected bynorth-south and east-west trending faults (Buser1986, 1996) into blocks with different subsidence rates. Two different paleogeographical domains were formed: a deeper-water Bovee Trough (Travnikstructural unit) with sedimentation of distal shelf limestones of the Sedlo Formation, and a pelagicplatform (sensu Santantonio 1994) named the Julian High. The Mangart structural unit representsthe tectonically most active margin of the Julian High. From the Pliensbachian, this area was subjected to repeated tectonic fracturing, depositionand erosion, so that sediments are preserved onlywithin numerous polyphase neptunian dykes. The Triglav Lakes Valley, Ravni Laz, and Luznica Lake sections represent the interior portions oftheJulian High that at that time may have emerged, enablingthe formation ofa karstic discontinuity surface. An alternative hypothesis is that the inner areas of the Julian High were also drowned, and the discontinuity surface formed by sea-floor dissolution (cf.Di Stefano & Mindszenty 2000). The timing of the formation ofthis discontinuity surface is difficult to determine because the overlying pelagic sediments are as young as Bajocian.
The EarlyJurassic extensional tectonic phasethat lasted from the middle Hettangian to the late Pliensbachian is recognized across entire passive south Tethyan continental margin (Winterer& Bosellini 1981, Bertotti et al. 1993, Sarti et al. 1992, Di Stefano & Mindszenty 2000, Di Stefano et al. 2002, Baumgartner et al. 2001, Clari & Masetti 2002). 


4.3 LATE PLIENSBACHIAN TO TOARCIAN: SEDIMENTATION IN THE BOVEC TROUGH 
In the Pliensbachian, the Bovee Trough is marked by sedimentation of deeper-water distal shelf limestones of the Sedlo Formation (MAl section, Fig.3.3). In the upper part of the Sedlo Formation, rudstone -packstone is present. It contain previously cemented echinoderm fragments and clasts of underlying lithologies. Its fi.mnation is related to another synsedimentary extensional pulse in the Pliensbachian that produced an unstable slope, uncovered older rocks and enabled erosion. This facies change from distal shelflimestones to echinoderm rudstone -packstone is similar to the change observed in the transition from the Inici M3 Member to 



4 j urassic and Crp/{w'ous .5I,dilllen la ,)' and /)aleogeogn,ph.ir I'lIOlliliO I/ of IIII'j u lia 1/ AI/)s 
IMNGART <J)STRUCTURAL 
w w 
UNIT 

DI NARIC < :I: <J)
TRENTO PlJ\TO BELLUN O BASIN (FRIULI) !.!
AGE PlJ\TFORM ....e; z C/> ;::

N <J) 
<J) .(3
! 3 

Fig. 4.3 Ages o f th e Jurass ic a nd Cretaceous fo rmatio ns and corre la tio n o f the investiga ted sec Li o ns in the .lulia n Ips with the Trento Pla teau a nd Be lluno Bas in (Ju rass ic fo rmaLi o ns afte r Ba umgartne r e t a l. 1995a, C retaceous fo rmatio n afte r Le h ner 1992), and with th e T o lmin Tro ugh (sec Li o n Perbla-T o lmin ske Ravn e) (a fter Caro n & Cousin 1972 , Cou in 1973, 19 I ). Time scale a fte r Odin (1994) . 
4 1I1m.,,;( "n" C''I'lfU'I'OIiS ,,'dimfnlmy aud jJalfogl'Ogmli1,i( 1'1I1"ulio/l o/lilf1111ial/ Alfls 
the Calcari a Crilloidi Formation at Monte Kumeta in western Sicily and is similarly interpreted to be a consequence of further and relative sea-level rise (see Di Stefano et al. 2002).
The pelagic wackestone/packstone with radiolarians, spicules and Fe-Mn nodules overlying rudstone -packstone indicate extremelyreduced sedimentation rates that reached a minimum with the formation of a 25 cm thick Fe-Mn hardground. Slowing of the sedimentation rates and formation of Fe-Mn nodules and crusts in the Bovec Trough is a result of the late Pliensbachian widespread Tethyan (R5 in Graciansky et al. 199H) that induced strong bottom currents that swept the sea floor and thus preventedsediment accumulation (cf. Schlager 1981, Martire 1992, 1996, Tucker 2001).
Sedimentation was restored in the Toarcian when limestones and shales ofthe Skrile Formation began to accumulate. Sedimentation rates increased most likely because ofthe weakening ofbottom currents due to the early Toarcian (T6 in Graciansky et al. 199H) (Fig. 4.1) and an importantincreased input of terrigenous clastics. The earlyToarcian shales and intercalated radiolarian-bearing limestones are organic-rich sediments depositedduring the early Toarcian Oceanic Anoxic Event, also recorded in other parts of the Mediterranean including the Southern Alps (Jenkyns 19H5, 1988, Jenkyns & Clayton 19H6,Jenkyns et al. 19R5, Baudin et al. 1990). The Bovec at that time acted as an anoxic basin, trapping the fine-grained sediments located within the oxygen minimum zone (cf.Jenkyns et al. 1991). Beds of siliceous limestone intercalated within shales, were deposited by fine-grained turbidites. The Skrile Formation records an early to middle Toarcian cycle (T6/R6 in Graciansky et al. 1998) (Fig. 4.1).The maximum transgression is represented by the most abundant intercalations ofsiliceous limestones in the lower part ofthe formation. At the same level, a peak in abundance of the radiolarian family Pantanelliidae was recorded, which may indicate the maximum development of eutrophic conditions (Gorican et al. 2(03). 

4.4 BAJOCIAN TO EARLY TITHONIAN: RAPID BAJOCIAN SUBSIDENCE AND SEDIMENTATION IN THE BOVEC TROUGH AND ON THE JULIAN HIGH 
In the Bajocian the sedimentation style of the study area was The Bovee Trough at this time deepened, and started to receive resedimented carbonates from the adjacent Dinaric (Friuli) Carbonate Platform. Additionally, the inner parts of theJulian deepened as well, and the sedimentation of the condensed Prehodavci Formation began in the We interpret this reorganization as a consequence of increased subsidence that occurred prior to the middle The accelerated subsidence pulse in the Bajocian is also documented westward in the Belluno Basin and on the Trento Plateau (Winterer & Bosellini 1981, Martire 1992, 1996, Winterer 199H).
In the Bovee Trough, a comprising at least the late Toarcian and Aalenian separates the Skrile Formation from the overlyingTravnik Formation. in the uppermost limestone beds of the Skrile Formation (section MAl, 
3.3) indicate sediment starvation. Moreover, a subsequent submarine erosion is evidenced by the reworked clasts of the older formation in the basal part of the Travnik Formation. This discontinuitysurface is correlative with the Mid-Cimmerian unconformity recorded in most of the European basin margins and structural intrabasinal highs (Jacquin & Graciansky 199R,Jacquin et aI., 199R). The diachronuous age of the base and different thicknesses of Member 1 of the Travnik Formation over very short distance indicates the existence ofa complex sea-bottom morphology in the Bajocian. Sediment bypassed more elevated areas (MAl section Fig. 3.3) and was trapped in lower, i.e. quieter areas (sections MA3 and MA4, Fig. 3.4). This sea-bottom morphology in the Bovec Trough was leveled by the Bathonian as evidenced by uniform thickness of Member 2 ofthe Travnik Formation. 
On the Julian High, the condensed limestone (Prehodavci Formation) directly overlies Lower Jurassic platform limestone. These started to accumulate in the Bajocian after a long periodof nondeposition. Similar stratigraphic gaps with a maximum from the Pliensbachian to lower Bathonian are common on submarine highs in the Mediterranean Tethys. They were documented on the Trento Plateau in the Dolomites (Winterer & 

4 Jumssir (lnd Crl'lacl'uus sedilfwnlm'Y (llid /Hlll'Ogmgm/'hir 0/I"f/l1li(1II Alps 
Bosellini 1981, Martire 1992, 1996, Baumgartner et al. 1995b, Clari et al. 1995, Clari & Masetti 2002), on the Sabina Plateau in the Apennines (Santantonio
1994, Santantonio etal. 1996, Santantonio & Muraro 2002), and on the submarine highs in Sicily (Di Stefano & Mindszenty 2000, Di et al. 2002, Baldanza et a!. 2002, Martire & Pavia 2004).These stratigraphic gaps are usually considered to have formed on more elevated areas of structural highs where current activity was strong enough to erode previously deposited sediments or totallyhinder sedimentation for a longer time span (e.g.Clari et a!. 1995).
The Middle and UpperJurassic deposits of the Bovec Trough are dominated by siliceous and carbonate background sediments (cherty limestones, cherts and siliceous limestones) and abundant platform derived carbonates that occur as coarse-grained debris-now deposits, coarse to fine-grainedturbidites, and oolitic megabeds.
In the Bajocian the Bovec Trough was characterized by the deposition of periplatform ooze and only a minor amount offine-grained turbidites (Member 1 of the Travnik Formation). These deposits may correspond to a flooding of the adjacentcarbonate platform due to the Bajocian transgression (T7 in Jacquin et al. 1998) and thus elevated 
transport of lagoonal mud (cf. Schlager et a!. 1994). In the upper part of Member 1 in the MA3 and MA4 sections (Fig. 3.4), a breccia OCCllrs and is correlative with the basal breccias ofMember 1 ofthe Travnik Formation in the MAl section (Fig.
The breccias contain many highly evolved glauconitic grains and reworked older lithoclasts. Some glauconitic grains still have preserved fractures on grain surfaces, indicating that they are probablyautochthonous and that they developed after the deposition ofthe breccia. Another possibility is that the grains were formed bef()re the deposition ofthe breccia and were later transported over relativelyshort distances (Odin & Fullagar 1988, Amorosi 1995, 1997). The reworked lithoclasts in the breccia document an important submarine erosion event cutting into the substratum down to the Sedlo Formation, which was probably exposed due to normal faulting. At the MAl section (Fig. this breccia level the basal part ofMember 1, whereas at and MA4 sections (Fig. 3.4) the breccia is intercalated within periplatform-ooze deposits. The formation of breccias thus cannot be simply a response to a major subsidence pulse in the Bajocian.The breccia could be related to the oversteepeningand back-stepping of the basin margin as a consequence of transgression (cf. Emery & Myers 1996) or could mark another extensional tectonic pulsecreating slope instability due to normal faulting.
In the Bathonian the thick oolitic beds of Member 2 ofthe Travnik Formation were deposited.They correspond to maximum ooid production on the adjacent platform. At that time the bioclastic limestone of the Lower Member of the Prehodavci Formation was deposited on theJulian High.
The upper Bathonian deposits of the Bovec Trough are marked by amalgamated successions of resedimented carbonates in the basal part of Member 3 ofthe Travnik Formation, mostly composed of coarse-grained breccias. Breccias contain lithoclasts of underlying deposits (the Sedlo Formation, and Members I and 2 of the Travnik Formation) that indicate exhumation of older strata. On the other hand, the basal breccias ofMember 3 represent the most proximal facies association ofthe Travnik Formation and are correlative with the late Bathonian lowstand (R7ITS inJacquin et a!. 1998). The breccias thus probably correspond to the late Bathonian lowstand. The late Bathonian lowstand is also recorded in the successions oftheJulian High, where in the bioclastic limestones ofthe Lower Member of the Prehodavci Formation form a distinct horizon with up to 10 cm large Fe-Mn nodules. 
At the Ravni Laz section (RI, Fig. 3.2) oftheJulian High the beds ofoolitic limestone conformablyoverlie the bioclastic limestone with Fe-Mn nodules. The oolitic limestone occurs within a typical condensed pelagic facies (Prehodavci Formation) and represents allochthonous gravity displaced deposits.A similar situation was reported from the Sabina Plateau in the Apennines where Santantonio and Muraro (2002) described up to 30 cm thick lenses of posidoniidloolite sediment on the top of the upper Bajocian Bugarone inferiore Formation. The occurrence of ooids on a prominent morpho-structural high is interpreted as a result of overbankingof a turbidity flow that traveled across the adjacentSabina Basin and impacted a huge obstacle represented by the marginal paleoescarpment of the plateau (Galluzzo & Santantonio 2002, Santantonio & Muraro 2002). We also believe that the occurrence of ooids within typical condensed limestones of the isolated Julian High can be explained in the same way. At the end of the Bathonian the eastern partof the Trento Plateau also started to receive ooids, however this case is different. Namely, by the end of the Bathonian, the Belluno Basin that separated the Trento Plateau from the Dinaric (Friuli) Platform was til1ed up to be level with the eastern margin of 

4 JllrrJssir and Crl'tlu:POns sf(limrntmy and IHl/I>O{!;PO{!;mllhir fvolution O/thPjlllilw AllIS 
the Trento Plateau (Bosellini et al. 1981, Winterer & Bosellini 1981, Clari & Masseti 2(02). Consequently,the Belluno Basin turned into a gentle slope connecting the Friuli Platform to the deeper Trento Plateau (Bosellini et al. 1981).
In the Bovee Trough the general thinning and fining upward trend from the upper Bathonian (Member 3) to Callovian-lower Oxfordian (lowerand middle part ofMember 4 of the Travnik Formation) corresponds to the second-order transgressionT8 ofJacquin et al. (1998) (Fig. 4.1). From the Bathonian upward the resedimented carbonates of the Bovec Trough also show a prominent increase in skeletal and concomitant decrease in ooidal content, finally resulting in beds composed exclusivelyof echinoderm fragments in the uppermost partof the Travnik Formation, as also observed in the coeval succession of the Belluno Basin (Bosellini et a!. 198 I ) . 
On the./ulian High, above the Fe-Mn nodules we observe a gradual change from high-energy bioclastic facies into the lower-eneq.,'Y light gray nodular limestone of the Lower Member of the Prehodavci Formation. This facies change reflects a weakeningof bottom currents during the aforementioned transgression (T8).
In the middle-late Oxfordian, the backgroundsedimentation in the Bovee Trough shows a prominent increase in clay admixture, resulting in the 2.5 m thick clay-rich package in the upper part of the Travnik Formation. We interpret this increased clay content as a consequence of a warm and humid climate in the Late Jurassic that enhanced weatheringand therefore increased clay input to the basins (Weissert & Mohr 1996, Thiry 2000, Picard et al. 2002).
In the successions of theJulian High, this level generally corresponds to a stratigraphic gap between the Lower and Upper Member of the Prehodavci Formation (Triglav Lakes Valley sections TV 1,2,3,5 and Ravni Laz: section RI). At Luznica Lake section (LJ) the red micritic marly limestone of the Middle Member of the Prehodavci Formation exists. A similar situation is present in an E-W oriented central belt of the Trento Plateau, where the middle Member of the Rosso Ammonitico Formation (RAM) is completely missing, while moving to the south, the RAM reappears (Martire 1996). On the basis of the geometry of RAM and numerous dykes,slides and seismites concentrated along the top of the Lower Member ofthe Rosso Ammonitico Formation (RAI) Martire (1996) concluded that after the uniform deposition of RAI the region was affected by an extensional tectonic phase, which generated a typical half graben structure. During the earlyCallovian to late Oxfordian the elevated areas were bypassed, and sediments were transported into lows and the deeper parts of slopes. It is also likelythat the observed irregular sea-bottom topographyof the Julian High controlled sedimentation. The Triglav Lakes Valley and Ravni Laz sections represented more elevated areas that were bypassed, while the Luznica Lake area was a low quiet area where sediment could be deposited. In the Oxfordian this effect may have been enhanced due to the higherinput of clay, which prevented early cementation and enabled the winnowing and bypass ofsediment in more elevated areas. However, apart from the irregular sea-bottom topography, there is no other evidence (dykes, seismites or slides) for the Callovian extensional tectonic event in theJulian High. So it is possible that this irregular sea-bottom topography was inherited and formed earlier, e.g. during Bajocian subsidence. This assumption is additionallysupported by the different thicknesses ofthe Lower Member of the Prehodavci Formation. 
In the Kimmeridgian and early Tithonian, the red nodular limestones of the Upper Member of the Prehodavci Formation were deposited on the Julian High, while at that time the Bovec Troughis marked by sedimentation of cherty limestones, cherts and siliceous mudstones with intercalations of fine to very coarse-grained calcarenites of Member 4 of the Travnik Formation. Of special interest are breccia bed and coarse-grained calcarenites in the uppermost part of the Travnik Formation. Theycontain large eroded clasts of underlying lithologies and also detritic grains of bytownite-anorthitefeldspars and represent the most proximal facies of Member 4 of the Travnik Formation. At this time the Julian High is marked by the development of neptunian dykes that cut the Upper Member of the Prehodavci Formation. At the Dm structural subunit at Mt. Mangart saddle (MA6) , Ravni Laz (RI) and Luznica Lake (LJ) sections, the dykes are filled with Kimmeridgian to lower Berriasian limestones, while at Triglav Lakes Valley (TVI) sections the correlative neptunian dykes also contain euhedral grainsof detritic quartz. The occurrence of breccia in the Bovec Trough and neptunian dykes on the Julian High coincides approximately with the onset of a compressive regime in the internal domains of the Dinarides (Chanell et al. 1979, Dimitrijevic 1982, Pamie 19R2, Karamata 19RR, Goriean 1994) and Hellenides (Baumgartner 1985) and with onset of the late Jurassic thrusting in the Northern Calcareous Alps (e.g. Gawlick et al. 1999). In the most external 

4 jumssir and C'PlfUPOI1S Sl'!lilllPIIlllly and jJfdl'llJ!;('oJ!;fIljillir ('<Iolulioll o/thl'jnlia/l Alp., 
domains of the Dinarides this event resulted in major uplift and emersion of the Dinaric (Friuli)Platform as evidenced by widespread bauxites overlain by Tithonian limestones with Clypeina jUfassica(Favre) (Dozet 1994, Dozet et al. 1996, Vlahovic et al. 20(5). Vlahovic et al. (2005) interpreted this facies variability ofthe Dinaric (Adriatic) Carbonate Platform as a consequence ofa new tectonic regime,characterized by inverse tectonics, since existinglineaments began to reactivate in order to adjust to compression/transpression. Similarly, we infer that the breccia and calcarenite in the upper partof the Travnik Formation and neptunian dykes in the Upper Member ofthe Prehodavci Formation are related to the onset ofconvergent plate movements in the Dinaric Tethys, that caused normal faultingand differential subsidence in pre-existing basins and swells in the external domains. 

4.5 LATE TITHONIAN TO EARLY APTIAN: PELAGIC SEDIMENTATION OF THE BIANCONE LIMESTONE 

At the early/late Tithonian boundary, the siliceous background sedimentation (cherts and chertylimestones of the Travnik Formation) in the Bovec Trough was replaced by carbonate backgroundsedimentation (Biancone limestone). A corresponding change is observed on the Julian High where the sedimentation of condensed limestones of the Prehodavci Formation is replaced by sedimentation of the pelagic Biancone limestone. The Biancone limestone resulted from normal pelagic sedimentation in a deeper-water environment. The nodular bedding present at places suggests the influence of sea-bottom currents that facilitated early selective cementation. Rare echinoderm grains indicate some limited input from shallower water areas. The Jurassic sea-bottom topography had become predominantly level by the end of the Jurassic as evidenced by the monotonous sedimentation of the Biancone limestone in the Julian High, Bovec Trough and Tolmin Basin (Buser 1986). However, the development ofdebris flows within the Biancone limestone at Vas na Skali indicate that some minor sea-floor topography still existed. 
The facies change from siliceous to calcareous background sedimentation is also observed in the Tolmin Tmugh (Cousin 1981, Buser 1986,1987),further south in the Dinarides (e.g. Gorican 1994), and in the Southern Alps (Weissert 1979, Winterer & Bosellini 1981, Baumgartner 1987, Baumgartner et al. 1995b, Bartolini et al. 1999). The only difference is that in the Dinarides this change is abrupt, while in the Southern Alps the change is gradual from the Oxfordian into the Lower Cretaceous. 
In theJulian Alps the jungest recorded age in the Biancone limestone is late Valanginian -earlyHauterivian (MAS section, Fig. 3.4) whereas in the Southern Alps (Trento Plateau, Belluno Basin) the deposition of the Biancone limestone may have persisted into the early Aptian (see Fig. 4.3, and chapter 5). In the studied sections, however, the transition to the overlying Scaglia variegata formation is never observed. In the Travnik structural unit, Triglav Lakes Valley, and Vas na Skali area the outcmp conditions do not allow observation of this transition. In the Mangart structural unit the situation is different (MA6, and MA7 sections), here the Biancone limestone is missing and Scaglia variegata or Scaglia rossa unconformably rest directly on the Lower Jurassic platform limestones cut by Jurassic neptunian dykes. 


4.6 ALBIAN TO EARLY CAMPANIAN: DEEPER-WATER SEDIMENTATION OF SCAGLIA V ARIEGATA AND SCAGLIA ROSSA 
The onset of sedimentation of the Albian Scagliavariegata postdates a tectonic phase in the earlyCretaceous (Buser 1989, 1996, Jurkovsek 1996)that caused a new tectonic reorganization of the investigated area, as evidenced by basal breccias and discontinuous contact with the underlyingdeposits. The area of the Julian Alps at that time deepened and became a part ofa deeper-water basin with the sedimentation of marls, cherts, siliceous limestones, and limestones with pelagic f()raminifers. The Scaglia variegata crops out only at section MA6 (Fig. 3.5a,b) in the Drn structural subunit of the Mt. Mangart saddle. Here the Scaglia variegataunconformably overlies the LowerJurassic platformlimestones penetrated by Kimmeridgian to lower Tithonian neptunian dykes. The contact is marked by basal breccias that contain chert clasts, which indicates erosion of the substratum. The obselved stratigraphical relationship is similar to that near Luznica Lake (Mt. Maselnik in Cousin 1981, Vol. 2, 
p. 496-497), where Albian variegated marls overlie coarse-grained breccias composed of platform

4 Jumssir: and Creta(e011S sedimentary and /mleogeograf)hir pvolution oftheJulian Alf)S 
limestone blocks embedded in a Kimmerid?;ianlower Tithonian pelagic matrix, that most probably represent neptunian dyke infill. The deposition of the Biancone limestone was probably re?;ionally uniform (see above), which implies that the Biancone limestone in the Drn structural subunit must have been completely removed by subsequent erosion. Another possibility for explaining the "anomalous" stratigraphy of the Drn structural subunit is that the pela?;ic Cretaceous deposits are draping and escarpment incised in the Lower Jurassic shallow water limestone penetrated by Jurassic neptuniandykes. These discontinuous pelagic thus seal a normal fault of pre-Sca?;lia age (cf. Martire & Montagnino 2002).
As previously mentioned, exposures of the Scaglia rossa are more common than those of the Scaglia variegata in theJulian Alps. The Scaglia rossa is characterized by deeper-water basinal sedimentation ofpela?;ic limestones with abundant ?;Iobotruncanids, calcareous turbidites and breccias that contain older deep-water deposits and also shallow-water elements transported from the aqjacent Dinaric Carbonate Platform. According to Buser (1987), and RadoiCic & Buser (2004) the maximum ran?;e ofthe Scaglia rossa is Cenomanian to Campanian (Buser1987). Scaglia Rossa usually unconformably overlies older strata. It rests either on the Triassic to Lower Jurassic platform limestones or onJurassic to earlyCretaceous deeper water strata (Cousin 1981, Buser 1986,1987,1989, I996,Jurkovsek 1987). In the study area (section MA7) the Sca?;lia rossa unconformablyoverlies Lower Jurassic platform limestones cut by
Jurassic neptunian dykes. The contact is erosional. We interpret that the onset of the deposition of Scaglia rossa followed a tectonic pulse in the Late Cretaceous, more precisely before the Senonian. Additional evidence of tectonic activity in the Late Cretaceous lies in the formation ofthe Upper Cretaceous neptunian dykes at the Ravni Laz section. Due to this tectonic reor?;anization, the Sca?;lia varie?;ata, Biancone limestone and condensedJurassic depositsof theJulian High were locally eroded. Since the Campanian or the Maastrichtian (Buser 1986, 1996,Jurkovsek 1986), flysch depositsstarted to fill the existing basin in the Julian Alps area, thus markin?; onset ofa compressional tectonic regime in this part of the Dinarides. 


5 




CORRELATION WITH NEIGHBORING AREAS 

Correlation of the areas is graphically shown in Fig. 4.3, for position of the paleogeographic units see Fig. 1.4 (the Siovenian Basin, ofFig. 1.4 is subdivided into a western (Bovee Trough) and a southern (Tolmin Trough) branch). 
5.1 CORRELATION OF THE BOVEC TROUGH WITH THE TOLMIN AND BELLUNO BASINS IN THE JURASSIC 

The succession of the Bovee Trough exposed in the Travnik structural unit at Mt. Mangart area is located in the region where the Southern Alpsoverlap with the Dinarides. The studied succession lies between the Tolmin Trough and the Belluno Basin and represents a possible paleogeographicconnection between them. The distinct feature ofall three previously mentioned basins are resedimented limestones ofMiddle and LateJurassic age that were transported from the Dinaric Carbonate Platform (Friuli Carbonate Platform). We therefore correlate the succession ofthe Bovee Trough with the successions of the Tolmin and Belluno basins. 
5.1.1 	CORRELATION WITH THE TOLMIN TROUGH 
The lower Jurassic platform limestone and the Pliensbachian Sedlo Formation ofthe Bovee Trough are time equivalents ofthe lower and middle Lower Jurassic Krikov Formation (Cousin 1970, 1981, Buser 1986, 1987), which contains deeper-water resedimented limestones with cherts. 
The Skrile Formation is correlative with the lower part ofthe Perbla Formation (Cousin 1973, 1981, Buser 1986, 1987) that consists mostly of shales. 
The Travnik Formation corresponds to a middle and upper part of the Perbla Formation (calcareous shales and siliceous limestones) and with radiolarites (black, green and red cherts) (Cousin 1973). Resedimented limestones are locally intercalated in the Perbla Formation and in the radiolarites but are much thinner than those of the Bovee Trough. Coarse to medium-grained resedimented limestones only occur in the most proximal settingsof the Tolmin Trough (Rozic 2003a, b) whereas distal parts are characterized only by fine-grainedcalcareous turbidites. 
The upper part of the Bovee Trough succession is marked by the Biancone limestone that is also present in the Tolmin Trough, thus indicatingregionally uniform pelagic sedimentation. The thickness of the Biancone limestone in the Tolmin Trough ranges from a few to 30 m (Buser 1986),however the sections are never complete, due to subsequent erosion. 
In the Bovec Trough the middle and upperCretaceous deposits are not preserved, but we suppose that they were similarly developed to those on theJulian High. Correlation of these deposits is discussed in chapter 5.3 below. 
The Bovee Trough and the preserved successiems of the Tolmin Trough are generally similar, however there are important differences: 
• 	
The Tolmin Trough was a deeper basin at the beginning of the Jurassic while the Bovee Trough was still a shallow water carbonate platform. 

• 	
The transition from the Krikov Formation to the Perbla Formation in the Tolmin Troughis continuous, while at the Bovee Trough the correlative boundary between the Sedlo and Skrile Formations is discontinuous and marked by a Fe-Mn hardground.

• 	
An important stratigraphic gap is recorded between the Skrile and the Travnik formations in the Bovee Trough, whereas the Tolmin Trough was characterized by continuous sedimentation at that time. 

• 	
The preserved successions of the Tolmin Trough contain less oolitic resediments (up to 25 m only) (Cousin 1981, Rozic 2003a, b) that were transported from the Dinaric Carbonate Platform. 



5 Cortplaliou wilh opighhOliug A,ms 
These differences suggest that the preselvedJurassic successions of the Tolmin Trough were more isolated from the Dinaric Carbonate Platform, and were fOl'med in a deeper sedimentaryenvironment, compared to the succession of the Bovec Trough. 

5.1.2 	CORRELATION WITH THE BELLUNO BASIN 

In the Bovee Trough the lower Jurassic platformdeposits are overlain by Pliensbachian deeper-waterlimestones of the Sedlo Formation. This mirrors the western part of the Belluno Basin where lower LowerJurassic Calcari Grigi are overlain by a chertylimestone of the Soverzene Formation (Masetti & Bianchin 1987) but differs from the central part of the Belluno Basin where the Soverzene Formation ranges down to the Hettangian.
The Skrile Formation is correlative to the Toarcian black shales, a member of the Igne Formation ofthe Belluno Basin (Masetti & Bianchin 1987). The early Toarcian Oceanic Anoxic Event was recorded in both areas. The Igne Formation is, however, much thicker, in general more calcareous, and also contains middle Toarcian and lower-?upper Bajociandeposits: limestones and dolomitic limestones with interbeds of marls and dolostones with chert layersand nodules (Bellanca et al. 1999, Clari & Masetti 2(02), while these deposits are completely missingin the Bovec Trough.
Resedimented limestones of Members 1, 2, and 3 of thc Travnik Formation are time and facies equivalents ofthe Vajont Limestone (Bosellini et al. 1981). The age ofthc Vajont Limestone has been a matter ofdebatc. On the basis ofcalcareous nannoplankton, Zempolich and Erba (1999) proposed an Aalenian to late Bajocian age, but Clari and Masetti (2002) assigned the Vajont Limcstonc to the late Bajocian to Bathonian. Our radiolarian data (Smuc& Goriean 2005) are consistent with the dates of Clari and Masetti (2002).
Member 4 of the Travnik Formation is correlative to the Callovian to lower KimmeridgianFonzaso Formation and overlying Ammonitico Rosso Superiore.
The Biancone limestone is present in both the Bovec Trough and the Bellul10 Basin (e.g. BaUlllgartner et al. 1995b, Clari & Masetti 2(02).
The Bovec Trough succession correlates well with the successions ofthe Bellul10 Basin. However, the resedimented limestones of the Formation are mllch thicker in the Bellul10 Basin (800 to 1000 m in most proximal sectors) than coeval Members 1-3 of the Travnik Formation of Mt. Mangart(42 m). This can be explained by paleobathymetry.The Mangart subsided block was located closer to the Dinaric Carbonate Platform and was topographically higher, which is also suggested by its relativelylate initial subsidence, conspicuous hiatuses and obvious sediment bypass within the Travnik Formation. On the other hand, in the Tolmin Trough the resedimented limestones with ooids are also very thin (25 m in most proximal areas). Oolite deposition on the platform was strongly controlled by surface currents (Bosellini et al. 1981). A windward positionof north-eastern margin of the Dinaric Carbonatc Platform tacing the Tolmin Trough is thus probable, so that most of the ooids were transported in south-western direction towards the Belluno Basin (Wright & Burchette 1996, p. 3(8).
Another important obselvation is that at the succession of the Bovec Trough, a thin layer of coarse-grained breccia composed of reworked basinal rocks and feldspars was found at the top of the Travnik Formation. This layer roughly correlatcs with the Fonzaso Formation/Ammonitico Rosso boundary. A similar breccia is not known in the Belluno Basin. 
5.2 	CORRELATION OF THEJULIAN HIGH WITH THE TRENTO PLATEAU IN THEJURASSIC 
The successions oftheJulian High are typical ofthe sedimentation on submarine structural highs and <u'c similar to the succession of the westward tilted Trento Plateau in the Southern Alps that belong-cd to the same passive continental margin (Bosellini et al. 1981, Winterer & Bosellini 1981, Martire 1989, 1992, 1996, Baumg-artner ct al. 1995b, 200 I, Clari & Masetti 2(02). The succession of theJulian Highis correlative with the succession of the central partof the Trento Plateau. 
The lower Jurassic platform limestones of the .Julian Carbonate Platform are time and facies equivalents ofthe lower and middle members ofthe Calcari Grig-i Formation (Clari & Masetti 2002).
On theJulian High the 10werJurassic platformlimestones are overlain by Bajocian Prchodavci Formation, marking a long stratigraphic gap. A correlative stratigraphic gap is present also on the Trento Plateau where it occurs between the Calcari Grig-i Formation and the Lower Member of the 

5 Corrr/alion wilh nfighbonng Arms 
Rosso Ammonitico Formation (Winterer & Bosellini 1981, Martire 1992, 1996, Baumgartner et a1. 1995b, Clari Masetti 2002). In the middle part of the Trento Plateau, the stratigraphic gap comprises the Toarcian to Bajocian, whereas in the other parts of the plateau the gap is shorter. In the western partof the plateau it comprises while at the eastern part the plateau time span of gap is middle Toarcian to Aalenian. 
The Lower Member of the Prehodavci Formation is partly time equivalent to the Lower Member of the Ammonitico Rosso Formation (RAI), which consists ofpseudonodular, mineralized and bioclastic limestones (cf. Martire 1992, 1996). The bioclastic limestone in the lower part ofthe Lower Member of the Prehodavci Formation contains abundant Fe-Mn nodules and encrustations and is therefore similar to the mineralized facies of the RAJ dated as Middle-Upper Bathonian (Martire 1992). The light gray nodular limestone in the upper part of the Lower Member of the Prehodavci Formation is devoid ofthe Fe-Mn mineralization and is marked bythe dominance ofbioclasts. It is the bcies equivalent to the bioclastic facies present in the upper part of the RAl. The light gray nodular limestone ofthe Prehodavci Formation is, however, younger (Callovian)compared to the bioclastic facies ofthe RAJ dated as lowermost Callovian (Martire 1992, 1996).
At the Ravni Laz section the three beds of resedimented oolitic limestones are intercalated between the bioclastic limestone and light graynodular limestone of the Lower Member of the Prehodavci Formation. Similar beds have not been found on the Trento Plateau. 
The red micritic, evenly bedded limestone of the Middle Member ofthe Prehodavci Formation is present only in one section (Luznica Lake section Ll) where it disconformably overlies a bioclastic limestone with Fe-Mn nodules. Due to the lack of diagnostic fossils, only a broad age assignment between the Callovian to the Kimmeridgian is possible.The red micritic limestone of the Middle Member of the Prehodavci Formation is a facies equivalent to the white to pink mudstones with radiolarian moulds found in the thin-bedded limestone facies of the Middle Member of the Rosso Ammonitico Formation (RAM). RAM was dated as Lower Callovian to Middle-Upper Kimmeridgian (Martire 1992, 1996, Beccaro 20(4). The Middle Member of the Prehodavci Formation is represented only by the red micritic limestone, while RAM consists of thin-bedded limestone and abundant chert and chertylimestone (Martire 1992, 1996,). No correspond
ing cherts and cherty limestones were found in the preserved sections of the.lulian High.
The upper Member of the Prehodavci Formation correlates with the Kimmeridgian to Tithonian Upper Member ofthe Rosso Ammonitico Formation (Martire 1992, 1996, Baumgartner et a1. 1995b).
The Biancone Limestone is present in theJulian High and the Trento Plateau. 
The successions of the Julian High arc in general similar with the successions of the Trento Plateau. The successions ofthe Triglav Lakes Valleyand Ravni Laz are similar to those successions in the middle part of the Trento Plateau, where the Middle Member of the Rosso Ammonitico Formation is missing. On the other hand the Luznica Lake section represents an anomalous section with its peculiar development of the Middle Member ofthe Prehodavci Formation that partly corresponds to the sections ofthe Trento Plateau where the Middle Member ofthe Rosso Ammonitico Formation is also present. The most important difference between the Julian High and the Trento Plateau is that in the successions of the Triglav Lakes Valley, the neptuniandykes with detritic quartz grains are present in the Kimmeridgian nodular limestones of the UpperMember of Prehodavci Formation. Similar dykes are not known on the Trento Plateau. 



5.3 	CORRELATION OF CRETACEOUS DEEPER-WATER DEPOSITS WITH THE TOLMIN AND BELLUNO BASINS, AND THE TRENTO PLATEAU 
The Albian to upper Cretaceous deeper-water deposits only crop out at the Mangart structural unit (01'11anel Mali Vrh structural subunits) of the Mangartsaddle. These sediments are correlative with the deeper-water deposits described from the Tolmin and Belluno basins, and the Trento Plateau. 
The Scaglia variegata deposits ofthe Dm structural subunit (MA6 section) are facies and time equivalent ofthe middle Cretaceous Lower flyschoidformation (Caron & Cousin 1972) of the Tolmin Trough, and to the Scaglia Variegata Formation in the Belluno Basin and Trento Plateau (e.g. Lehner 1992, Luciani & Cobianchi 1999) (Fig. In all of these areas a high input of clastics into basins is observed. In the Belluno Basin and in the eastern part of the Trento Plateau, the Scaglia VariegataFormation conformably overlies the underlying 

5 CO/,/f'/at;on with npighbming Arms 
Biancone limestone, while in the western sector of the Trento Plateau a sharp discontinuity surface marked by facies change, hardground and glaucony mineralization occurs between the Biancone limestone and the Scaglia Variegata (Lozar 1995).At the Drn structural subunit and in the Tolmin Trough the contact between the Biancone limestone and Scaglia variegata is also erosional. Thus the Biancone limestone in the mentioned areas is only partly preserved or, in places, is entirely missing(Caron& Cousin 1972, Buser 1986). The Lower fyschoid formation ofthe Tolmin Trough begins with calcareous breccias overlain by shales and marls with intercalated turbidites. The base of the formation is dated as Albian (or Aptian ?) and is therefore correlative with the basal breccia and calcarenite at the Drn structural subunit at Mt. Mangart. This impliesthat the early Cretaceous tectonic event that enabled the sedimentation of Albian deposits is regionallytraceable within the Julian Alps, and probably occurred within orjust prior to the Albian (Gorican& Smuc 20(4). The discontinuity surface between the Biancone limestone and the Scaglia Variegata in the western sector of the Trento Plateau is similarlyinterpreted as a consequence of an Aptian-Albian tectonic event (Lozar 1995). 
The Scaglia rossa deposits of the Mali Vrh subunit (MA7 section) are time equivalent of the red marls and pelagic limestones of the ScagliaRossa Formation in the Belluno Basin and Trento Plateau (cf. Lehner, 1992, Luciani & Cobianchi 1999), and deeper-water calciturbidites ofthe Voice limestone ofthe Tolmin Trough (Buser 1986, 1987, 1989, 1996).
The VoIce limestone, however, contains significally more shallow-water grains (Ogorelec et a1. 1976). These shallow-water grains originated from the south lying Dinaric Carbonate Platform (Ogorelec et a1. 1976, Buser 1996), thus indicating a more proximal position of the Tolmin Trough sections compared to the successions of the Bovec Trough.
The deposition of the Scaglia rossa in the Julian Alps followed a tectonic pulse in the Late Cretaceous. The Late Cretaceous tectonic event is also recorded on the margins ofthe Dinaric (Friuli)Platform. In the Coniacian-Campanian, the intense destruction of the northern margin of the Dinaric (Friuli) Platform started and the Tolmin Trough began to advance on the former platform (Buser 1989, 1996). Thus the Voice Limestone in places directlyoverlies shallow-water Upper Triassic and Jurassic limestones (Buser 1986, 1987, 1989, 1996). 

6 


CONCLUSIONS 

In theJurassic, theJulian Alps belonged to the passive south Tethyan continental margin and contain record ofrifting history, platform drowning and subsequent deeper-water deposition. The Jurassic and Cretaceous successions of the Julian Alps correlate with regional tectonics, eustatic sea-level changesand major paleogeographic changes as follows: 
1. 
Lower Jurassic plati(mll deposits of the Julian Alps were deposited on the Julian Carbonate Platform and represent a continuation of shallow-water sedimentation from the Late Triassic. Facies associations of shallow-water deposits are representative ofa carbonate platform with diverse hydrodynamic conditions. In the inner parts ofthe platform, tidal flat and lagoonal limestones were deposited, whereas the margins are marked with a high-energy sandbelt. In marginal parts small patchreefs thrived as well. 

2. 
In the Pliensbachian, shallow-water sedimentation on the Julian Carbonate Platform ended due to an extensional tectonic phase. At that time the platform was dissected into blocks with diflerent subsidence rates and two different paleogeographical domains formed: a deeper-water Bovec Trough(Travnik structural unit ofMt. Mangart saddle) and a pelagic plateau named theJulian High (Mangartstructural unit ofMt. Mangart saddle, Triglav Lakes Valley, Ravni Laz, Luznica Lake, C:isti Vrh, and Vas na Skali). In the Bovee Trough distal shelf deposits of the Sedlo Formation started to accumulate, while the Julian High may have been emergent at that time. 

3. 
The Fe-Mn hardground separating the Sedlo and Skrile formations in the Bovec Trough is interpreted to be the local record of the Pliensbachian/Toarcian lowstand. 

4. 
The black and brown shales, capped by the intensively bored limestones of the Skrile Formation record Toarcian transgressive/regressive cycle.

5. 
The accelerated subsidence in the Bajocian 


caused further deepening of the investigated area. The Bovec Trough at that time became a part of a deeper basin with sedimentation of the Travnik Formation which contains siliceous backgrounddeposits and resedimented carbonates from the adjacent Dinaric (Friuli) Carbonate Platform (TravnikFormation). Additionally, theJulian High deepenedand the sedimentation ofthe condensed Prehodavci Formation began in the Bathonian. 
6. 
Coarse-grained breccias capped by fine-grainedcalcarenites at the base of Member 3 of the Travnik Formation represent the most proximal facies association ofthe Travnik Formation and rdlect the late Bathonian lowstand. On the Julian High, the mentioned lowstand is recorded in the Lower Member of the Prehodavci Formation as a distinct horizon with up to 10 cm large Fe-Mn nodules. 

7. 
A middle-late Oxfordian increase in clay admixture in the Bovec Trough is a consequence of a warm and humid climate in the LateJurassic that enhanced weathering, thus increasing clay input to the basins. This level corresponds to the stratigraphic gap between the Lower and Upper Member of the Prehodavci Formation on theJulian High. 


R. The occurrence of Kimmeridgian/? lower Tithonian breccias. in the Bovec Trough and coeval neptunian dykes on the Julian High could be related to extensional tectonic movements duringthe initial stages of compression in more internal Dinaric domains. 
9. 
In the late Tithonian, the Jurassic sea-level morphology had become predominantly leveled as evidenced by monotonous sedimentation of the Biancone limestone in the Bovec Trough, Julian High, in the Tolmin and Belluno basins, and on the Trento Plateau. 

10. 
A tectonic phase in the Albian caused a new tectonic reorganization of the investigated area. The area of the Julian Alps at that time deepened 



(j COliriuS;OIlS 
and became a part of a deeper-water basin with sedimentation of Scaglia variegata. 
II. After a tectonic pulse in the Late Cretaceous, the deposition of the Scaglia rossa began. 
Comparison with the Tolmin and the Belluno Basin shows that the exposed sections of the Bovee Trough are similar to those in the marginal, western part of the Belluno Basin. In the earlyJurassic, the Tolmin Trough and most of the Belluno Basin were already deep-water basins while the Bovee Trough formed after of the Julian Carbonate Platform no earlier than in the early Pliensbachian. The preserved Middle to UpperJurassic successions of the Belluno and Tolmin 
basins were deposited in deeper basinal located more distally from the Dinaric (Friuli) Platform than the preserved successions of the Bovee Trough. Considering the present day facies distribution (Fig. 1.4), these facts indicate that the Belluno Basin and the Tolmin Trough were not continuous but were and, at least until the earlyEarlyJurassic, disconnected by a topographicrepresented by the area of the future Bovee Basin. The condensed successions oftheJulian High show good correlation with the successions of the Trento Plateau. They arc found to be most similar to the those parts of the Trento Plateau where the middle member of the Ammonitico Rosso (RAM) did not develop. The successions with development of the equivalent of the RAM are rare in theJulian Alps. 

7 

ACKNOWLEDGMENTS 

The Ivan Rakovec Institute of Paleontology ZRe SAZU, Scientific Research Centre SAZU, and Slovenian Research Agency are gratefully acknowledged for financial support. I'm much obliged to Kata Cvetko-Baric, who prepared thin-sections, to Milko, Petra, Grega, Miha, Bacci, Tone, and Pavle for their field assistance, and Rabel for his photos. I' am grateful to Irena Debeljak for determination of bivalves, to prof. JernejPavsic, prof. Joze prof. Luca Martire, and Adrijan KosiI' for thorough review of the manuscript, and Glenn Jaecks for English correction of the final text. 
I would especially like to express my sincere thanks to my mentor and friend Spela Gorican for her guidance in all stages of Illy study, for long constructive discussions and comments, for reviewing, radiolarian dating and everything else. I equally like to thank all my colleagues at the Institute of Palcontolof,"Y for their support. 

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