GEOLOGIJA 2011 | št.: 54/2 dodatek/supplement Bojan OGORELEC Mikrofacies mezozojskih karbonatnih kamnin Slovenije Microfacies of Mesozoic Carbonate Rocks of Slovenia GeoZS Geološki zavod Slovenije Geological Survey of Slovenia GEOLOGIJA 54/2 - dodatek / supplement doi:10.5474/geologija.2011.011 ISSN 0016-7789 ISSN 1854-620X Bojan OGORELEC Mikrofacies mezozojskih karbonatnih kamnin Slovenije Microfacies of Mesozoic Carbonate Rocks of Slovenia GeoZS GEOLOGIJA 2011 54/2 - dodat./suppl. 1-136 Ljubljana GEOLOGIJA ISSN 0016-7789 © Geološki zavod Slovenije Izdajatelj: Geološki zavod Slovenije, zanj direktor Marko Komac Publisher: Geological Survey of Slovenia, represented by Director Marko Komac Financirata Javna agencija za knjigo Republike Slovenije in Geološki zavod Slovenije Financed by the Slovenian Book Agency and the Geological Survey of Slovenia Vsebina dodatka je bila sprejeta na seji Uredniškega odbora, dne 2. 12. 2011. Manuscripts of the supplement accepted by Editorial and Scientific Advisory Board on December 2, 2011. Glavna in odgovorna urednica / Editor-in-Chief: Mateja Gosar Avtor / Authors: Bojan ogorelec Recenzenti / Reviewers: Bogdan Jurkovšek Jože Car Prevod I Translation: Lektura I Revision Matevž Novak Simon Pirc Matevž Novak Tehnična urednica / Technical Editor: Bernarda Bole Naslov uredništva / Editorial Office: GEOLOGIJA Geološki zavod Slovenije / Geological Survey of Slovenia Dimičeva ulica 14, SI-1000 Ljubljana, Slovenija Tel.: +386 (01) 2809-700, Fax: +386 (01) 2809-753, e-mail: urednik@geologija-revija.si URL: http://www.geologija-revija.si/ GEOLOGIJA izhaja dvakrat letno / GEOLOGIJA is published two times a year GEOLOGIJA je na voljo tudi preko medknjižnične izmenjave publikacij / GEOLOGIJA is available also on exchange basis Baze, v katerih je Geologija indeksirana / Indexation bases of Geologija: Directory of Open Access Journals, GeoRef, Zoological Record, Geoscience e- Journals Cena / Price Posamezni izvod / Single Issue Posameznik / Individual: 15 € Institucija / Institutional: 25 € Letna naročnina / Annual Subscription Posameznik / Individual: 25 € Institucija / Institutional: 40 € Tisk / Printed by: Tiskarna Formatisk d.o.o. Citiranje / example: Ogorelec, B. 2011: Mikrofacies mezozojskih karbonatnih kamnin Slovenije = Microfacies of Mesozoic Carbonate Rocks of Slovenia. Geologija, 54/2-suppl.: 1-136, doi:10.5474/geologija.2011.011. CIP - Kataložni zapis o publikaciji Narodna in univerzitetna knjižnica, Ljubljana 552.54:551.76.022(497.4) OGORELEC, Bojan Mikrofacies mezozojskih karbonatnih kamnin Slovenije = Microfacies of mesozoic carbonate rocks of Slovenia / Bojan Ogorelec ; [prevod Simon Pirc]. - Ljubljana : Geološki zavod Slovenije = Geological Survey of Slovenia, 2011. - (Geologija ; letn. 54, 2) ISBN 978-961-6498-29-6 258616832 GEOLOGIJA 54/2 - dodatek/supplement, 1-136, Ljubljana 2011 doi:10.5474/geologija.2011.011 Mikrofacies mezozojskih karbonatnih kamnin Slovenije Microfacies of Mesozoic Carbonate Rocks of Slovenia Bojan OGORELEC Geološki zavod Slovenije, Dimiceva ul. 14, SI-1000 Ljubljana; e-mail: bojan.ogorelec@geo-zs.si Ključne besede: mikrofacies, karbonatne kamnine, zgornji perm, trias, jura, kreda, Slovenija Key words: microfacies, carbonate rocks, Upper Permian, Triassic, Jurassic, Cretaceous, Slovenia Steklo tanko, kos apnenca, tanek snop svetlobe - čarovnija, nam pričara morje plitvo, plažo, ocean globine. Izvleček Karbonatne kamnine mezozojske starosti so v Sloveniji precej razširjene, saj zavzemajo kar okrog 40 % njenega ozemlja, njihova celotna skladovnica pa je debela preko 5000 metrov. V mikrofaciesu apnencev in dolomitov prepoznamo skoraj vse strukturne tipe, saj so nastajali v različnih sedimentacijskih okoljih, značilnih za karbonatne kamnine, tako v odprtih in zatišnih delih karbonatnega šelfa, lagunah in na obrežnih ravnicah, na različnih vrstah grebenov, pregibih in v bazenu. Večkrat so karbonatno sedimentacijo spremljali tudi dotoki terigenega materiala in produkti vulkanskih aktivnosti. Med diagenetskimi procesi raziskanih karbonatnih kamnin imata največji obseg dolomitizacija in okremenitev. V prispevku je predstavljenih 250 mikroskopskih posnetkov značilnih apnencev in dolomitov s slovenskega prostora. V uvodnem delu, v katerem so za orientacijo dodani shematski litostratigrafski stolpci, je na kratko predstavljen geološki razvoj karbonatnih kamnin. Zaradi celostnega prikaza »karbonatnega obdobja« so poleg mezozojskih plasti v pregledu zajeti tudi zgornjepermski apnenci in dolomiti. Abstract Carbonate rocks of Mesozoic age are widespread in Slovenia where they consitute about 40 % of its territory, and attaining total thickness of more than 5000 metres . With respect to microfacies almost all structure types can be recognized, the limestones and dolomites being formed in various sedimentary environments, such as in open and in restricted parts of carbonate shelf, in lagoons and on coastal plains, in different types of reefs, on slopes and in the basin. Carbonate sedimentation was often accompanied also by the supply of terrigenous material and products of volcanic activity. Among diagenetic processes in investigated carbonate rocks the most extensive are dolomitization and silicification. In the present text 250 microscopic photographs of characteristic limestones and dolomites from Slovenian territory are assembled. In the introductory part, to which for orientation schematic stratigraphic columns are added, the geologic development od these carbonate rocks is briefly outlined. For the sake of completeness in presenting the »carbonate era« in the overview, Upper Permian limestones and dolomites are also described next to Mesozoic beds. Vsebina / Contents UVOD ..................................................................................................................................................................................................................................................................................................................5 KRATEK PREGLED LITOLOGIJE IN RAZVOJA MEZOZOJSKIH KARBONATNIH KAMNIN SLOVENIJE ....................................................................................................................................................................................................................................................................................7 ZGORNJI PERM ....................................................................................................................................................................................................................................................................10 TRIAS ..................................................................................................................................................................................................................................................................................................................11 SPODNJI TRIAS ....................................................................................................................................................................................................................................................................12 SREDNJI TRIAS......................................................................................................................................................................................................................................................................15 Anizij....................................................................................................................................................................................................................................................................................................15 Ladinij................................................................................................................................................................................................................................................................................................15 ZGORNJI TRIAS ....................................................................................................................................................................................................................................................................17 Karnij ..................................................................................................................................................................................................................................................................................................17 Norij in retij..............................................................................................................................................................................................................................................................................19 JURA ....................................................................................................................................................................................................................................................................................................................20 Dinarska karbonatna plošča................................................................................................................................................................................................................................21 Slovenski bazen ........................................................................................................................................................................................................................................................................25 Julijska karbonatna plošča ....................................................................................................................................................................................................................................25 Vzhodne Alpe ................................................................................................................................................................................................................................................................................26 KREDA..............................................................................................................................................................................................................................................................................................................26 Dinarska karbonatna plošča................................................................................................................................................................................................................................26 Globljemorski razvoj ........................................................................................................................................................................................................................................................31 Vzhodne Alpe ................................................................................................................................................................................................................................................................................32 MICROFACIES OF MESOZOIC CARBONATE ROCKS OF SLOVENIA..........................................................................................33 LITERATURA - REFERENCES ............................................................................................................................................................................................................................45 TABLE - PLATES ..........................................................................................................................................................................................................................................................................57 Ob 50. obletnici izida klasifikacije karbonatnih kamnin (Folk 1962, Dunham 1962, Ham (ed.) 1962). UVOD Karbonatne kamnine mezozojske starosti gradijo okrog 40 % slovenskega ozemlja (Buser & Komac, 2002). V tej, preko 5.000 metrov debeli skladovnici apnencev in dolomitov, ki jih le mestoma prekinjajo klastične sedimentne kamnine, vulkaniti in piroklastiti, zasledimo skoraj vse facialne razvoje, značilne tako za plitvomorska karbonatna okolja kot za globljemorska okolja. Na majhnem prostoru je razvito celotno zaporedje sedimentnih kamnin v stratigrafskem razponu od devona do kvartarja. Ta raznolikost je v precejšnji meri posledica dejstva, da je slovenski prostor stičišče treh velikih geotektonskih enot -Alp, Dinaridov in Panonskega bazena. Intenzivna tektonska dogajanja, dviganje in spuščanje terena, so povzročila, da se lahko ob številnih prelomih in narivih stikajo različni razvoji posameznih formacij, istočasno pa s tem večkrat niso opazni bočni prehodi med različnimi okolji sedimentaci-je. V vsakem pogledu je naše ozemlje lahko »mala zbirka« razvojev mezozojskih karbonatnih kamnin na prostoru nekdanje zahodne Tetide. Čeprav iz naslova publikacije ni razvidno, zbrano gradivo presega okvire mezozoika, saj so vklju~eni tudi zgornjepermski apnenci in dolomiti. Ti so v objavo zajeti zato, ker se z njimi pričenja zvezna karbonatna sedimentacija na enoviti Slovenski plošči, ki je obstajala od zgornjega perma do sredine anizija (Buser, 1989). K pripravi monografije je avtorja vodila želja po predstavitvi rezultatov mikrofacialnih analiz več desetletnih raziskav apnencev in dolomitov slovenskega ozemlja. Te raziskave so v prvih letih potekale predvsem v sklopu izdelave Osnovne geološke karte SFRJ v merilu 1 : 100.000, ki je bila zaključena leta 1989, nadalje projekta Mezozoik v Sloveniji, v zadnjem času pa preko geoloških projektov v okviru nacionalnega raziskovalnega programa Javne agencije za raziskovalno dejavnost Republike Slovenije. Precej podatkov je bilo zbranih tudi pri raznih aplikativnih raziskavah, kot so raziskave rudišč živega srebra v Idriji ter svinca in cinka v Mežici, nadalje iz globokih geo-termalnih in naftnih vrtin, kamnolomov, predo- rov in cestnih usekov, v zadnjih letih pa tudi z raziskavami za novo Formacijsko geološko karto Slovenije v merilih 1 : 50.000 in 1 : 25.000. Težišče oziroma predmet predstavljene monografije je, kot pove njen naslov, mikrofacies. Medtem, ko ima pojem facies že dolgo zgodovino, odkar ga je sredi 19. stoletja, kot eno najbolj pomembnih definicij v geologijo uvedel Gressly (1838), pa je ime mikrofacies približno sto let mlajše. Prvi ga je leta 1943 predlagal Brown za tisti del kamnine, ki ga vidimo v preparatu pod mikroskopom. Kasneje se je ta pojem med geologi zakoreninil in močno razširil, še posebno po svetovnem naftnem kongresu v Parizu leta 1951, za kar je posebej zaslužen Cuvillier (1952, 1962). Danes pojem mikrofacies opisuje združbo vseh sedimentno-petrografskih in paleontolo-ških značilnosti v območju mikroskopskega merila preparata. Vezan je predvsem na karbonatne kamnine - apnence in dolomite. Kasneje so k poznavanju mikrofaciesa v svetu največ prispevali Carozzi (1960, 1989), Folk (1962) in Dunham (1962), slednja s klasifikacijama karbonatnih kamnin, Ham (1962) in Bathurst (1971), posebno pa Flügel (1978, 1982, 2004), ki je sistematično zbral vse dotedanje vedenje o mikrofaciesu in raziskovalnih metodah ter predstavil nove, poglede na praktičen pomen mikro-facialnih raziskav karbonatnih kamnin. Knjiga Microfacies of Carbonate Rocks (Flügel, 2004) je bogato dokumentirana s fotografijami značilnih fosilov pod mikroskopom. Nekaj predstavljenih vzorcev v teh publikaciji izvira tudi iz slovenskega prostora. Wilson (1975) je na osnovi Flüglovih idej (1972) izdelal in v prakso uvedel pojem standardni mikrofacies (SMF - Standard Microfacies Type), ki sloni na 24 osnovnih vrstah mikrofaciesa ter devetih značilnih okoljih nastanka karbonatnih kamnin. Poseben odmev je Wilsonova klasifikacija mikrofaciesa doživela v naftni geologiji in v računalniški informatiki sedimentnih kamnin. S sedimentacijskimi okolji in modeli karbonatnih kamnin so se v zadnjem obdobju poleg omenjenih avtorjev intenzivno ukvarjali še Milliman (1974), Reading (1978), James (1979), Scholle s sodelavci (1983), Tucker & Wright (1990), Bosellini (1991), James & Kendall (1992), Einsele (1992) ter drugi (npr. Elf-Aquitaine 1975; AGIP 1988). V Sloveniji se je pojem mikrofacies pojavil že dokaj zgodaj, saj ga že leta 1961 omenjata E. Flü- gel in A. Ramovš pri opisu zgornjetriasnega dach-steinskega apnenca z Begunjščice. Poudarek v tem članku je na opisu fosilne flore in favne ter na primerjavi z ustreznim apnencem v Severnih Alpah. Na žalost ta objava ni dokumentirana s slikami. Leta 1966 je Rajka Radoicic izdala za tisti čas, izvrsten in bogato ilustriran ter obsežen prispevek o mikrofaciesu jurskih plasti v Dinaridih, ki zajema tudi opise in slike več vzorcev apnencev iz južne Slovenije. Po tem začetku je pri študiju mikrofaciesa karbonatnih kamnin v Sloveniji prišlo do desetletnega zatišja. Apnenci so bili takrat predmet predvsem paleontoloških analiz in stratigraf-skih določitev v okviru Osnovne geološke karte (OGK). Močan zagon sedimentologiji in pri tem tudi mikrofacialnim raziskavam predstavlja obdobje po letu 1973, ko je zaživel projekt Mezozoik v Sloveniji. V okviru le-tega je prišlo do celovitih raziskav triasnih, jurskih in krednih formacij s težiščem na apnencih in dolomitih. Tovrstne raziskave so se sicer s formalno drugačnimi naslovi v okviru raznih projektov nadaljevale, tako da se je na Geološkem zavodu Slovenije v dvajsetih letih zbralo in preiskalo preko 25.000 mikroskopskih preparatov. Njihov izbor predstavlja potrebno osnovo in material za pričujočo publikacijo. V zbranem gradivu je prikazan le mikrofa-cies, ki ga prepoznamo v zbruskih apnencev in dolomitov slovenskega prostora. Makrofosili ter izolirana mikroflora in mikrofavna (npr. radio-lariji, konodonti, nanoplankton, pelodi in drugo) zato niso zajeti v slikovnem materialu, zelo skromno pa tudi v literaturi. Večina člankov in publikacij, ki so bile natisnjene v šestdesetih in sedemdesetih letih prejšnjega stoletja, obravnava litologijo, paleontologijo, regionalni razvoj ali stratigrafijo mezozojskih karbonatnih kamnin na slovenskem. Posebej to velja za tolmače k posameznim listom OGK 1 : 100.000. Več sedimento-logije je zajete v tolmačih k novejšim geološkim kartam, meril 1 : 50.000 (Jurkovšek et al., 1996) ali 1 : 25.000 (Jurkovšek, 2010; Čar, 2010), delno tudi v publikaciji Geological development in Slovenia and Croatia - Guidebook, ki je izšla ob priliki 16. evropskega mikropaleontološkega kon- gresa (Drobne,1979). Celovit in zgoščen prikaz biostratigrafije in litologije zgornjepermskih in mezozojskih kamnin je prikazan v Geologiji Slovenije (Plenicar, M., ogorelec, B. & Novak, M., ur., 2009) in sicer v poglavjih, ki zajemajo zgornji perm (Skaberne et al., 2009), trias (Dozet & Buser, 2009), juro (Buser & Dozet, 2009) ter kredo (Plenicar, 2009). Pregleden prikaz geoloških razvojev po geotektonskih enotah je zajet v delih S. BusERja (1979a), P. Mioca (2003) in U. PREMRuja (2005). Ko govorimo o faciesu karbonatnih kamnin, moramo omeniti tudi pregledne prispevke o njihovih facialnih razvojih (Plenicar & Pavlovec, 1984), o njihovih facialnih značilnostih (Plenicar & Premru, 1975), kamninah kot možnih matičnih plasteh za nastanek ogljikovodikov (Ogorelec et al., 1996) ter o njihovi izotopski sestavi (Ogorelec et al., 1999b). Osnovna namena publikacije sta dva. V prvi vrsti je ta namenjena študentom geologije, ki se prvič srečujejo s pojmom mikrofacies ter tujim raziskovalcem zaradi spoznavanja naših karbonatnih kamnin in njihove primerjave s sosednjimi ozemlji. Koristna pa bo lahko tudi drugim, saj mikrofacies v mnogočem povezuje sedimentologe s paleontologi, regionalnimi geologi in tektoniki. Zaradi boljše preglednosti gradiva je v uvodnem delu podan zgoščen litološki opis celotne skladovnice mezozojskih in zgornjepermskih kamnin v Sloveniji. Gradivo je vsebinsko razdeljeno po geoloških obdobjih, pri čemer je težišče publikacije slikovno gradivo z 250 fotografijami mikroskopskih preparatov. Uvodni tekst, dopolnjen z nekaterimi litološkimi stolpci ter literaturo, predstavlja le potrebno ogrodje, da kamnine postavimo v čas in prostor. Tuja literatura je zelo okrnjena, citirana samo zaradi primerjave karbonatnih kamnin slovenskega s sosednjima, alpskim in dinarskim prostorom. Glede na to, da prihaja do tiska pričujoče publikacije prav ob 50. obletnici za karbonatno sedimentologijo pomembnega dogodka, namreč izida enega temeljnih del petrografije apnencev in dolomitov - Klasifikacije karbonatnih kamnin (Ham, 1962), se avtor na ta način pridružuje praznovanju tega jubileja. Narava vedno eno iz drugega ustvarja in nič ne nastane prej, predno drugo ne preide. (Titus Lucretius Caro (99-55 pnš. -»De rerum natura«) KRATEK PREGLED LITOLOGIJE IN RAZVOJA MEZOZOJSKIH KARBONATNIH KAMNIN SLOVENIJE Po odložitvi kopenskih klastičnih kamnin, je prostor Slovenije v zgornjem permu zajela obsežna transgresija morja in začela se je sedimenta-cija karbonatnih kamnin. Ozemlje je bilo vse od zgornjega perma do sredine anizija sestavni del enotne, plitve karbonatne plošče, poznane kot Slovenska plošča (Buser, 1989), ki se je raztezala še v Furlanijo, Istro in na prostor Panonskega bazena. V aniziju je ta plošča razpadla in se razdelila na Dinarsko karbonatno ploščo na jugu in Julijsko karbonatno ploščo na severu, ločil pa ju je Slovenski bazen (cousiN, 1973; Buser, 1989). Karbonatna sedimentacija se je v večjem ali manjšem obsegu na obeh ploščah nadaljevala vse do zgornje krede, ko je prišlo do razpada Dinarske karbonatne platforme in nastanka več vmesnih flišnih bazenov. Na sliki 2 je prikazan litološki razvoj zgornje-permskih in mezozojskih karbonatnih kamnin v posameznih paleogeografskih enotah - na Dinarski in Julijski karbonatni plošči, v Slovenskem bazenu ter posebej v Severnih Karavankah, ki ležijo severno od Periadriatskega lineamenta. Na sliki 3 so shematsko predstavljena njihova sedimentacijska okolja. Zaradi močne tektoni-ke in z njo povezane narivne zgradbe slovenskega ozemlja, so lahko odnosi med posameznimi litološkimi enotami in geološkimi formacijami prikazani le shematsko. Skladi Dachsteinskega apnenca na Kaninu Dachstein limestone on Mt. Kanin V zadnjem času se kot približni sinonim za Dinarsko karbonatno ploščo uporabljajo izrazi Karbonatna platforma zunanjih Dinaridov (Grandi} et al., 1999), Jadransko-Dinarska karbonatna platforma (Gu{i} & Jelaska, 1993) ali enostavno Jadranska karbonatna platforma (Gusi} & Jelaska, 1990, Veli} et al., 2002; Vlahovi} et al., 2005; Jež, 2011), glede na to, da je bila to največja karbonatna plošča na Jadranski mi-kroplošči v obdobjih jure in krede. V pričujoči monografiji še vedno uporabljam »star« izraz Dinarska karbonatna plošča. Sl. 1. Pregledna in poenostavljena geološka karta Slovenije (priredil M. Plenicah) Fig. 1. Simplified overview geological map of Slovenia (adapted by M. Plenicar) Sl. 2. Shematski prikaz razvoja zgornjepermskih in mezozojskih plasti v različnih paleogeografskih enotah Slovenije. Apnencev in dolomitni razvoj sta naznačena z barvami (po podatkih Osnovne geološke karte 1 : 100.000 (večji del), po literaturnih podatkih in po podatkih lastnih raziskav). Fig. 2. Schematic depiction of Upper Permian and Mesozoic beds development in various paleogeographic units of Slovenia. Limestone and dolomite development are shown in colours (adapted mainly according to the Basic Geological Map 1 : 100,000, literature and personal research data). Sl. 3. Sedimentacijska okolja zgornjepermskih in mezozojskih karbonatnih kamnin v Sloveniji Fig. 3. Sedimentary environments of Upper Permian and Mesozoic carbonate rocks in Slovenia V nadaljevanju slede zelo zgoščeni opisi lito-logije po posameznih geoloških obdobjih s poudarkom na karbonatnih formacijah in njihovih mikrofacialnih ter diagenetskih značilnostih. Glede na to, da so triasne plasti v Sloveniji najbolj razširjene ter istočasno tudi najbolj pestro razvite, jim je v monografiji namenjenega največ prostora. ZGORNJI PERM Zgornjepermske plasti so v Sloveniji zastopane s karbonatnimi kamninami. Litološko so precej pestro razvite. V zahodnem delu Posavskih gub - med Ljubljano, Škofjo Loko in Idrijo dosežejo debelino do 250 metrov. Tod prevladujeta plastovit, temno siv do črn apnenec in laporast apnenec nad dolomitom, vmes pa se večkrat pojavljajo tanke pole skrilavega laporovca. Po kraju Žažar pri Vrhniki so poimenovane kot Žažarska formacija (Ramovš, 1958), ki je ekvivalent Belero-fonski formaciji v Alpah (Heritsch, 1934; Buser et Značilni mikrofacies algnega apnenca Žažarske formacije. Zgornji perm. Dolina Idrijce pri Masorah. Merilo 1 mm Characteristic algal limestone facies of Žažar Formation. Upper Permian. Idrijca valley at Masore. Scale 1 mm al., 1988; Kolar-Jurkovšek et al., 2011). V vzhodnem delu Posavskih gub, pri Laškem, Izlakah, Sevnici in na Bohorju so zgornjepermske plasti debele le do nekaj deset metrov in so razvite pretežno dolomitno. V bazalnih plasteh, tik nad klastiti Grodenske formacije, vsebujeta apnenec in dolomit še precej terigene primesi kremena in sljude. Apnenec je v splošnem izredno bogat s fosili, predvsem s skeletnimi algami, ehinodermi in foraminiferami. Delež karbonata v apnencu se giblje med 85 in 97 %. V Južnih Karavankah je zgornjepermsko zaporedje razvito dolomitno, kot Karavanska formacija, ki je debela do 300 metrov (Buser et al., 1988). Za spodnji del te formacije je značilen do 80 m debel paket satastega dolomita (Rauhwacke). Sedimentacijsko okoje zgornjepermskih plasti je bil zelo plitev in zaprt šelf z lagunami in sabkami, ki je imel povezavo s širšim prostorom Tetide. Na to kaže univerzalna flora in favna in- doarmenskega tipa. Za zaprti šelf in lagune so značilni različki algnega biomikritnega apnenca tipa packstone, za sabke pa satasti dolomiti in evaporitni minerali, od katerih sta zastopana sadra in anhidrit. V biomikritnem apnencu so prisotne forami-nifere (Agathamina sp., Glomospira sp., Hemi-gordius sp., Reichelina sp., Climacammina sp., Geinitzina sp., Ammovertella sp., Ichtyolaria sp., Staffella sp.), skeletne alge Gymnocodium bellerophontis, Vermiporella nipponica, Permo-calculus fragilis, Velebitella triplicata, Mizzia ve-lebitana, M. cornuta), brahiopidi, ehinodermi in polži (Bellerophon sp.), lokalno pa se pojavljajo še manjše kopuče koral vrste Waagenophyllum indicum (Ramovš, 1958, 1986a; Buser et al., 1988; Skaberne et al., 2009). Permsko-triasna (P/T) meja je zaznamovana z nenadnim izginotjem številnih fosilnih vrst, predvsem alg in foraminifer ter s spremembo izotopske sestave ogljika v apnencih in dolomitih. Spodnjetriasni karbonati so obogateni z do 5 %o lažjim izotopom ogljika kot zgornjepermski (Dolenec T. et al., 1995, 1999a,b,c, 2004). Tik pod P/T mejo se ponekod pojavlja tanjša plast oolit-nega apnenca (Dolenec, M. & Ogorelec, 2001; Dolenec, M. 2004), ki jo lahko primerjamo s Te-sero horizontom v Alpah (Assereto et al., 1972). Paleontološko je bila P/T meja v Sloveniji v zadnjih letih dokazana na osnovi konodontne cona-cije (Kolar-Jurkovšek & Jurkovšek, 2007; Kolar--Jurkovšek et al., 2011) in foraminifer (Nestell et al., 2011). Takoj nad permsko/triasno mejo je značilna drobna foraminifera Earlandia. Med diagenetskimi procesi, ki so zajeli zgor-njepermske karbonatne kamnine, ima daleč največji obseg dolomitizacija, v manjši meri pa sta prisotni še okremenitev in dedolomitizacija. Ob dedolomitizaciji je prišlo v plasteh z evaporitnimi minerali do izločanja epsomita, kar je lepo vidno v idrijskem rudniku živega srebra. Pretežni del dolomita je zgodnjediagenetske-ga značaja in je nastal po evaporitnem modelu dolomitizacije (Shinn & Ginsburg, 1964). Na ari-dno klimo v zgornjem permu kažejo poleg sadre in ahidrita tudi izotopske analize 518O (Polšak & Pezdic, 1978; Dolenec T. et al., 1981; Ogorelec et al., 1999b) ter visoke vsebnosti Na+ za karbonate (Ogorelec & Rothe, 1979). Obdobje zgornjega perma je bilo zaradi specifičnih sedimentacijskih razmer in klime ugodno za nastanek stratiformnih rudišč svinca in cinka. Taka nahajališča so pogosta v vzhodnih Posavskih gubah in sicer v vrhnjem delu zgornjepermskega zaporedja (Puharje pri Šoštanju, Iskra, 1969) ter na meji med zgornjim permom in spodnjim tria-som (Mokronog, Bohor, Ledina pri Sevnici, Dro-venik et al., 1980). Zgornjepermske plasti slovenskega prostora imajo v splošnem enak ali zelo podoben mikrofa-cies kot ga kažejo apnenci in dolomiti iste starosti na sosednjih ozemljih - npr. v Karnijskih Alpah (Buggisch, 1974; Buggisch et al., 1976; Holser & Schonlaub, 1991; Magaritz & Holser, 1991; Noe, 1987), v Dolomitih (Bosellini & Hardie, 1973), na Sl. 4. Litološki stolpci zgornjepermskih plasti v Sloveniji (Buser et al.,1988) Fig. 4. Lithological columns of Upper Permian beds in Slovenia (Buser et al., 1988) Sl. 5. Litologija in izotopska sestava karbonatnega ogljika na permsko-triasni meji v profilu Masore pri Idriji. Opazen je izrazit padec 513C na meji (Dolenec, T. et al., 2004) Fig. 5. Lithology and stable isotope composition of carbonate carbon across the Permian-Triassic boundary in the Masore section at Idrija (Dolenec, t. et al., 2004) Velebitu (Kochansky-Devidé, 1979; sremac, 1991, 2005) in na Madžarskem (Haas, 2001; Haas et al., 2004, 2006). TRIAS Triasne kamnine so v Sloveniji med vsemi najbolj razširjene, saj zavzemajo skoraj eno četrtino njenega ozemlja in skupno debelino celo do 3800 metrov (Buser, 1979), pri čemer karbonatne kamnine močno prevladujejo nad klastičnimi in piroklastičnimi različki (sl. 2). Kažejo izredno pestro litologijo z značilnostmi alpskega razvoja znotraj Tetide, podobnega ali enakega tistemu v Severnih Alpah. V spodnjem triasu je karbonatno sedimenta-cijo na plitvem šelfu spremljal dotok terigenega, večji del drobnozrnatega materiala s kopnega, v spodnjem aniziju pa so karbonati povsem prevladovali. Koncem anizija (Buser, 1989), na Idrijskem pa že v srednjem aniziju (Čar, 1985, 2010), se je pričela Slovenska karbonatna plošča zaradi intenzivne tektonike diferencirati, na Dinarsko karbonatno plo{~o na jugu in Julijsko karbonatno plo{~o na severu z vmesnim Slovenskim bazenom (sl. 6). Ta je na prostoru osrednje Slovenije obstajal vse do sredine jurske periode, ko se je razširil še na ozemlje Julijske karbonatne plošče, proti Dinarski karbonatni plošči pa je obstajal vse do konca krede. Podrobnejši opisi paleogeografskega razvoja triasa na celotnem prostoru Slovenije, paleotek-tonike in biostratigrafske razčlenitve so podani predvsem v delih: Buser, 1979, 1980b, 1988, 1996; Sl. 7. Bahamski šelf z osrednjim globokim jarkom, oceanskim jezikom (Tongue of the Ocean - TOC). Dimenzije tega jarka lahko primerjamo s Slovenskim bazenom, ki je v času od anizija do zgornje krede potekal preko osrednje Slovenije (http:// www.keysdisease.blogspot.com/) Fig. 7. Bahama shelf with the central Tongue of the Ocean trough (TOC). Its size is comparable to the Slovenian basin which existed in the central part of Slovenia from Anisian to Upper Cretaceous (http://www.keysdisease.blogspot.com/) Sl. 6. Današnji položaj geotektonskih enot v zahodni in osrednji Sloveniji in razširjenost sedimentov nekdanje Jadranske in Dinarske karbonatne plošče ter Slovenskega bazena (Buser, 1996, Buser et al. 2007). Fig. 6. Actual position of geotectonic units in western and central Slovenia with extent of sediments of the ancient Julian and Dinaric carbonate platforms and the intermediate Slovenian basin, respectively (Buser 1996, Buser et al., 2007). Dozet & Buser, 2009; Premru, 1980, 1982, 2005; Buser et al., 2007, 2008; Placer, 2009. Recentni primer, kako je izgledal in bil oblikovan tak paleogeografski prostor na Slovenskem v času triasa imamo na Bahamskem otočju (sl. 7), kjer sicer enotno, zelo plitvo karbonatno ravnico razdvaja do 900 metrov globok jarek Tongue of the Ocean. Po dimenzijah nekaj sto kilometrov ga lahko primerjamo z nekdanjim Slovenskim bazenom. Na sl. 8 je shematski prikaz litološkega razvoja triasnih kamnin v Sloveniji z izbranimi strati-grafskimi stolpci. SPODNJI TRIAS (induanij in olenekij) Debelina spodnjetriasnega zaporedja je dokaj različna. Giblje se med 40 in 500 metri, v Južnih Karavankah pa doseže tudi do 600 metrov (Buser, 1980a). Plasti so na celotnem slovenskem prostoru južno od Periadriatskega lineamenta precej enotno razvite. V spodnjem delu zaporedja, ki je debelo do 250 metrov, se menjavajo kla-stiti in karbonati, posebej pa na terenu izstopajo oolitne plasti. Dolomit in apnenec spodnjega dela spodnjega triasa, imata zaradi primesi terigene-ga kremena in sljude peščen izgled. Nekarbonatni delež mestoma doseže tudi 50 %. Klastite sestavljajo rdečkasti glinavci, laporovci in meljevci. Apnenec je po sturkturi največkrat biomikrit ali pelmikrit. Odlagal se je v zelo plitvem, zatišnem delu šelfa, ki je imel občasno značilnosti lagun in litorala. Večkrat je popolnoma ali delno dolomi-tiziran, značilne zanj pa so tudi bioturbacijske teksturne oblike. Tanjše leče ter gnezda sadre in Tuf tufit, apnenec z roáencem konglomerat, peščenjak, keratofir Tuff, limestone w. chert nodules, conglomerate, sandstone, keratophyr Siv biomikritni. sparitni in stromatolitni dolomit Gray biomicritio, sparitic and str amatol ithic dolomite Litoral - littoral Temno siv biomikritni lapornat apnenec Dark gray biomicritic marly limestone Zaprti šelf - restricted shelf Svetlo siv dolomit Light gray dolomite Litoral - littoral Meljast skrilavec, peščenjak, plasti ooiltnega apnenca Sllty shale and sandstone, layers of oolithic limestone Klastični litoral in oolitne delte Clastic littoral & oolithic deltas Dolomit z detrltično primesjo Dolomite, detritic admixture Črn biomikritni apnenec, redke pole skrilavca Black biomicritic limestone, shale intercalations Zaprti šelf - restricted shelf Temeo mikcrtm dolomit. satast dolomit Dark irie t c dolomite. cellular dolomite Litorai- littoral Rdeč peščenjak, skrilavec in konglomerat Red sandstone, shale and conglomerate Rečno okolje - fluvial env. Sl. 9. Shematski stolpec zgornjepermskih in spodnjetriasnih plasti na Žirovskem (Ogorelec & Grad, 1986) Fig. 9. Schematic column of Upper Permian and Lower Trias-sic beds of Žiri area (Ogorelec & Grad, 1986) anhidrita kažejo na lokalne in občasne evaporit-ne pogoje sedimentacije. Na idrijsko-žirovskem ozemlju je v najvišjem delu spodnjetriasnega zaporedja razvit t.i. pasnati apnenec (Mlakar, 1969; Kolar-Jurkovšek et al.; 2011). Spodnjetriasni oolitni dolomit. Hematitni pigment je obarval ooide rdečkasto. Rimske Toplice. Merilo 1 mm Lower Triassic oolitic dolomite. Owing to hematite pigment ooids are of reddish colour. Rimske Toplice. Scale 1 mm Ooliti so nastajali v medplimskih kanalih in deltah, kjer je bila energija okolja višja. Značilna zanje je rdečkasta barva, kot posledica hema-titnega pigmenta. Jedra ooidov je večkrat zajela kasnodiagentska dolomitizacija, ki se kaže v do 300 ^m velikih dolomitnih romboedrih. Med ooidi so pogosto pomešane ploščice ehinodermov ter drobne hišice polžev, opisanih kot vrsti Natica gregaria in Holopella gracilior, večkrat pa so prisotne tudi drobna zrna kremena in sljude. V vrhnjem delu spodnjetriasnega zaporedja se delež terigene komponente zmanjšuje. Prevladuje temnejši biomikritni ali pelmikritni laporasti apnenec (mudstone do packstone) nad svetlejšim dolomitom. Med fosili so zastopane foraminifere, v nekaterih plasteh so številni ostrakodi, ploščice ehinodermov in drobne školjke, prisotni pa so tudi konodonti (Kolar-Jurkovšek & Jurkovšek, 1995, 1996, 2007). Za stratigrafijo tega dela spod-njetriasnih plasti, je med foraminiferami najbolj pomembna Meandrospira pusilla. Severno od Periadriatskega lineamenta, posebno v okolici Črne na Koroškem, so spodnje-triasne plasti razvite pretežno klastično, glede na to, da pripada prostor Severnih Karavank vzhod-noalpskemu geotektonskemu bloku. Razvite so kot peščenjaki, skrilavi meljevci in konglomerati tipa »Buntsandstein« (Mioc, 1983) in so brez fosilnih ostankov (Štrucl, 1971). Spodnjetriasne plasti slovenskega prostora kažejo v velikem delu enak ali zelo podoben mi-krofacies, kot ga imajo kamnine iste starosti na sosednjih ozemljih - npr. Werfenske plasti v Severnih Alpah (Mostler & Rossner, 1984), v Karnijskih Alpah (Holser & Schonlaub, 1991), v Dolomitih (Assereto et al., 1972), na Madžarskem (Nagy, 1968; Haas, 2001), na avstrijskem delu Južnih Karavank (Anderle, 1970), na Svilaji v dalmatinski Zagori (Šcavnicar et al., 1983; Jelaska et al., 2003) in drugod, kar kaže na zares obsežno in enotno sedimentacijsko okolje v času spodnjega triasa. - a' ° t3 ^ 0 n" ft H M S3 1 0 « 0 3 ? >0 o -M o - S 't? K CD a n o b n a n a ft ft D h ft a (M g % g H £ " P H S a m J rt 2 ^ P - rt CO KI co L; Cft I K -H o" S H M H ^ B 0) O K O 0 O m ^ g =3 n < s ^ S 5n ^ T3 , o >g > § £ CO 5 S u ^ ä s ■ * K _ o r av >N g I > M Ö £ 1 CO m cn so-e M , d I ^ I 00 ^ 1—1 e B H rt CM -M (D O s g H H m g P S GO H 'H D B MOD d OS M tn r lje o o li ¡.¿¡Mcu as n 1 - h 00 co ft - S H S S H K ce rl le O fc I p! « K >M >0 EH O S S >š p H or Ü o a k o 00 1n S i- J co co O Cft CO D ^ < ' K o3 j i: 0 O B O - O O o3 Si e M H m - > O * s D 1-5 s 8 N K p ^ O P csi - rt ' H £ S Ü o 0 P J rt P4 o ^ CD ^ Cu le tu p tu - >0 ' o M . 00 ■f com co »o O H-o O p i: — J s 8 ^ o , o ^ o s £ M ° e v oa ol e Ph O ' cs e v o o 3 ^ no -R M , CO Q 0 EH < >0 & X o 00 P o ft a la ij bl ri rb cd t "s - o M cq H , O M K ^ D m h? ° < ^ CQ fc^ § p w 03 ^ >0 M O P > ea m cq •c 1 o M a e t3 2 ft M a n n ri rt i ^ 1 rt a k> cc w M 1 ^ co c^ M t- « M H P^ ¡> > M M P3 o i: - - ko H o3 K M ^ O > ^ ^ ^ - sco C- CQ co H c^ m 55 ^ H >s« ■ m ' D M « K D « K PS $ ' iä CS ^ S rt ft e '«i o ^ ^ ss ph U b ČL o 0 t c^S n a v o ft ' >0 tu ^^ i - u I 5o ft, M o O H CO S CO O cn O ^H o . , M ' N rt ft ki s ns k a P 'G ft o3 J ä fc^ 1 > K UO e o M M O S M P S « - E^ ; tu M 1 js nj e - tu > o 1 ol t fc J >M ^ > - o K M S P M ^ -1 ^^ J i-i S =3 a rt < > t» rt is p w K g o3 o tr a a rt 0 ¡d M K SREDNJI TRIAS Anizij Anizijske plasti so v Sloveniji razvite precej enotno, večji del kot plastovit dolomit, ki kaže pogoste znake medplimske sedimentacije s stro-matoliti in izsušitvenimi porami (Grad & Ogore-lec, 1980; Dolenec et al., 1981). Apnenec je razvit v manjšem obsegu kot biomikrit. Med fosili prevladujejo foraminifere (Meandrospira dinari-ca, Pilammina densa, Glomospirella irregularis, G. grandis, G. semiplana, Trochammina sp.), mestoma so prisotne tudi alge (Physoporella pau-ciforata). V severnem delu Julijskih Alp je med Mojstrano in Kranjsko Goro ohranjen masiven grebenski apnenec, ki ga gradijo predvsem alge in trombolitne tvorbe (Ramovš, 1987). Enak razvoj kaže tudi grajska stena nad Blejskim jezerom (Flügel et al., 1993). Debelina anizijskih plasti doseže do 600 metrov. Meandrospira dinarica v stromatolitnem dolomitu z izsušitvenimi porami. Anizij. Zakamnik nad karavanškim cestnim predorom. Merilo 1 mm Meandrospira dinarica in stromatolitic dolomite with shrinkage pores. Anisian stage. Zakamnik above Karavanke highway tunnel. Scale 1 mm Severno od Periadriatskega lineamenta izda-nja v Topli pod Peco plastovit dolomit, ki je oru-den s svinčevimi in cinkovimi minerali (Strucl, 1974). Nad njim leži temen mikritni apnenec z gomolji roženca. Sredi anizija je Slovenska plošča pričela razpadati. Tako se je sedimentacija od srednjega triasa dalje odvijala na treh geotektonskih enotah v različnih okoljih. Na širšem Idrijskem je prišlo do lokalnih okopnitev in nastanka debelejših konglomeratnih in peščenih plasti (Čar & Čadež, 1977; Čar, 2010). Za globlji razvoj anizija, kakršnega poznamo v Karavankah pri Tržiču, na Idrijskem in v vzhodnih Posavskih gubah, so značilni amoniti in konodonti (Kolar-Jurkovšek, 1983, 1991). Ladinij Ladinijske plasti so litološko med najbolj pisanimi, saj se hitro menjavajo različni litološki tipi. Izdanjajo na več krajih v osrednji Sloveniji, Sl. 10. Poenostavljen prikaz paleogeografskega razvoja v Sloveniji v obdobju med anizijem in koncem triasa s položajem koralno-spongijskih grebenov (Turnšek et al., 1984) Fig. 10. Simplified sketch of the paleogeographic development in Slovenia from Anisian to the end of Triassic with position of coral-sponge reefs (Turnšek et al., 1984) na širšem Idrijskem in Cerkljanskem, v predgorju Julijskih Alp in v Karavankah, v večjem obsegu pa severno od Periadriatskega lineamenta, predvsem na pogorju Pece. Rezultat intenzivne tektonike v času idrijske tektonske faze (Buser, 1980b) je močna razko-sanost ozemlja v osrednji Sloveniji. V globljih jarkih je prišlo do vulkanskih izlivov spilitno-ke-ratofirske asociacije (bazalti, kremenovi kerato-firji, porfir,...) ter sedimentacije njihovih tufov in tufitov (Buser, 1979; Dozet & Buser, 2009). Nekateri tektonski bloki so okopneli, na kar kažejo debele plasti pobočnih breč in konglomeratov. V Južnih Karavankah in v delu Julijskih Alp je to Ugoviška breča (Buser, 1986b; Jurkovšek, 1987), na Idrijskem pa konglomerat med Idrijo in Rov-tami ter Stopniški konglomerat (Mlakar, 1969; Čar & Čadež, 1977; Čar & Skaberne, 2003; Čar, 2010). Na Dinarski in Julijski karbonatni plošči so se zaradi občasne povezave z bazenom lokalno odlagali temni apnenci z roženci in vmesnimi plastmi tufov, v osrednjem delu Slovenskega bazena pa Psevdoziljske plasti, za katere je značilno menjavanje temnih skrilavih glinavcev, peščenjakov in tufov; apnenci so podrejeni. Apnenec je po strukturi ponavadi biomikritni mudsto-ne ali wackestone, med fosili pa so poleg tankih lupin mehkužcev zastopani predvsem konodonti (Kolar-Jurkovšek, 1983, 1991; Kolar-Jurkovšek & Placer, 1987; Placer & Kolar-Jurkovšek, 1990; Kolar-Jurkovšek & Rižnar, 2006) in radiolariji (Gorican, 1997; Gorican & Buser, 1990; Skaberne et al., 2003). Med makrofosili so pomembni amo-niti in školjke (Jurkovšek, 1983, 1984; Ramovš & Jurkovšek, 1983; Ramovš, 1989). V piroklastitih najdemo na Idrijskem tudi manjše grebenske kope (čar, 2010). V Kamniško-Savinjskih Alpah je iz zgornjega ladinija zanimiva Korošiška formacija. Leži nad zrnatim dolomitom in zelenim tufom. Apnenec je rahlo bituminozen, črn biomikrit z gomolji ro-ženca. Med fosili so prisotne školjke (Jurkovšek, 1984), amoniti in skeleti rib ter plazilcev (Celarc, 2004a; Celarc & Žalohar, 2010). V Severnih Karavankah je na območju Mežice obstajal v času ladinija in cordevola preko 1000 metrov debel kompleks masivnega, mestoma plastovitega apnenca in dolomita, znanega kot Wettersteinski apnenec (Štrucl, 1970, 1971). Najbolj značilen tak masiv je pogorje Pece. Apnenec je oruden s cinkovo in svinčevo rudo (Štrucl, 1971, 1984; Brigo et al., 1977; Drove-nik et al., 1980). Spodnji del Wettersteinske formacije je bolj masiven in kaže grebenski razvoj s koralami in hetetidami (Turnšek, 1997; Bole, 2002), njen vrhnji del, ki je že cordevolske starosti, pa se je večji del odlagal v medplimskem okolju odprtega šelfa in vsebuje pogoste stromatolitne in loferitne plasti. Proti jugu prehaja Wettersteinski apnenec v temne glinavce in laporovce z redkimi polami apnenca. Te plasti, znane kot Partnaška formacija, so nastajale v zaprtem in nekoliko globljem delu šelfa. Mestoma so v tem paketu prisotne tudi leče in gomolji evaporitnih mineralov, predvsem sadre (Strucl, 1971; Mioc 1973). ZGORNJI TRIAS Karnij Karnijske plasti so najbolj razširjene v zahodni Sloveniji. Znotraj njih stratigrafsko ločimo plasti cordevolske, julske in tuvalske podstop-nje. Zastopane so v plivomorskem in globlje-morskem razvoju. Celotno karnijsko obdobje je trajalo 14 milijonov let. V novejšem obdobju se pojem cordevolska pod-stopnja opušča (celarc, 2004b; Lucas et al., 2010), ker naj bi te plasti po fosilni združbi pripadale že spodnjemu delu julske podstopnje. Glede na poseben, bolj grebenski facies masivnega apnenca in dolomita, kakršen je poznan iz obdobja najnižjega dela karnija v Sloveniji, in glede na tradicijo pri izdelavi Osnovne geološke karte, pa je cordevol-ska podstopnja v pričujoči monografiji ohranjena še kot samostojna stratigrafska enota. Kamnine cordevolske starosti so razvite le karbonatno, večji del kot svetel, masiven zrnat dolomit, v katerem je prvotna struktura kamnine ohranjena le poredko. Po fosilih, predvsem dazi-kladacejskih algah in koralah sklepamo, da predstavlja cordevolski dolomit nekdanje grebene, katere je kasneje intenzivno zajela dolomitizaci-ja. Apnenci cordevolske starosti grade večji del Mežakle in Pokljuke v Julijskih Alpah (Ramovš, 1988; Ramovš & Turnšek, 1984; Turnšek & Buser, 1989) ter obsežne predele v Kamniško-Savinjskih Alpah (Krvavec, Velika planina, Menina - Pre-mru, 1974, 2005; Ramovš & Sribar, 1993; Celarc 2004a; Žalohar & Celarc, 2010), v manjših krpah pa se pojavljajo tudi na Idrijskem, prostoru med Cerknim in Ljubljano ter v vzhodnih Posavskih gubah. Zaradi paleozakrasevanja in lokalnih emerzij (Buser, 1980b) je apnenec večkrat obarvan rdečkasto in vsebuje žepe rdeče gline in boksita. Tak apnenec je zanimiv kot okrasni kamen. Pridobivajo ga v kamnolomih Hotavlje in Lesno Biosparitni apnenec s preseki alge Diplopora annulata. Corde-vol. Usivec na Veliki planini. Merilo 1 mm Biosparitic limestone with Diplopora annulata algae. Corde-volian substage. Usivec on Velika planina. Scale 1 mm Močno okremenjen sparitni dolomit. Vzorec je z dna najgloblje vrtine v Sloveniji (Ljut-1 pri Ljutomeru, 4025 m). Domnevno triasna starost. Merilo 1 mm Sparry dolomite, intensely silicified. Sample from the bottom of the deepest borehole in Slovenia (Ljut-1 at Ljutomer, 4025 m). Presumably Triassic age. Scale 1 mm Brdo pri Vrhniki (Ramovš, 1995, 2000). V dolomitu in apnencu so na vseh omenjenih območjih med fosili najbolj pogoste skeletne alge (Diplopora annulata, Diplopora annulatissima, Gyroporella ladinica), ki so mestoma kamenotvorne (Ramovš, 1988, 1992; Dozet, 1979, 2004; čar, 2010). Poseben, plastovit razvoj dolomita poznamo na Vojskarski planoti v Zgornji Idrijci in v Gač-neku, kjer v 40 metrov debelem profilu zasledimo teksture, ki so značilne za litoralno medplimsko okolje (čar, 2010). Na območju Severnih Karavank se je v cor-devolu nadaljevala sedimentacija plastovitega apnenca in dolomita v vrhnjem delu Wetterstein-ske formacije. Debelina cordevolskega dolomita in apnenca je lahko precej različna in doseže v različnih tektonskih enotah Slovenije od nekaj deset do 600 metrov. Kamnine julske in tuvalske podstopnje so pestro, pretežno karbonatno razvite. Med apnenci in dolomiti se pojavljajo plasti laporovca ter vložki klastitov in tufov. Njihova debelina znaša med 100 in 400 metri. Klastiti in tufi ima- Biomikritni apnenec s foraminiferami in školjčnimi lupinami. Značilen facies plasti julsko-tuvalske starosti. Črna voda v Tamarju. Merilo 0,5 mm Biomicritic limestone with foraminifers and bivalves. Characteristic facies of Julian-Tuvalian beds. Črna voda in Tamar valley. Scale 0.5 mm jo od severa proti jugu na Dinarski karbonatni plošči vedno večji obseg, tako da na Idrijskem in Kočevskem že prevladujejo nad karbonati (Cigale, 1978; Dozet, 1990a). V nasprotju s cordevolskim dolomitom, so se julske in tuvalske plasti odlagale na zaprtem plitvem šelfu, pogosto v lagunah. Temna barva apnenca in piritni pigment kažeta na redukcijske razmere v sedimentacijskem okolju. Apnenec je pogosto laporast in ima mestoma budinaža-sto teksturo. Delež organske snovi se v poprečju giblje okrog 1 % in doseže največ do 4 %, njen izvor pa je večji del terestričen (Ogorelec et al., 1996a). Po strukturi je apnenec mikriten in bio-pelmikriten tipa mudstone do packstone, med fosili pa prevladujejo tankolupinske školjke (Jelen, 1990; Jurkovšek, 1994), skeletne in neskeletne alge (Poikiloporella duplicata, Clypeina besici), ostrakodi in drobne foraminifere (Nodosaria ordinata, Glomospira sp., Diplotremina astrofimbria-ta, Lamelliconus multispirus, Ammodiscus para-priscus, Frondicularia pupiformis) (Oblak, 2001) ter školjke vrste Triadomegalodon idrianus (Čar, 2010). Na nekoliko bolj razgibano okolje kažejo posamezni ooidi in onkoidi. Apnenec je pogosto zajela tako zgodnje- kot poznodiagenetska dolo-mitizacija ter karstifikacija z žepi in plastmi boksitov (Dozet, 1979, 2004; Buser, 1980b). Vrhnji del julskega in tuvalskega zaporedja je pogosto zastopan s sivim dolomitom, med katerim so redke plasti laporovca, mestoma pa tudi več metrov debele plasti tufskega glinavca. Ta dolomitni paket postopno preide v svetlejši, pla-stnat dolomit brez vmesnih lapornih pol, v Glavni dolomit. Starost tega dolomita je določena z do nekaj cm velikimi megalodontidnimi školjkami, foraminiferami, algami (Poikiloporella duplicata) ter konodonti (Kolar-Jurkovšek, 1991). Poseben razvoj julsko-tuvalskega zapored-j a so Amfiklinske plasti, ki so na Cerkljanskem in v Baški grapi debele do 250 metrov (Buser, 1986b). Zanje je značilno menjavanje temno sivega do črnega laporastega biomikritnega apnenca, skrilavega laporovca, kremenovega peščenjaka, apnenčevih konglomeratov ter tufov in tufitov. V tem kompleksu se na širšem Cerkljanskem pojavljajo na več mestih od nekaj pa do 40 metrov debeli grebeni (Senowbari-Daryan & SchAfer, 1979; Čar et al. 1981; Turnšek et al., 1984), katere gradijo predvsem spongije in v manjši meri korale (Turnšek, 1997). Po teksturnih značilnostih apnencev in po postopni zrnavosti v plasteh sklepamo na sedimentacijo Amfiklinskih plasti na pregibnem delu karbonatnega šelfa proti Slovenskemu bazenu (Turnšek et al., 1984). V Julijskih Alpah opazujemo tako plitvomor-ski kot globljemorski razvoj julskih in tuvalskih plasti. Plitvomorski razvoj opazujemo npr. v Tamarju in Logu pod Mangartom (Ogorelec et al., 1984; Jurkovšek, 1987). Apnenec, ki je biomikri-ten (wackestone do packstone), vsebuje številne skelete foraminifer, drobnih megalodontidnih in drugih školjk ter ploščic ehinodermov; večkrat je dolomitiziran. Pogosto je laporast (do 15 % ne-karbonatne primesi, večinoma glina in organska Sl. 11. Razvoj karnijskih plasti v mežiškem rudišcu in Helenski grapi pod Peco (prirejeno po Pungartniku in sod., 1982). Fig. 11. Development of Carnian beds in Mežica mine and Helena gorge at the foot of Mt.Peca (adapted after Pungartnik et al., 1982). snov). Za globljemorski razvoj je značilen gost biomikritni apnenec z gomolji roženca. V favni prevladujejo tankolupinske školjke, kalcitizira-ni radiolariji in naplavljene ploščice ehinoder-mov (Ogorelec et al., 1984; Jurkovšek 1987). V teh plasteh so bili na Kozji dnini pod Triglavom najdeni fosilna riba Birgeria sp. (Jurkovšek & Ko-lar-Jurkovšek, 1986), črv Valvasoria carniolica (Kolar-Jurkovšek & Jurkovšek, 1997) in številni drugi fosili (Dobruskina et al., 2001; Bitner et al., 2010), v zahodnih Karavankah pa alga Clypeina besici (Kolar-Jurkovšek & Jurkovšek, 2003), makroflora (Dobruskina et al., 2001), foraminifere in konodonti (Kolar-Jurkovšek et al., 2005). Julske in tuvalske plasti so v Severnih Karavankah pri Mežici zastopane z do 350 metrov debelim zaporedjem apnenca in dolomita (sl. 11), ki je razvito v 20 ciklotemah loferskega tipa, značilni zanje pa so trije klastični horizonti skrilavca, me-ljevca in laporovca (Štrucl, 1970, 1971; Pungart-nik et al., 1982). Klastične horizonte povezujemo z evstatičnimi fazami in humidnim klimatskim sunkom, znanim kot CPE (Carnian Pluvial Event - Kolar-Jurkovšek & Jurkovšek, 2010). Nekatere plasti so izredno bogate s fosili (Jurkovšek 1978; Jurkovšek & Kolar-Jurkovšek, 1997; Kaim et al., 2006; Jurkovšek et al., 2002; Kolar-Jurkovšek & Jurkovšek, 2009, 2010). Na bolj razgibano okolje znotraj plitvega šelfa kažejo posamezne oolitne plasti in onkoidi. Norij in retij Kamnine norijske in retijske starosti so v Sloveniji zastopane v treh razvojih. Na obeh karbonatnih ploščah, Julijski in Dinarski, se pojavljata Glavni dolomit in njegov lateralni različek Dachsteinski apnenec, v Slovenskem bazenu pa sta razvita Baški dolomit in Železnikarski apnenec (sl. 13). Glavni dolomit in Dachsteinski apnenec zavzemata precejšen obseg in sta najbolj razprostranjeni formaciji v Sloveniji. Gradita pretežni del Julijskih Alp, velik del Notranjske, severni del Trnovskega gozda in del Dolenjske. Kompleks Glavnega dolomita je debel med 800 in 1300 metri, prav toliko pa je lahko debel tudi Dachsteinski apnenec. Apnenec je v večjem delu razvit na Julijski platformi, medtem ko na Dinarski karbonatni platformi prevladuje dolomit. Debelina Baškega dolomita je tri do štirikrat tanjša in je ocenjena na največ 400 metrov (Buser, 1986b). Dachsteinski apnenec je debeloplastnat in kaže značilen loferski razvoj, kakršen je poznan iz Severnih Alp (Fischer, 1964; Zankl, 1971; Piller & Lobitzer, 1979; Piller, 1981), Dolomitov (Bosel-lini, 1967; Bosellini & Rossi, 1974) ali Madžarske (Haas, 1994). Posamezne cikloteme (sl. 12) sestavljajo do 2 metra debele plasti biomikritnega in biosparitnega apnenca, katerega prekinjajo tanke stromatolitne in loferitne plasti ter lokalno tudi medplastovne breče z glinenim vezivom. Med fosili so najbolj pogoste foraminife-re (Triasina hantkeni, Aulotortus gr. sinuosus, A. permodiscoides, A. friedli, Miliolipora cuvil- Sl. 12. Različni tipi ciklotem v Dachsteinskem apnencu na Krnu (Ogorelec & Buser, 1997) Na levi je klasična loferska ciklotema po Fischerju (1964). 1 - megalodontide; 2 - korale in onkoidi; 3 - apnenec z izsušitvenimi porami (loferit); 4 - laminit; 5 - stromatolit; 6 -tempestitne plasti (»nadplimski konglomerat«); 7 - korozijske votline; 8 - emerzijska breča z rezidualno karbonatno glino Fig.12. Various types of cyclothems in the Dachstein limestone on Mt. Krn, Julian Alps (Ogorelec & Buser, 1997). Classical Lofer cyclotheme after Fischer (1964) is on the left. 1 - Megalodontids; 2 - Corals and oncoids; 3 - Limestone with shrinkage pores (loferite); 4 - Laminite; 5 - Stromatolite; 6 -Tempestite layers (»flat pebble conglomerate«); 7 - Solution cavity; 8 - Emersion breccia with residual carbonate clay Loferitni dolomit z izsušitvenimi porami prerašča stromato-litna plast, nad njo pa je mikritni dolomit. Značilen facies medplimskega okolja. Dachsteinski apnenec, norij. Grudnica nad Slapom ob Idrijci. Merilo 1 cm Loferitic dolomite with shrinkage pores, overgrown by stromatolite layer and micritic dolomite. Characteristic facies of the intertidal environment. Dachstein limestone, Norian. Grudnica above Slap ob Idrijci. Scale 1 cm lieri, Galeanella sp.), alge (Macroporella retica) in ehinodermi. V nekaterih plasteh so velike me-galodontidne školjke kamnotvorne. Dachsteinski apnenec se je odlagal na plitvem, odprtem in priobrežnem šelfu, z občasnimi medplimskimi in nadplimskimi pogoji (Ogorelec, 1988; Ogorelec & Rothe, 1992; Dozet & Ogorelec, 1990). Plasti, Sl. 13. Shematski paleogeografski prikaz sedimentacijskih okolij v noriju in retiju na ozemlju zahodne Slovenije Fig. 13. Schematic paleogeographic presentation of sedimentary environments during Norian and Rhaetian in Western Slovenia ki so se odlagale v litoralnem okolju, so večkrat dolomitizirane. Na Julijski karbonatni plošči se znotraj formacije Dachsteinskega apnenca pojavljajo večji grebenski masivi (Begunjščica, Pokljuka, Bohinj) ali manjši grebeni z bogato koralno favno (Turnšek & Ramovš, 1987; Turnšek & Buser, 1991; Turnšek, 1997). Občasno je na obeh, Dinarski in Julijski karbonatni plošči prišlo do kratkotrajnih okopnitev njunih posameznih delov. V takih primerih se je razvil paleokras. Slednji je posebno lepo razvit na Kaninskem pogorju in na Krnu (Babic, 1980/81; Ogorelec & Buser, 1996). Enako favno in mikrofacies, kot ju opazujemo v gre-benskem apnencu slovenskega dela Alp, kažejo tudi norijsko-retijski grebeni v Severnih Alpah (Zankl, 1971; Flügel, 1981; Piller, 1981; Stanton & Flügel, 1989; Flügel & Koch, 1995; Turnšek et al., 1999). Glavni dolomit kaže monoton, popolnoma dolomiten razvoj. Zanj je značilno ciklično menjavanje debelejših dolosparitnih in biomikrit-nih plasti s tanjšimi stromatolitnimi plastmi, loferiti, mestoma tudi z nadplimskim konglomeratom in emerzijskimi brečami. Med fosili so zastopane velike megalodontide, foraminifere in alge. Lokalno so prisotne tudi plasti in leče z onkoidi in vadoznimi pizoidi (Ogorelec, 1988; Dozet, 1991). Glavni dolomit se je, sprva kot apnenec, odlagal na zelo plitvem zaprtem šelfu z obsežnimi medplimskimi ravnicami, v plitvejšem delu šelfa kot Dachsteinski apnenec. Dolomi-tizacija je bila zgodnjediagenetska z »evaporative pumping« modelom (Illing et al., 1965), kasneje pa je kamnino zajela še kasnodiagenetska dolo-mitizacija. Tudi dolomit kaže večkrat znake pa-leozakrasevanja. Manjše in večje korozijske votline zapolnjuje conarni sparitni cement, večkrat je vmes tudi rdeč interni mikrit. V istem obdobju, ko sta se odlagala na platformi Dachsteinski apnenec in Glavni dolomit, sta v bazenu in njegovem obrobju nastajala Ba{ki Korozijska votlina s kokardno teksturo sparitnega kalcita nakazuje paleozakrasevanje. Dachsteinski apnenec v Smrekovi Dragi na Trnovskem gozdu. Merilo 5 cm Solution cavity filled with sparry calcite of cockade textu-reindicating paleokarstification. Dachstein limestone from Smrekova Draga on Trnovski gozd. Scale 5 cm dolomit in Železnikarski apnenec (Buser, 1979; Ramovš, 1970; Gale, 2010). Karbonatni sediment v obeh formacijah je mikriten, z zelo redkimi fosili, drobnimi foraminiferami (Rožic, 2006, 2008; Rožic & Kolar-Jurkovšek, 2007; Buser & Ogorelec, 2008; Rožic et al., 2009; Gale, 2010) in konodonti (Kolar-Jurkovšek, 1982, 1991, 2011), značilne za obe formaciji pa so vmesne plasti in gomolji roženca. JURA Prostor Slovenije je, enako kot v srednjem in zgornjem triasu, tudi v juri pripadal trem geotek-tonskim enotam, ki istočasno predstavljajo tudi različna sedimentacijska okolja. Južna Slovenija je bila sestavni del Dinarske karbonatne plošče, za katero sta značilni plitvomorska sedimentacija in velika debelina karbonatnih kamnin, ki v juri Zakrasel jurski apnenec. Kolk na Trnovskem gozdu Karstified Jurassic limestone. Kolk on Trnovski gozd dosežejo preko 1500 metrov (Buser, 1989; Buser & Dozet, 2009). Na severu je karbonatno ploščo omejeval Slovenski bazen, severno od njega pa je obstajala Julijska karbonatna plošča. Ta je v dog-gru razpadla, tako da se je bazen razširil tudi na ta prostor. Dinarska karbonatna plošča Prehod zgornjetriasnega Glavnega dolomita in Dachsteinskega apnenca v jurske plasti ni oster. Ponekod je na kontaktu razvit do nekaj deset metrov debel paket intraformacijske breče (npr. Čepovan, Grčarevec), ki je nastala v kratkotrajnih emerzijskih fazah (Buser, 1979b; ogorelec & Rothe, 1992; Jurkovšek et al., 1996). Stroma-toliti, ki so značilni za Glavni dolomit, postopno izginjajo, še vedno pa so v spodnjeliasnih plasteh pogoste teksturne oblike litoralnega okolja - izsušitvene pore in razpoke, nadplimski konglomerat in laminiti (ogorelec 1988, 2009; orehek & ogorelec, 1979, 1980; Dozet, 1992a, 1998). V srednjem in zgornjem liasu ter doggru opazujemo različna okolja znotraj karbonatnega šelfa (Buser, 1979b; orehek & ogorelec, 1979, 1981; Strohmenger & Dozet, 1990, Dozet, 1992a,b). Na Trnovskem gozdu, Hrušici, Logaški planoti in na Gorjancih se je sedimentacija odvijala na odprtem delu šelfa z višjo energijo. Prevladujejo oolit-ni apnenci (Buser, 1973,1978; Strohmenger et al., 1987; ogorelec & Dozet, 2000), ki lahko dosežejo debelino tudi več sto metrov. Med njimi se ponekod pojavljajo plasti z velikimi onkoidi. Lokalno so pogoste litiotidne školjke, ki gradijo lumakele (Buser, 1978; Buser & Debeljak, 1996, Debeljak & Buser, 1998; Ramovš, 2000). Med fosili, ki jih opazujemo v zbruskih spod-njejurskih - liasnih plasti, sta pomembni algi Paleodasycladus mediterraneus in Sestrospha-era liasina, med foraminiferami pa so določene vrste Orbitopsella praecursor, Involutina liassi-ca, Agerella martana, Trocholina turris, Pseudo- Sl. 15. Spodnjeliasne plasti v Preserju pri Borovnici (Ogorelec, 2009) Fig.15. Lower Liassic beds in Preserje near Borovnica (Ogorelec, 2009) : o3 a d e h n e v lo Sl v n a k ih ni t a n a n o b a k a g a k p e h M o3 M • " m 1—1 —j K « a ti dc oe po s i c imi hi rni raph ug z h mo im p ski e afs th gra th m Sl ni in a i ss >M 10 pq p ?? ® -M 9) lil l., e ocS S ! >o >o Oolitni apnenec. Spodnjeliasne plasti v Preserju pri Borovnici. Merilo 1 mm Oolitic limestone from the Lower Liassic succession in Pre-serje at Borovnica. Scale 1 mm Ol 00 M Onkoidi v zgornjeliasnem apnencu. Prelaz Vahta na Gorjancih. Merilo 5 cm Oncoidal limestone of Upper Liassic succession. Vahta pass on Gorjanci Mts. Scale 5 cm cyclammina liassica in Haurania deserta (Šribar, 1979a in podatki iz različnih tolmačev k Osnovni geološki karti 1 : 100.000). Številni so tudi, sicer za stratigrafijo manj pomembni, primerki alge Thaumatoporella parvovesiculifera, ehinodermi, mikrogastropodi, školjke, ostrakodi, mestoma pa tudi drobni brahiopodi. V doggerskih plasteh sta določeni foraminifera Mesoendothyra croati-ca in alga Selliporella donzelli. Na Hrušici in na Trnovskem gozdu so poredke kopuče koral in plasti krinoidnega apnenca. Na Notranjskem nastopa v spodnji in srednji juri temno siv biomikritni in pelmikritni apnenec, ki kaže na sedimentacijo v bolj zatišnih in zaprtih delih šelfa z lagunami in občasno redukcijskimi pogoji (Orehek & Ogorelec, 1981). Večkrat se med apnencem pojavljajo leče zrnatega dolomita. Na Kočevskem zasledimo mestoma tudi tanjše plasti premoga (Dozet, 1998). Debelina spodnje-in srednjeliasnih plasti znaša 200 do 400 metrov, zgornjeliasnih in doggerskih pa prav tako do 450 metrov (Buser, 1979b). V spodnjem malmu se je preko Trnovskega gozda, ki je v tem času predstavljal severni rob Dinarske karbonatne plošče, vlekel več deset km dolg in nekaj km širok koralno-stromatoporidni greben. Debel je do 500 metrov (Turnšek, 1966, Sl. 16. Shematski profil jurskih plasti na Trnovskem gozdu (orehek & ogorelec, 1979) Fig. 16. Schematic columnar section of Jurassic beds on Trnovski gozd (Orehek & Ogorelec, 1979) femiUSë .»¿t: : M ê • Uh-r«■ •» ft local lagoon«] RAR ASTROMATO -PORID ZONE ACTINOSTROMARIID ZONE REEF-SLOPE OPEN SEA „ îtr&â ■ ¿i ÏÛIS -—-- biological characteristics (fossil association) Hydrozoa.- Actlnostromariicea Ftarastromaroporicca *öof 5PEOP5 25 11 sion rt1. Cladocoropsis Chaetetida Anthozoa. Stvlinina, massive ramose s 11 5 cl t --— — -.— Favilna, massive 10 o —.----—--------— . — — ~ ----——— — _____ Airphiastraeina Funqiina 6 29 — — --— — —--- CrinQidea (fragments) 6 Echinidea [spines) — — — — Brachiopoda Nerinea, Dtceras T -—--- — — Foraminifera Algae Cephalopoda, Tmtinnlna — —--------■ ---------— — — --- Sl. 17. Shematski presek malmskega bariernega grebenskega kompleksa v Sloveniji s facialno conacijo in favnisticnimi združbami (Turnšek et al., 1981) Fig. 17. Schematic cross section of the Malmian barrier-reef complex in Slovenia showing its facies zonation and faunal associations (Turnšek et al., 1981) so ugotovljene troholine (Trocholina alpina in T. elongata), Protopeneroplis striata, Pfenderina salernitana, Kurnubia palestinensis, K. jurassica in Nautiloculina oolithica (Šribar, Lj. - analize za OGK). Nekatere plasti kažejo znake litoralne sedimentacije. Na Trnovskem gozdu je del karbonatnega kompleksa popolnoma dolomitiziran. Slovenski bazen Jurske plasti v pelagičnem razvoju so razvite na širšem prostoru Tolmina in Bovca, v predgorju Julijskih Alp in v zahodnem delu Južnih Karavank, v manjšem obsegu pa tudi v vzhodnem delu Posavskih gub. Liasne plasti, ki dosežejo debelino do 300 metrov, so zastopane s ploščastim mikritnim apnencem z gomolji roženca, med katerim so tudi tanke plasti glinastega laporovca. Med fosili sta prisotni foraminiferi Ophthalmidium leischneri in Involutina liassica ter radiolariji in spongije. Ob robovih bazena so se odlagali debelejši paketi apnenčevih breč, ki so splazele po pregibu z roba šelfa (Rožic, 2006, 2008; Rožic & Popit, 2006; Buser & Ogorelec, 2008). Med kosi breče so pomešani tudi ooidi. Breča in plasti drobnejših kalkarenitov pogosto kažejo postopno zrnavost in laminacijo. Na Begunjščici so ploščasti apnenci z roženci impregnirani z manganovimi oksidi in vsebujejo številne amonite. Doggerske in spodnjemalmske plasti se težko določijo s fosili, debele pa so le nekaj deset metrov. Zastopane so z glinastimi skrilavci, radiolariti in s plastmi mikritnega in biomikritnega apnenca z roženci (Buser, 1979b; Ogorelec & Dozet, 1997). Med fosili se pojavljajo foraminifera Globigerina helvetojurassica in radiolariji (Goričan, 1997). Zgornji malm - tithonij je v do 50 metrov debeli skladovnici zastopan z belim in svetlosivim gostim mikritnim apnencem tipa »biancone«, ki vsebuje gomolje in pole roženca. V apnencu so pogoste kalpionele in radiolariji. Enak apnenec se je odlagal zvezno še v spodnji kredi, berriasiju in spodnjem valanginiju, tako da doseže celoten paket kalpionelidnih apnencev do 250 metrov (Cousin, 1981; Buser, 1986, 1987; Jurkovšek, 1987; Jurkovšek et al., 1990). Julijska karbonatna plošča Spodnjejurske plasti so razvite v plitvomor-skem faciesu odprtega šelfa. V njih se menjavajo biosparitni, oolitni in mikritni apnenci, mestoma pa so prisotne tudi stromatolitne in loferitne plasti. Na kontaktu z zgornjetriasnimi karbonati so ponekod emerzijske breče in neptunski dajki, oboji zapolnjeni z rdečkastim glinastim vezivom (Babic, 1980/81; Jurkovšek et al., 1990; Črne et al., 2007). V zgornjem liasu je bila Julijska karbonatna plošča razkosana na več blokov, ki so bili različno poglobljeni. Na njih se je pričela pelagična sedi-mentacija ter kondenzacija sedimentov (Buser, 1986a; Jurkovšek et al., 1990; Šmuc, 2005). Na Mangartu, Rombonu, v Trenti ter v Dolini Triglavskih jezer izdanjajo rdečkasti biomikritni apnenci tipa »ammonitico rosso«, ki vsebujejo železove in manganove gomolje (Jurkovšek et al., 1990; Šmuc, 2005; ogorelec et al., 2006). Opisani apnenci kažejo zelo podoben mikrofacies, kot je poznan s klasične lokalnosti gomoljastih globlje-morskih apnencev v Severnih Alpah (npr. Adnet pri Salzburgu - Böhm et al., 1999). Nad manganskim horizontom leži še do nekaj deset metrov rdečega in rjavkastega mikritnega apnenca z radiolariji in gomolji roženca dog-gerske in malmske starosti, nato pa berriasijski apnenec z gomolji roženca tipa »biancone«. Sl. 18. Globljemorski razvoj zgornjetriasnega Baškega dolomita in jurskih plasti na Kobli (Buser & Ogorelec, 2008) Fig. 18. Deeper-marine development of Upper Triassic Bača dolomite and Jurassic beds on Mt. Kobla, Julian Alps (Buser & Ogorelec, 2008) Vzhodne Alpe V Severnih Karavankah so spodnjejurske plasti v okolici Uršlje gore razvite kot rdečkasti ploščasti in gomoljasti rdečkasti apnenci z lečami roženca, ki so se odlagale v globljem morju (Ramovš & Rebek, 1970; Mioc & Sribar, 1975). KREDA Čeprav je bila kredna perioda v mezozojskem obdobju najdaljša, saj je trajala kar 80 milijonov let, je na slovenskem prostoru razvita dokaj monotono, na Dinarski plošči kot debela skladovnica apnencev in dolomitov, v Slovenskem bazenu, ki Biomikritni apnenec z lupinami moluskov in radiolarijev. Pe-lagicni facies. Dogger. Dolina Triglavskih jezer. Merilo 1 mm Biomicritic limestone with mollusc shells and radiolarians. Pelagic facies. Dogger. Triglav lakes valley. Scale 1 mm Manganski gomolji v jurskem apnencu. Dogger. Grapa Slat-nek pri Bovcu Manganese nodules in Jurassic limestone. Dogger. Slatnek gorge near Bovec je v tem času segal tudi na prostor Julijske karbonatne plošče, pa kot flišne plasti z vmesnimi paketi globljemorskih apnencev. Debelina krednih plasti na Dinarski plošči doseže do 2000 metrov, v bazenu pa do 800 metrov (Buser, 1989; Plenicar, 1979, 2009). Koncem krede je prišlo na južnem Primorskem in v Istri do dolgotrajnejše okopnit-ve. V istem obdobju je Dinarska karbonatna plošča razpadla na več manjših enot z vmesnimi flišnimi bazeni, ki so se že od zgornje krede pa vse do konca paleogena postopno selili od severa oziroma Bovškega proti jugu v osrednjo Istro (Buser, 1986b). Shematski prikaz razvoja krednih plasti je prikazan na slikah 2 in 3, posebej pa na sliki 14. Dinarska karbonatna plošča Spodnjekredne plasti so v plitvomorskem razvoju najbolj razširjene na Dolenjskem, Notranjskem, Hrušici in na zahodnem delu Trnovskega gozda. Razvite so dokaj monotono in kažejo značilnosti sedimentacije na zaprtem šelfu z lagunami in občasnimi medplimskimi pogoji. Glede na mikrofacies prevladujejo med apnenci tipi z mi- kritno osnovo (mudstone do packstone) ter s fosili, ki so značilni za bolj mirno okolje - foraminifere, ostrakodi, alge in moluski. Litološko je prehod zgornjejurskih plasti v berriasijske postopen. Apnenec je po strukturi biopelmikriten, večkrat z izsušitvenimi porami in z laminacijo, mestoma rahlo laporast in zaradi sledov organske primesi ponavadi temnejše sive barve. Nekatere apnenčeve plasti je zajela tudi zgodnja ali/in poznodiagenetska dolomitizacija. Slednja se kaže v dolomitnih romboedrih, pogosto s conarno zgradbo ter z manjšimi lečami zrnatega dolomita. Sribarjeva (1979b) je celotno spodnjekredno zaporedje na Logaški planoti razdelila na osnovi mikrofosilne združbe v pet cenocon, enaka razdelitev pa je veljala tudi za prostor Trnovskega gozda (Koch, 1988; Koch et al., 1989) in za Kočevsko (Dozet, 1990c; Dozet & Sribar, 1991): Za berriasijske in valanginijske plasti sta značilna in najbolj pomembna mikrokopro-lit Favreina salevensis in alga Salpingoporella annulata. Favreine so mestoma tako številne, da so kamnotvorne. Med foraminiferami se pojavlja vrsta Pseudocyclammina lituus. V vrhnjem delu valanginijskih in v hauterivijskih plasteh so prisotne alga Clypeina solkani, foraminiferi Pseudo-textulariella salevensis in Orbitolinopsis capuen-sis, v večjem številu pa so prisotni še ostrakodi in drobni moluski. Tudi v tem obdobju so poleg biomikritnih apnencev prisotni mikrofacialni tipi s pogostimi izsušitvenimi porami, ki kažejo na podobne paleogeografske razmere kot v valangi-niju - zaprt šelf z lagunami in medplimskimi ravnicami (Orehek & Ogorelec, 1979, 1981; Sribar, 1979b; Dozet & Sribar, 1991). Barremijski apnenec je zastopan z daziklada-cejskimi algami vrste Salpingoporella muehlber-geri, aptijski pa z vrsto Salpingoporella dinarica, ki je v nekaterih plasteh na prehodu v albij izredno številna. V aptiju vrsto S. dinarica spremljajo še foraminifera Palorbitolina lenticularis, miliolide ter številni primerki mikroorganizma problematičnega izvora Bacinella irregularis, za katerega se domneva, da pripada cianobakterij-skim tvorbam (Flügel, 2004). V tem obdobju je Rudistni apnenec. Štanjel na Krasu Limestone with rudist bivalves. Štanjel na Krasu Biomikritni apnenec z algo Salpingoporella dinarica. Facies plitvega zaprtega šelfa. Aptij-albij. Nanos. Merilo 1 mm Biomicritic limestone with Salpingoporella dinarica algae. Shallow restricted shelf facies. Aptian-Albian. Nanos. Scale 1 mm prišlo na Dinarski karbonatni plošči zaradi intenzivne tektonike do njene diferenciacije in do spremembe paleookolja. To je privedlo do bolj pestrega faciesa in več razlik v debelini posameznih cenocon znotraj posamezne serije (Koch et al., 1989). Lokalno je prišlo tudi do kratkotrajnih okopnitev posameznih delov plošče. Na Krasu je taka okopnitev nakazana z emerzijsko brečo na meji med Brsko in Povirsko formacijo (sl. 19) oziroma na meji med aptijem in albijem (Jurkovšek et al., 1996; Jurkovšek, 2008, 2010; Koch & Ogorelec, 1987). Apnenec od valanginijske pa vse do albijske starosti je pogosto dolomitiziran, delno ali v popolnosti; dolomitizacija ima poznodiage-netski značaj. V vrhnji del spodnjekrednih plasti, ki je^ albij-ske starosti, Šribarjeva (1979b ter Dozet & Sribar, 1991) prišteva apnenčeve in dolomitne plasti z orbitolinami (Orbitolina ex gr. texana) ter foraminiferami (»Valdanchella« dercourti). Dokaj pogoste v tej cenoconi so tudi miliolide, med molu-ski pa rekvienije. Višji energijski indeks znotraj spodnjekred-nega zaporedja nakazujejo redke plasti z ooidi in psevdooidi. Oboji so bili v mirnejše okolje z mikritnim karbonatnim blatom naplavljeni in pomešani s peleti in drobnimi fosili. Lokalno so obstajali tudi manjši grebeni in biostrome koral, hidrozojev in alg. Iz berriasija in valanginija je znan tak koralni greben pri Zavrhu na Banjški planoti (Turnšek & Buser, 1974), iz časa aptija in albija pa so opisani koralni grebeni iz Kanalskega vrha in okolice na Banjški planoti (Turnšek & Buser, 1974; Grotsch, 1991; Grotsch et al., 1994) in s Kočevske gore (Turnšek et al., 1992). V apti-ju je bil na Sabotinu manjši algni greben, zgrajen v večjem delu iz vrste Lithocodium aggregatum (syn. Bacinella irregularis) (Koch et al., 2002). Znotraj hauterivijskega zaporedja se na zahodnem delu Trnovskega gozda in na Sabotinu pojavlja 15 do 40 metrov debel paket črnega bio-mikritnega in biopelmikritnega ploščastega bitu-minoznega apnenca z gomolji roženca (»Trnovski ploščasti apnenec«, Plenicar & Buser, 1967), ki Sl. 19. Litostratigrafski stolpec krednih in paleogenskih plasti severnega dela Tržaško-komenske planote (Jurkovšek, 2010) Fig. 19. Lithostratigraphic column of Cretaceous and Paleogene beds of the northern part of Trieste-Komen plateau (Jurkovšek, 2010) vsebuje do 1,1 % Corg. Analize več vzorcev kažejo, da ta apnenec lahko uvrščamo med potencialne matične kamnine za nastanek ogljikovodikov z nizko sposobnostjo njihovega generiranja (Ogo-relec et al., 1996a). Zgornjekredne plasti so se odlagale na bolj odprtem in plitvem šelfu z višjim energijskim indeksom. Značilne zanje so svetla barva apnencev, debele plasti in bogata rudistna favna (Plenicar, 2005; Plenicar & Jurkovsek, 1996, 1998). Zastopani so sicer vsi tipi apnencev, vendar pa sta tipa packstone in grainstone najbolj pogosta. V večjem obsegu zgornjekredne plasti izdanjajo na Tržaško-komenski planoti in na Nanosu, v manjšem obsegu pa tudi na Javornikih, Dolenjskem in Kočevskem. Zaradi velikih debelin posameznih plasti, zanimivega izgleda in dobrih tehniških lastnosti kamna, so le-te zanimive kot arhitektonski kamen, ki ga predvsem na Krasu lomijo v številnih kamnolomih. Dolomitnih plasti je precej manj kot v spodnjekrednem zaporedju. Kljub enoličnemu litološkemu razvoju je možno natančno razčleniti zgornjekredne plasti na osnovi fosilov, predvsem rudistov in foraminifer, (Šribar & Plenicar, 1990; Plenicar, 1960, 1979, 2005, 2009; Jež, 2011). Taka razdelitev je za prostor jugozahodne Slovenije prikazana na sl.19. Za srednji in zgornji cenomanij je med foraminife-rami značilna Broeckina (Pastrikella) balcanica, za zgornji turonij neskeletna alga Aeolisaccus ko-tori, za obdobje coniacija in spodnjega santoni-ja foraminifera Pseudocyclammina sphaeroidea za zgornji santonij in campanij Keramospherina tergestina, za maastrichtij pa Orbitoides media Rudistni rožasti apnenec (»fiorito«) (foto: B. Jurkovsek) Rudist ornamental limestone (»fiorito«) (pphoto: B. Jurkovsek) in Rhapydionina liburnica (Šribar & Plenicar, 1990). Na območju Tržaško-komenske planote so izdvojene formacije: Povirska formacija ceno-manijske starosti, Sežanska formacija zgornje-turonijske, coniacijske in santonijske starosti ter Lipiska formacija santonijske in campanijske starosti (Jurkovsek et al., 1996; Jurkovsek, 2008, 2010; Jurkovsek & Kolar-Jurkovsek, 2007). Znotraj Repenske formacije, ki obsega spodnji tu- Litologijo Lithology Cenocona - Assemblage zone Makrofavna - Macroiauna Starost - Age VIII, Cenocona - L Assemblage zone Assem. z. —Gansserina Rhapydionina liburnica^^^ gansseri Gyropleura sp. 1 Bournonia s p. ^^ Zgornji maastrichtij Upper Maastrichtian ' i '1 1 p1 VII. Cenocona - Assemblage zone Orbitoides media Hippurites (Vacc.) braclensis Joufia reticulata Spodnji do srednji maastrichtij Lower-Middle Maastrichtian :sr : , i ; H ] : VI. Cenocona - Assemblage zone Keramosphaerina tergestina H. (Orbignya) nabresinensis H. (Vacc.) salopeki Katzeria hercegovinaensis Zgornji santonij-campanij Upper Santon i an-Companion V. Cenocona - Assemblage zone Pseudocyclammrna sphaeroidea Idatina antiqua Radiohtes praegalloprovincialis Hippurites (Vacc.) oornuvaccinum Con iacij-spod nji son t on ij Coniaeian-Lower Sontonian IV. Cenocona - Assemblage zone Aeolisaccus kotori bledeella xignaaa M. acuticostata Rhynchonella contorta Zgornji turonij Upper Turonian /? i ' i lighter carbon isotope with respect to the Upper Permian ones (Dolenec T. et al., 1995, 1999a, b, c, 2004). Just below the P/T boundary in places a thinner bed of oolitic limestone appears (Dolenec, M. & ügorelec, 2001; Dolenec M., 2004) that can be compared with the Tesero horizon in the Alps (Asseretü et al., 1972). Paleontologically the P/T boundary in Slovenia was proved lately on basis of the conodont zonation (Kolar-Jurkovšek & Jurkovšek, 2007; Kolar-Jurkovšek et al., 2011) and foraminifers (Nestell et al., 2011). Just above the Permian/Triassic (P/T) boundary the characteristic small foraminifer Earlandia occurs. Among the diagenetic processes affecting the Upper Permian carbonate rocks, dolomitization has by far the larges extent, and to a lesser extent silificication and dedolomitization are present also. As a result of dedolomitization in beds with evaporitic minerals epsomite precipitated, which can be observed in the Idrija mercury mine. The major part of dolomite is of early diage-netic origin, and it formed according to the eva-poritic model of dolomitization (Shinn & Ginsburg, 1964). Aridic climate in Upper Permian is indicated next to gypsum and anhydrite also by isotopic analyses of 518O (Polšak & Pezdic, 1978; Dolenec et al., 1981; ügorelec et al., 1999b) and Na+ contents that are high for carbonates (ügorelec & Rothe, 1979). Owing to specific sedimentary conditions and climate, the time of Upper Permian was favorable for formation of stratiform lead and zinc deposits. Such deposits are abundant in the eastern Sava folds, namely in the upper part of the Upper Permian sequence (Puharje near Šoštanj, Iskra, 1969) and at the boundary between the Upper Permian and Lower Triassic (Mokronog, Bohor, Ledina near Sevnica, Drovenik et al., 1980). The Upper Permian beds in Slovenia have in general the same or very similar microfacies as the limestones and dolomites of same age in neighbouring areas, e.g. in the Carnic Alps (Buggisch, 1974; Buggisch et al., 1976; Holser & Schön- LAUB, 1991; Magaritz & Holser, 1991; NoÉ, 1987), Dolomites (Bosellini & Hardie, 1973), on Mt. Velebit (Kochansky-Devidé, 1979; Sremac, 1991, 2005) and in Hungary (Haas, 2001; Haas et al., 2004, 2006). TRIASSIC Triassic rocks are in Slovenia the most abundant of all, covering almost a quarter of its territory, and their total thickness attains up to 3800 meters (Buser, 1979), with carbonate rocks decidedly predominating over clastic and pyro-clastic rock types (Fig. 2). They are distinguished by an extraordinary diversity of lithologies with characteristics of Alpine development within the Tethys which is similar or identical to that known in the Northern Alps). In Lower Triassic the carbonate sedimentation on shallow shelf was accompanied by supply of terrigenous, largely fine-grained terrestrial material, while in Lower Anisian the carbonates completely prevail. End of Anisian (Buser, 1989), in the Idrija area already in Middle Anisian (Car, 1985, 2010), the Slovenian platform started to differentiate as a result of intense tectonics, into the Dinaic carbonate platform in the south, the Julian carbonate platform in the south, and the intermediate Slovenian basin (Fig. 6). The latter persisted in the central Slovenian region all to the middle of Jurassic period when it extended also to the Julian carbonate platform territory, while toward the Dinaric carbonate platform it existed till the end of Cretaceous. More detailed descriptions of paleogeographic development inTriassic on the integral Slovenian territory, of paleotectonics and biostratigraphic subdivisions are found above all in the works by Buser, 1979, 1980b, 1988, 1996; Dozet & Buser, 2009; Premru, 1980, 1982, 2005; Buser et al., 2007, 2008, and Placer, 2009. A recent example of how this paleogeograp-hic region in Slovenia might look like in Triassic time is given by the Bahamas archipelago (Fig. 7) where the unique very shallow carbonate plain is split by the up to 900 meters deep trench, the Tongue of the Ocean. By the dimension of several hundred kilometers' this trench is comparable with the size of the ancient Slovenian basin. In Fig. 8 a schematic presentation of lithologic development of the Triassic rocks in Slovenia is given with selected stratigraphic columns. LOWER TRIASSIC (Induan and Olenekian) Thickness of the Lower Triassic sequence is highly variable. It varies between 40 and 500 meters, while it attains up to 600 meters in the Southern Karavanke Mts. (Buser, 1980a). In the entire Slovenian region south of the Periadriatic lineament the beds appear in a rather uniform development. In the lower part of sequence which is up to 250 meters thick clastic and carbonate beds alternate with oolitic layers that are especially distinctive in the field. Dolomites and limestones have a sandy appearance owing to admixture of terrigenous quartz and mica. The non-carbonate component locally attains as much as 50 %. Clas-tites are represented by reddish claystones, marlstones and siltstones. As to texture, the limestone is mostly biomicrite or pelmicrite. It was deposited in a very shallow restricted part of shelf that possessed at times characteristics of lagoons and littoral. It is often entirely or partly dolomitized, and bioturbation structural features are also typical. Thinner lenses and nests of gypsum and anhydrite indicate local and periodic evaporitic conditions of sedimentation. Oolites formed in intertidal channels and deltas with higher energy index. Characteristic is their reddish color resulting from hematitic pigment. Nuclei of ooids were often subjected to late diagenetic dolomitization manifested by up to 300 pm large dolomitic rhombohedrons. Between ooids occur often plates of echinoderms and tiny gastropod shells of Natica gregaria and Holopella gracilior species, and also fine terrigenous grains of quartz and mica. In the upper part of the Lower Triassic succession terrigenous content decreases. A darker biomicritic or pelmicritic marly limestone (mud-stone to packstone) prevails over the lighter colored dolomite. Among fossils foraminifers, and in certain beds also abundant ostracods, echino-derm plates and thin valves of species Claraia clarai are represented. Some conodonts are present too (Kolar-Jurkovšek & Jurkovšek, 1995, 1996, 2007). The most important for stratigraphy is foraminifer Meandrospira pusilla. North of the Periadriatic lineament, especially in surroundings of Črna na Koroškem, the Lower Triassic beds appear in an clastic development, in respect that the region of the Northern Karavanke Mts. is a part of the Eastern Alpine geo-tectonic unit. They are developed as sandstones, shaly siltstones and conglomerates of the Buntsandstein type (Mioc, 1983), and they contain no fossil remains (Štrucl, 1971). Lower Triassic beds on the Slovenian territory generally display the same, or a very similar microfacies to beds of same age in neighbouring areas, e.g. the Werfen beds in Northern Alps (Mostler & Rossner, 1984), in Carnic Alps (Holser & Schonlaub, 1991), Dolomites (Assereto et al., 1972), Hungary (Nagy, 1968; Haas, 2001), in Austrian part of Southern Karavanke Mts. (An-derle, 1970), at Mt. Svilaja in Dalmatian Zagora (Ščavničar et al., 1983, Jelaska et al., 2003) and elsewhere, which indicates a vast and uniform sedimentary environment in the Lower Triassic. MIDDLE TRIASSIC Development of Anisian beds in Slovenia is rather uniform, mostly as bedded dolomite that exhibits frequent indications of intertidal sedimentation with stromatolites and shrinkage pores (Grad & Ogorelec, 1980; Dolenec et al., 1981). Limestone is less common than dolomite. Among fossils foraminifers (Meandrospira dinarica, Pilammina densa, Glomospirella irregularis, G. grandis, G. semiplana, Trochammina sp.) prevail, locally also algae (Physoporella pauciforata) occur. In northern part of Julian Alps between Mojstrana and Kranjska Gora massive reef limestone is preserved, consisting primarily of algae and thrombolitic structures (Ramovš, 1987). The same development is present also in the castle rock wall above the Bled lake (Flügel et al., 1993). Thickness of Anisian beds attains up to 600 meters. North of the Periadriatic lineament, at Topla below Mt. Peca bedded dolomite is exposed which is mineralized with lead and zinc ores (Štrucl, 1974). It is overlain by dark micritic limestone with chert nodules. In the middle of Anisian the Slovenian platform begun to disintegrate. As a result the sedimentation from Middle Triassic on took place on separate geotectonic units in different environments. For the deeper marine development of Anisian as known in Karavanke Mts. near Tržič, in Idrija area and in eastern Sava folds ammonites (Balatonites balatonicus, Buser, 1979a) and conodonts (Kolar-Jurkovšek, 1983, 1991) are characteristic. Ladinian beds are distinguished by a highly diverse lithology of various rapidly alternating lithologic types. They are exposed in a number of localities in central Slovenia, in broader Idrija and Cerkno areas, in foothills of Julian Alps and Karavanke Mts., and in a larger extent north of the Periadriatic lineament in the Peca mountains. As a result of intense tectonics during the Idrija tectonic phase (Buser, 1980b) the territory of central Slovenia became drastically dismembered. In deeper trenches volcanic effusions of spilitic-keratophyric association (basalts, quartz keratophyres, porphyries ...) occurred, accompanied by deposition of their tuffs and tuffites (Buser, 1979; Dozet & Buser, 2009). Some blocks became subaerially exposed as indicated by thick beds of slope breccias and conglomerates. In Southern Karavanke Mts. and part of Julian Alps they appear as the Ukve (Ugovizza) breccia (Buser, 1986b; Jurkovšek, 1987), and in surroundings of Idrija as the Stopnik conglomerate (Mlakar, 1969; Car & Čadež, 1977; Čar & skaberne, 2003; Čar, 2010). On Dinaric and Julian platforms in some places dark limestones with chert and in-terbedded tuff layers deposited, and in the central part of Slovenian basin the Psevdozilja beds that are characterized by an alternation of dark shaly claystones, sandstones and tuffs with subordinate limestones. Texture of limestone is generally biomicritic mudstone or wackestone, and among fossils in addition to thin mollusc shells especially the conodonts (Kolar-Jurkovšek, 1983, 1991; Kolar-Jurkovšek & Placer, 1987; Placer & Kolar-Jurkovšek, 1990; Kolar-Jurkovšek & Rižnar, 2006) and radiolarians occur (Gorican, 1997; Gorican & Buser, 1990; Skaberne et al., 2003). Important macrofossils are ammonites and bivalves (Jurkovšek, 1983, 1984; Ramovš & Jurkovšek, 1983; Ramovš, 1989). Interesting in the Upper Ladinian of Kam-nik-Savinja Alps is the Koro{ica Formation that overlies granular dolomite and green tuff. The limestone is a slightly bituminous black biomi-crite containing chert nodules. Among fossils bivalves (Jurkovšek, 1984), ammonites and fish as well as reptile skeletons occur (Celarc, 2004a; celarc & Žalohar, 2010). In the Northern Karavanke Mts., in Mežica area an over 1000 meters thick complex of massive, in part bedded limestone and dolomite occur in Ladinian and Cordevolian, known as the Wetterstein limestone (Štrucl, 1970, 1971). The most characteristic such massif is the Mt. Peca group. The limestone is mineralized with zinc and lead ores (Štrucl, 1971, 1984; Brigo et al., 1977; Drovenik et al., 1980). The lower part of Wetterstein Formation is more massive, and includes reef limestones with corals and chaetetides (Turnšek, 1997; Bole, 2002), whereas its upper part, already of Cordevolian age, was deposited largely in intratidal zone of an open shelf. The rocks contain frequent stromatolitic and loferi-tic beds. Southwards the Wetterstein limestone passes into dark mudstones and marlstones with rare limestone interbeds. These beds, known as the Partnach Formation, were sedimented in a restricted, somewhat deeper part of shelf. In this packet locally also lenses and nodules of evapori-tic minerals, mostly gypsum occur (Štrucl, 1971; Mioc, 1973). UPPER TRIASSIC carnian beds are the most abundant in western Slovenia. Within them stratigraphically the Cordevolian, Julian and Tuvalian rocks can be distinguished. They occur in the shallow marine and in deeper marine development. The entire Carnian time lasted 14 million years. Lately, the term Cordevolian substage is beeing abandoned (Celarc, 2004b; Lucas et al., 2010) because the fossil assemblage of these beds belongs already to the lower part of the Julian substage. However, considering the distinctive, more reefal facies of massive limestone and dolomite known from lowermost Carnian in Slovenia, as well as the traditional subdivision in the Basic Geologic Map, Cordevolian substage is kept as a separate stratigraphic unit in this monograph. Rocks of cordevolian age occur only in carbonate development, mostly as light, massive saccharoidal dolomite with primary texture of rock only exceptionally preserved. The fossils, predominantly dasycladacean algae and corals, allow the supposition that the Cordevolian dolomite represents ancient reefs that were later subjected to intense dolomitization. Limestones of this age compose the larger part of Mts. Mežakla and Pokljuka in the Julian Alps (Ramovš, 1988; Ramovš & Turnšek, 1984; Turnšek & Buser, 1989) and extensive areas in Kamnik-S a vin j a Alps (Krvavec, Velika planina, Menina - Premru, 1974, 2005; Ramovš & Šribar, 1993; Celarc 2004a; Žalohar & Celarc, 2010), whereas in smaller outcrops they appear also in the region between Cerkno and Ljubljana and in eastern Sava folds. As a result of paleokarstification (Buser, 1980b) the limestone is often reddish colored, and it contains pockets of red clay and bauxite. Such limestone has been appreciated as ornamental stone. It is being extracted in quarries at Hotavlje and Lesno Brdo near Vrhnika (Ramovš, 1995). In dolomite and limestone of the mentioned areas, the most frequent fossils are skeletal algae (Diplopora annulata, Diplopora annulatissima, Gyroporella ladinica), that are locally rock-forming (Ramovš, 1988, 1992; Dozet, 1979; 2004; Čar, 2010). A special bedded development of dolomite is known on the Vojsko plateau at Gačnek, where in a 40 meters thick succession structures typical for littoral intertidal environment can be found (Mlakar, 1969; Čar, 2010). In the region of Northern Karavanke Mts. the sedimentation of bedded limestone and dolomite as the top part of the Wetterstein Formation continued in Cordevolian. Thicknesses of Cordevolian dolomite and limestone may be very variable, from several tens meters up to 600 meters in different geotectonic units of Slovenia. Rocks of Julian and Tuvalian substages are variable, mainly carbonatically developed. Within limestones and dolomites also layers of marlstones and packages of clastites and tuffs occur. Their thickness varies between 100 and 400 meters. In the southwards direction on the Dinaric carbonate platform clastites and tuffs become more and more abundand, so that in the Idrija and Kočevje areas they already prevail above the carbonates (Cigale, 1978; Dozet, 1990a). In contrast to Cordevolian dolomite, the Julian and Tuvalian beds were deposited on restricted shallow shelf, often in lagoons. Dark color of limestone and pyritic pigment indicate ano-xic conditions in the sedimentary environment. Limestone is often marly and locally with boudi-nage structural features. Organic matter content varies around an average of 1 %, at most to 4 %, and its origin is largely terrestrial (Ogorelec et al., 1996a). According to texture the limestone is micritic and biopelmicritic mudstone to packstone. Predominant fossils are thin-valved bivalves (Jelen, 1990; Jurkovšek, 1994), skeletal and nonskeletal algae (Poikiloporella duplicata, Cly-peina besici), ostracods and smaller foraminifers (Nodosaria ordinata, Glomospira sp., Diplotremi-na astrofimbriata, Lamelliconus multispirus, Am-modiscus parapriscus, Frondicularia pupiformis) (Oblak, 2001) and bivalves of Triadomegalodon idrianus species (Čar 2010). A somewhat more agitated environment is indicated by individual ooids and oncoids. Limestone was often affected by early- as well as late-diagenetic dolomitiza-tion and karstification with pockets and layers of bauxites (Dozet, 1979, 2004; Buser, 1980b). The upper parts of Julian and Tuvalian sequence are often represented by grey dolomite with rare marlstone intercalations, and locally also with several meters thick layers of tuffaceous claystone. This dolomitic packet gradually passes to lighter-colored bedded dolomite without intercalated marly sheets, the Main dolomite. Age of this dolomite is determined by up to several cm large megalodontid bivalves, foraminifers, algae (Poikiloporella duplicata) and conodonts (Kolar-Jurkovšek, 1991). A distinct development of Julian-Tuvalian sequence are the Amphiclina beds, which in Cerkno area and in Baška grapa attain thicknesses of up to 250 meters (Buser, 1986b). Characteristic for them is interbedding of dark grey to black marly biomicritic limestone, shaly marlstone, quartz sandstone and conglomerate, tuffs and tuffites. In this complex several up to 40 meters thick reefs occur in the wider Cerkno area (Senowbari-Dar-yan & Schafer, 1979; Čar et al., 1981; Turnšek et al., 1984). They are mainly built of sponges and to a lesser degree of corals (Turnšek, 1997). Structural characteristics of limestones and graded bedding in beds allow to interpret the sedimentation of Amphiclina beds as taken place in the transitional zone of carbonate shelf toward the Slovenian basin (Turnšek et al., 1984). In Julian Alps the shallow- as well as the deeper-marine development of Julian and Tuva-lian beds can be observed. The shallow marine development crops out e.g. at Tamar and Log pod Mangartom (Ogorelec et al, 1984; Jurkovšek, 1987). The biomicritic limestone (wackestone to packstone) contains numerous foraminiferal tests, small megalodontids and other bivalves, echinoderm plates. It is often dolomitized, largely marly, containing up to 15 % noncarbonate admixture, mostly clay and organic matter. For the deeper sea development dense biomicritic limestone with chert nodules is characteristic. Among fauna thin-valved bivalves, calcitized ra-diolarians and washed-in plates of echinoderms prevail (Ogorelec et al., 1984; Jurkovšek, 1987). In these beds on Kozja dnina below Mt. Triglav the fossil fish Birgeria sp. was found (Jurkovšek & Kolar-Jurkovšek, 1986), a worm Valvasoria car-niolica (Kolar-Jurkovšek & Jurkovšek, 1997) and other fossils were found (Dobruskina et al., 2001; Bitner et al., 2010), while in the western part of Southern Karavanke Mts. algae Clypeina besici (Kolar-Jurkovšek & Jurkovšek, 2003) and radio-larians (Kolar-Jurkovšek et al., 2005). Julian and Tuvalian beds in Northern Karavanke Mts. are represented at Mežica with an up to 350 meters thick succession of limestone and dolomite developed in 20 cyclothems of lofer type, for which three clastic horizons of shale, siltstone and marlstone are characteristic (Štrucl, 1970, 1971; Pungartnik et al., 1982). Certain beds are extremely rich with fossils, especially crinoids (Jurkovšek, 1978; Jurkovšek & Kolar-Jurkovšek, 1997; Kaim et al., 2006; Kolar-Jurkovšek & Jurkovšek, 2009, 2010; Jurkovšek et al., 2002). A rather agitated environment within the shallow shelf is indicated by individual oolitic layers and oncoids. Rocks of Norian and Rhaetian ages are represented in Slovenia by three developments. In both Julian and Dinaric carbonate platform the Main dolomite and its lateral variety, the Dachstein limestone occur, and in Slovenian basin the Baca dolomite and Železniki limestone (Fig.13). Main dolomite and Dachstein limestone cover large areals, and are the most widespread rock formations in Slovenia. They build most of the Julian Alps, a large part of Notranjska, northern part of Trnovski gozd and part of Dolenjska. The thickness of Main dolomite is between 800 and 1300 meters, the same as also of the Dachstein limestone. Limestone predominates on the Julian carbonate platform, whereas on the Dinaric platform dolomite prevails. Thickness of the Baca dolomite is 3 to 4 times smaller, and is estimated to at most 400 meters (Buser, 1986b). Dachstein limestone is thickly bedded, and it occurs in the typical lofer develoment as known in the Northern Alps (Fischer, 1964; Zankl, 1971; Piller & Lobitzer, 1979; Piller, 1981), Dolomites (Bosellini, 1967; Bosellini & Rossi, 1974) or in Hungary (Haas, 1994). Individual cyclothems (Fig. 12) consist of up to 2 meters thick beds of biomicritic and biosparitic limestone which are interrupted by thin stromatolitic and loferitic layers, and locally also interbedded by breccias with clayey matrix. Among fossils the most abundant are foramini-fers (Triasina hantkeni, Aulotortus gr. sinuosus, A. permodiscoides, A. friedly, Miliolipora cuvil-lieri, Galeanella sp.), algae (Macroporella retica) and echinoderms. In certain beds large mega-lodontid bivalves are even rock-forming. The Dachstein limestone was deposited on a shallow open and near-shore shelf with periodic intertidal and supratidal conditions (ügorelec, 1988; Dozet & ügorelec, 1990; ügorelec & Rothe, 1992). The beds deposited in littoral environment are often dolomitized. On Julian platform larger reef massifs occur within the Dachstein limestone Formation (e.g. Begunjščica, Pokljuka, Bohinj), and smaller reefs containing a rich coral fauna (Turnšek & Ramovš, 1987; Turnšek & Buser, 1991; Turnšek, 1997). On both Dinaric and Julian carbonate platforms periodically short-term emersions of their individual parts occurred. In such occasions pa-leokarst developed. It is best preserved in Kanin Mts. and on Mt. Krn (Babic, 1980/81; ügorelec & Buser, 1996). Equal fauna and microfacies as found in reef limestone of Slovenian part of the Alps occur also in Norian-Rhaetian reefs in the Northern Alps (Zankl, 1971; Flügel, 1981; Piller, 1981; stantün & Flügel, 1989; Flügel & Koch, 1995; Turnšek et al., 1999). Main dolomite has a monotonous, entirely dolomitic development. Characteristic is cyclic interchanging of thicker dolosparitic and bio-micritic beds with thinner stromatolitic layers, loferites, locally also supratidal conglomerate and emersion breccias. Among fossils large mega- lodontids, foraminifers and algae are represented. Locally also beds and lenses with oncoids and vadose pisoids appear (Ogorelec, 1988; Dozet, 1991). Main dolomite deposited initially as limestone on very shallow restricted shelf with wide coastal plains, in the shallower part of shelf as Dachstein limestone. Dolomitization was early diagenetic according to the evaporative pumping model (Illing et al., 1965). Later the rock was affected also by the late diagenetic dolomitiza-tion. Dolomite also shows often indications of paleokarstification. Smaller and larger corrosion vugs are filled with zonal sparitic cement, commonly accompanied by red internal micrite. In the same time, when Dachstein limestone and Main dolomite were depositing on the platforms, the Ba~a dolomite and Železniki limestone were formed in the basin and on its margins (Buser, 1979; Ramovš, 1970; Gale, 2010). The carbonate sediment in both formations is micritic, with very rare fossils, i.e. small foraminifers (Rožic, 2005, 2006, 2008; Rožic & Kolar-Jurkovšek, 2007; Buser & Ogorelec, 2008; Rožic et al., 2009; Gale et al., 2010) and conodonts (Kolar-Jurkovšek, 1982, 1991, 2011) but characteristic for the two formations are interbeds and nodules of chert. jurassic As in the Middle and Upper Triassic the territory of Slovenia also in Jurassic belonged to three geotectonic units that at the same time represented distinct sedimentary environments. Southern Slovenia was a part of the Dinaric carbonate platform with typical shallow water sedimentation and imposing thickness of carbonate rocks which attains in Jurassic more than 1500 meters (Buser, 1989; Buser & Dozet, 2009). To the north the carbonate platform bordered on the Slovenian basin, and north of it the Julian carbonate platform still existed. The latter disintegrated in Dogger, and was replaced by the basin. Dinaric carbonate platform The transition of Upper Triassic Main dolomite and Dachstein limestone to Jurassic beds is not sharp. Only locally an up to several tens of meters thick package of intraformational breccia occur on the contact, which formed during short-term emersion phases accompanied by paleokarstification (Buser, 1979b; Ogorelec & Rothe, 1992; Jurkovšek et al., 1996). Stromatolites which are typical for Main dolomite gradually disappear, but frequent structural features of the littoral environment - shrinkage pores and desiccation cracks, supratidal conglomerate and laminites - still persist in the Lower Lias beds (Ogorelec, 1988, 2009; Orehek & Ogorelec, 1979, 1980; Dozet, 1992a, 1998). In Middle and Upper Lias as well as in Dogger various environments within the carbonate shelf can be recognized (Buser, 1979b; Ore- hek & Ogorelec, 1979, 1981; Strohmenger & Dozet, 1990, Dozet, 1992a,b). On Trnovski gozd, Hrušica, Logatec plateau and on Gorjanci Mts. sedimentation took place on the open shelf with a higher energy. Oolitic limestones prevail (Buser 1973, 1978; Strohmenger et al., 1987; Ogorelec & Dozet, 2000) which may attain a thickness of several hundred meters. Within them locally layers with large oncoids appear. Locally lithiotid bivalves are frequent, so that in places they form coquinas (Buser, 1978; Buser & Debeljak, 1996; Debeljak & Buser, 1998; Ramovš, 2000). Among important fossils that can be observed in thin-sections of Lower Jurassic - Liassic beds algae Paleodasycladus mediterraneus and Ses-trosphaera liasina, and foraminifers Orbitopsella praecursor, Involutina liassica, Agerella mar-tana, Trocholina turris, Pseudocyclammina liassica, Haurania deserta were determined (Sribar, 1979a, and data from explanatory books to Basic Geologic Map 1 : 100,000). Abundant are also stratigraphically less characteristic species of alga Thaumatoporella parvovesiculifera, echi-noderms, microgastropods, bivalves, ostracods, and locally also tiny brachiopods. In Dogger beds the foraminifer Mesoendothyra croatica and alga Selliporella donzelli were determined. On Mt. Hrušica and Trnovski gozd rare coral buildups and layers of crinoidal limestone occur. In Notranjska dark grey biomicritic and pel-micritic limestone occurs in Lower and Middle Jurassic, that indicates sedimentation in rather secluded and restricted parts of shelf with lagoons and periodic anoxic conditions (Orehek & Ogorelec, 1981). Within the limestone often lenses of sparry dolomite occur. In Kočevje area locally also thinner coal seams appear (Dozet, 1998). Thickness of Lower and Middle Lias beds varies from 200 to 400 meters, and of Upper Lias and Dogger beds up to 450 meters (Buser, 1979b). In Lower Malm a several tens kilometers long and several kilometers wide coral-stromato-poridic reef extended across the Trnovski gozd, which at that time represented the northern margin of Dinaric carbonate latform. The reef is up to 500 meters thick (Turnšek, 1966, 1969, 1972, 1997; Turnšek et al., 1981). Between the reefs that extended with interruptions to Suha Krajina and across Gorjanci to Lika in Croatia (Velic et al., 2002) sedimentation of interreef breccias and bedded limestones with hydrozoan Cladocoropsic mirabilis took place. For the Upper Malm (Kimmeridgian and Tithonian) are again characteristic oolitic and biomicritic limestones with algae Clypeina juras-sica and Salpingoporella annulata (Buser, 1979b; Orehek & Ogorelec, 1981; Strohmenger & Dozet, 1990), and with aberrant tintinnidas (Kercmar, 1961). Among foraminifers the trocholinas (Trocholina alpina in T. elongata), Protopeneroplis striata, Pfenderina salernitana, Kurnubia pa-lestinensis, K. jurassica in Nautiloculina oolithica were recognized (Sribar Lj. - Analyses for BGM). Certain beds indicate littoral sedimentation. On Mt. Trnovski gozd a part of the carbonate complex is completely dolomitized. Slovenian basin Jurassic beds in pelagic development are found in the broad region of Tolmin and Bovec, in foothills of Julian Alps and in western part of Southern Karavanke Mts., and in a reduced extent also in eastern part of Sava folds. Lias beds, attaining a thickness of up to 300 meters, are represented by platy micritic limestone with chert nodules, intercalated with thin shaly marlstone layers. Among fossils fora-minifers Ophthalmidium leischneri and Involutina liassica, radiolarians and sponges occur. Along basin margins thicker packets of calcareous breccias sedimented sliding down the shelf edge -Rožic, 2006, 2008; Rožic & Popit, 2006; Buser & Ogorelec, 2008). Between breccia fragments also ooides are found. Breccia and beds of finer cal-carenites often display graded bedding and lamination. On Mt. Begunjš~ica platy limestones with chert are impregnated with manganese oxides, and they contain numerous ammonites. Dogger and Lower Malm beds are not easily determined by fossils. Their thickness is several tens of meters only. They are represented with shales, radiolarites and beds of micritic and bio-micritic limestone with chert nodules -Buser, 1979b; Ogorelec & Dozet, 1997). Among the fossils foraminifer Globigerina helveto-jurassica and radiolarians appear -Gorican, 1997). Upper Malm - Tithonian is represented in the up to 50 meters thick succession with white and light grey micritic limestone of the biancone type containing chert nodules and sheets. In limestone calpionellas and radiolarians are frequent. The same limestone type continued to sediment also in Lower Cretaceous, in Berriasian and Lower Valanginian, so that the entire package of calpi-onellid limestones can be up to 250 meters thick -Cousin, 1981; Buser, 1986, 1987; Jurkovšek, 1987; Jurkovšek et al., 1990). Julian carbonate platform The Lower Jurassic beds are developed in a shallow water facies of the open shelf. In them biosparitic, oolitic and micritic limestones alternate, and locally also stromatolitic and loferi-tic beds are present. On the contact with Upper Triassic carbonates emersion breccias and neptunian dikes occur in places, both impregnated with reddish clayey matrix -Babic, 1980/81; Jurkovšek et al., 1990; črne et al., 2007). In Upper Lias the Julian platform became dissected into several blocks that subsided to various depths. On them pelagic sedimentation and condensation of sediments started -Buser, 1986a; Jurkovšek et al., 1990; Šmuc, 2005). On Mts. Mangart and Rombon, in Trenta valley and in the Valley of Triglav lakes reddish biomicritic limestones of the »ammonitico rosso« type outcrop that contain iron and manganese nodules -Jurkovšek et al., 1990; Šmuc, 2005; Ogorelec et al., 2006). The variegated limestones exhibit a microfacies that is very similar to the one known from the classic locality of nodular deeper water limestones in Northern Alps (e.g. at Adnet near Salzburg -Böhm et al., 1999). The manganese-bearing horizon is overlain by several meters thick reddish and brownish micri-tic limestone with radiolarians and chert nodules of Dogger and Malm age, followed by Berriasian »biancone« type limestone with chert nodules. Eastern Alps In Northern Karavanke Mts. Lower Jurassic beds occur in the area of Uršlja gora and surroundings as reddish platy and nodular reddish limestones with chert lenses, deposited in a deeper sea (Ramovš & Rebek, 1970; Mioc & Šribar, 1975). CRETACEOUS Although Cretaceous period is the longest one in Mesozoic era, lasting for whole 80 millions years, its development in Slovenian region is rather monotonous. On the Dinaric platform as a thick sequence of limestones and dolomites, and in the Slovenian basin, that at that time extended also to the region of the Julian carbonate platform, as flysch beds with intermediate packets of deeper water limestones. Thickness of Cretaceous beds on the Dinaric carbonate platform attains up to 2000 meters, and in the basin up to 800 meters (Plenicar, 1979, 2009; Buser, 1989) ; OGK Explanatory books). At the end of Cretaceous a long period of subaerial exposure started in southern Primorska and in Istria. In the same time the Dinaric carbonate platform disintegtrated to several smaller units with intermediate flysch basins that starting in the Upper Cretaceous all to the end of Paleogene gradually shifted from the north, resp. from the Bovec area southwards to central Istria (Buser, 1986b). Schematic presentation of development of Cretaceous beds is shown on figures 2 and 3, and separately on figure 14. Dinaric carbonate platform The Lower Cretaceous beds are the most extensively represented in shallow water development in Dolenjska, Notranjska, on Mt. Hrusica and on western part of Trnovski gozd. Their development is rather monotonous, having characteristics of sedimentation on restricted shelf with lagoons and periodical intertidal conditions. With respect to microfacies among limestones prevail types with micritic matrix (mudstone to packstone) and fossils typical for quieter environments - fora-minifers, ostracods, algae and molluscs. The lithologic transition of Upper Jurassic to Berriasian beds is gradual. The limestone texture is biopelmicritic, often with desiccation cracks and lamination. The rock is locally slightly marly, and owing to traces of organic matter usually of medium to darker grey color. Some limestone beds were affected by early or/and late diagenetic dolomitization. The latter is manifested by dolomite rhombohedrons, often of zonal structure, and by smaller lenses of sparry dolomite. Šribar (1979b) subdivided the entire Lower Cretaceous succession on Logatec plateau into five cenozones on the basis of microfossil assemblages. The same subdivision is valid also for the Trnovski gozd (Koch, 1988; Koch et al., 1989) and Kočevje areas (Dozet, 1990c; Dozet & Šribar, 1991). Characteristical of Berriasian and Valanginian stage and the most important are the microcopro-lite Favreina salevensis and algae Salpingoporella annulata. Favreinas are locally so numerous that they become rock-forming. Among the foramini-fers species Pseudocyclammina lituus appears. In the upper part of Valanginian and Hauteri-vian beds alga Clypeina solkani and foraminifers Pseudotextulariella salevensis and Orbitolinop-sis capuensis are present. In larger numbers occur also ostracods and tiny molluscs. In those times were present next to biomicritic limestones also microfacial types with frequent desiccation cracks that indicate paleogeographic conditions similar to those in Valanginian, i.e. restricted shelf with lagoons and intertidal plains (Orehek & Ogorelec, 1979, 1981; Šribar, 1979b; Dozet & Šribar, 1991). Barremian age of limestone is supported by dasycladacean algae Salpingoporella muehlber-geri, and the Aptian age by species Salpingopo-rella dinarica, which is extraordinarily numerous in some beds at transition to Albian. In Aptian S. dinarica is accompanied by foraminifer Pal-orbitolina lenticularis, miliolids and numerous specimens of microorganism of problematic origin Bacinella irregularis Radoičic, for which it is assumed to belong to cyanobacteria (Flügel, 2004). Due to intense tectonics thedifferentiation of Dinaric platform and changes of paleoenviron-ment occurred in this time. This resulted into a greater diversity of facies and of thicknesses of individual cenozones within particular series (Koch et al., 1989). Locally also short-lived emersions of some parts of platform occurred. In the Kras area such an subaerial exposure is indicated by emersion breccia on the boundary between the Brje and Povir Formations (Fig. 19), i.e. on the boundary between Aptian and Albian (Koch & Ogorelec, 1987; Jurkovšek et al. 1996; Jurkovšek 2010; ). Limestone of Valanginian to Albian age is often dolomitized, partly or totally, the dolomiti-zation being of late diagenetic character. To the upper part of Lower Cretaceous beds, of Albian age, Šribar (1979b and Dozet & Šribar 1991) attributed limestone and dolomite beds containing orbitolinas (Orbitolina ex gr. texana) and foraminifers (»Valdanchella« dercourti). Quite frequent in this beds are also miliolids, and requienids among the molluscs. A higher energy index within the Lower Cretaceous succession is indicated by rare beds con- taining ooids and pseudoooids. Both were transported into the quieter environment with micritic carbonate mud, and mixed between pellets and tiny fossils. Locally also smaller reefs and biostromes of corals, hydrozoans and algae existed. Such coral reef is known from Berriaian and Val-anginian at Zavrh on Banjšcice plateau (Turnšek & Buser, 1974), and from Aptian and Albian coral reefs at Kanalski vrh and environs on Banjšcice plateau (Turnšek & Buser, 1974; Grotsch, 1991; Grotsch et al., 1994), and on Kočevska gora (Turnšek et al., 1992) were described. In Aptian a smaller algal reef consisting predominantly of Lithocodium aggregatum (syn. Bacinella irregularis) existed on Mt. Sabotin (Koch et al., 2002). Within the Hauterivian succession occurs in western part of Trnovski gozd and on Mt. Sabotin a 15 to 40 meters thick packet of black biomic-ritic and biopelmicritic platy and bituminous limestone with chert nodules (»Trnovo platy limestone«, Plenicar & Buser, 1967) which contains up to 1.1 % Corg. Analyses of a number of samples indicate that this limestone could be regarded as a potential source rocks for hydrocarbons with low capability for their generation (Ogorelec et al., 1996a). Upper cretaceous beds were deposited on a more open and shallow shelf of a higher energy index. For them are characteristic light color of limestones, thick beds and rich rudist fauna (Plenicar, 2005; Plenicar & Jurkovšek, 1996, 1998). All types of limestones are represented, but packstone and grainstone are the most frequent. The Upper Cretaceous beds are exposed to a larger extent on the Trieste-Komen plateau and on Mt. Nanos, and to a lesser extent on Ja-vorniki Mts., in Dolenjska and Kočevje area. Owing to great thicknesses of individual beds, interesting appearance and good technical properties they are appreciated as architectural stone, and are quarried especially in the Kras region in numerous quarries. Dolomite beds are considerably less frequent than in the Lower Cretaceous succession. In spite of monotonous lithologic development the Upper Cretaceous beds can be biostratigrap-hically well subdivided on basis of fossils, especially foraminifers and rudists (Šribar & Plenicar, 1990; Plenicar, 1960, 1979, 2005, 2009; Jež, 2011). Such division is shown on Fig. 20 for the region of southwestern Slovenia. For Middle and Upper cenomanian among foraminifers Broeckina (Pas-trikella) balcanica is characteristic, for Upper Turonian the nonskeletal alga Aeolisaccus kotori, for coniacian and Lower Santonian foraminifer Pseudocyclammina sphaeroidea, for Upper San-tonian and campanian Keramospherina terge-stina, and for Maastrichtian Orbitoides media and Rhapydionina liburnica (Šribar & Plenicar, 1990). In the Trieste-Komen plateau region formations were defined in addition to cenozones : the Povir formation of Cenomanian age, Sežana formation of Upper Turonian, Coniacian and San-tonian, and the Lipica formation of Campanian (Jurkovšek et al., 1996; Jurkovšek, 2008, 2010, Jurkovšek & Kolar-Jurkovšek, 2007). Within the Repen formation comprising Lower Turonian in certain levels extremely numerous calcispheres occur that may become even rock-forming (cal-cispheric packstone), indicating a sea-level rise-between the Cenomanian and Turonian (Jenkyns 1985, 1991; Haq et al., 1987, Jurkovšek et al., 1996; Jurkovšek, 2010), i.e. the subsidence of the platform. A sedimentological and microfacial peculiarity within the lower part of Sežana formation is represented by a several meters thick horizon with large oncoids (Oncoidal limestone, Jurkovšek et al., 1996; Jurkovšek, 2010). This oncoidal horizon is widespread and is recognizable as a marker horizon throughout the Dinaric carbonate platform (Gušic & Jelaska, 1990; Tišljar et al., 2002). In the region of Dinaric carbonate platform two well-marked emersion phases occurred in the Upper Cretaceous that resulted in strati-graphic gaps. The first such phase in the interval from Upper Cenomanian to Coniacian happened on the northern edge of platform and it can be best recognized on Mt. Sabotin, wheras toward Mt. Nanos its extent is already smaller, covering only a part of Coniacian (Jež, 2011). In Kras area this gap cannot be recorded. The second emersion phase covered a wider time-span. In places on Kras subaerial exposure lasted for an insignificant time-range between Campanian and Maastrichtian, while more to the south (Matarsko podolje, Istria) it existed already from Senonian on, and lasted up to Eocene (Drobne, 1979; Buser, 1980; Jurkovšek et al., 1996; Otonicar, 2006, 2007; Jež, 2011). Results of emersion phases and karsti-fication are pockets of bauxitic clay. Within the Upper Cretaceous succession on the Trieste-Komen plateau black platy and bituminous limestones with chert nodules are characteristic, known in literature as »the Komen fish-shales« for the numerous fossil remains of fishes (Gorjanovic-Kramberger, 1895; Jurkovšek et al., 1996; Jurkovšek, 2010; Oavin et al., 2000; Palci et al., 2008). Primarily (Buser, 1968) these limestones were attributed to three horizons within the Albian-Cenomanian, Turonian and Senonian succession, however newer research revealed more horizons. In the interval from Cenomanian to Santonian they belong to the Komen limestone, and in the Santonian-Campanian part of the Lipica formation horizons of Tomaj limestone occur (Jurkovšek et al., 1996; Jurkovšek, 2008, 2010). The texture of Komen limestone is biomicritic and biopelmicritic, often with millimeter-scale lamination. It was deposited in shallow restricted lagoons under anaerobic conditions and on intertidal plains. The latter are indicated by torn laminae (»flat pebble conglomerate«), stromatolites and shrinkage pores. The microfossil assemblage is poor and atypical (foraminifers, ostracods, algae - mainly Thaumatoporella parvovesiculifera). Periodic communication of lagoons with the open sea is indicated by pelagic fossils. Next to fishes also other macrofossils occur in limestone, such as plants, saccocomas, ammonites and others (JURKOVŠEK & KOLAR-JURKOVŠEK, 1995, 2007; Do-BRusKiNA et al., 1999; Summesberger et al., 1996, 1999). The Tomaj limestone contains beds of bio-calcarenite as well, often showing graded bedding. Calcarenite is believed to have been deposited as allodapic limestone in local deepenings occurring within anoxic basins. owing to tectonics (Ogorelec et al. 1987). In spite of black color and smell of bitumen the Komen limestone contains only a scarce proportion of organic C, in major part up to 0.8 %, and only exceptionally to 1.7 %. Unfavorable for oil potential is the composition of organic matter which is predominantly of terrestrial origin (Ogorelec et al., 1996a,b). The Cretaceous time is terminated by limestones of the Liburnian Formation which continues further to Lower Paleocene. Biosparitic limestone is alternating with biomicritic varieties, and locally with stromatolitic beds. Characeans indicate sedimentation in brackish palustrine environment. In the lower part of Liburnian formation which is marked by Vreme beds, and is still of Maastrichtian age, the most charac-teristical foraminifer Rhapydionina liburnica (Stache) occurs, which is accompanied by milio-lids, rhizocodia, ostracods and molluscs, especially gyropleuras (Drobne, 1981; Drobne et al., 1989, 1995; Plenicar et al., 1992; Hotzl & Pavlo-vec, 1979). In this facies also thinner coal seams appear in places, which were mined in the past (Vremski Britof, Lipica, Sečovlje; Hamrla, 1959). The cretaceous-Tertiary (K/T) boundary in Slovenia is recognizable in Kras region where it was studied in several sections, at Dolenja vas (Drobne et al.,1988, 1989, 1995, 1996, 2009), on Sopada near Štorje (Ogorelec et al.t 2007), at Kozina (Delvalle & Buser, 1990), and Čebulovica (Ogorelec et al., 2001). On Italian side of the area it was studied at Padriče (Padriciano, Brazzati et al., 1996) and Bazovica (Basovizza, Riccamboni, 2005). Its geologic peculiarity is a shallow water facies development which is extraordinary and unique for the entire Mediterranean domain. The very boundary lies within a 0.2 do 2 meters thick emersion breccia deposited in an intertidal environment of a restricted lagoon with characteristic shrinkage pores, rhizocodium structures (Paronipora sp.), stromatolitic laminae and bauxite pockets (Jurkovšek et al., 1996; Ogorelec et al., 2007; Drobne et al., 2009). Limestone just below the boundary is light biomicrite and pelmicrite (wackestone and packstone), locally slightly marly, and dark biomicrite with gy-ropleuras and foraminifers (Drobne et al., 1995; Pugliese et al., 1995). Biomicritic limestone prevails just above the boundary in Lower Danian, and shows all characteristics of palustrine facies (Otonicar & Košir, 1998; Ogorelec et al., 2001; Košir 2004). In addition to the change of biota the boundary is marked also by a change of isotopic composition of limestone - an extraordinary, up to 8 %o enrichment with light 513C isotope exactly at the boundary (Dolenec et al., 1995; Ogorelec et al., 1995, 2007), an increased iridium con- tents (Hansen et al., 1995), and presence of glassy spherulae (Gregoric et al., 1998). Deeper-marine development of cretaceous Deeper-marine development of sedimentary rocks in the region of Slovenian basin continued from Jurassic into Cretaceous that, in addition, advanced northwards. For this deeper environment beds with intermediate limestone breccias are characteristic, in short the clastic development of Cretaceous (Plenicar, 1979, 2009). Flysch occurs in two thicker packets - as the lower flysch formation, 100 to 400 meters thick, in Aptian and Albian (Cousin, 1970), and as the upper, up to 800 meters thick flysch formation in the Upper Cretaceous (Buser, 1986). The source material for carbonate breccias were shallow-marine limestones that broke off the edge of the Dinaric platform, and slided down the slope, while the flysch was deposited from the northwest (Ogorelec, 1970; Kuscer et al., 1974). The total thickness of deeper-marine Cretaceous succession varies between 500 and more than 1000 meters. The most complete development of these strata of the Slovenian basin is found in Tolmin area (Buser, 1986a,b) and in eastern Sava folds between Krsko and Gorjanci Mts., whereas in the Bovec area and in central Slovenia they occur rather fragmentarily. From the standpoint of carbonate sedimen-tology and microfacies only three facies types or rock packets are interesting within the Cretaceous deeper water development: - white and light grey platy limestones of Berriasian age, that continue from the Upper Jurassic, - marly limestones of »scaglia« type of Albian to Turonian and »Senonian« ages, and - the Volce limestone of »Senonian« age. The oldest Cretaceous beds of deeper-marine development belong to the white micritic limestone of the biancone type (mudstone and wacke-stone) with chert nodules. It represents the continuation of sedimentation from the upper part of Jurassic. It is the uppermost part of a 100 to 250 meters thick limestone packet of which the Berriasian and Lower Valanginian age is determined by calpionellas (Calpionella elliptica, C. alpina, Tintinopsella hungarica) and radiolari-ans (Plenicar, 1979, 2009; Sribar, 1981; Buser, 1986). In the region of the Slovenian basin no sediments from Valanginian to Barremian are known at present. The succession starts transgressively with flysch rocks on biancone beds not earlier than in Aptian, whereas the sedimentation of flysch and intermediate limestone breccias in environs of Bohinj started already in Valanginian (Buser, 1986; Budkovic, 1978); their deposition lasted to the end of Lower Cretaceous. Age of this flysch has been dated by nanoplankton (Buser & Pavsic, 1978; Pavsic & Gorican, 1987; Pavsic, 1994). In the lower part of Upper Cretaceous, i.e. in Cenomanian and Turonian, reddish platy and marly limestones were deposited in the wider Tolmin area. They are interbedded with marlstones, chert sheets and with calcarenites, and the formation is known as »scaglia variegata« (Buser, 1986b). In the wider surroundings of Mt. Mangart such sediments appear already in Albian (Smuc, 2005). Age of these beds is determined with nanoplankton (Pavsic, 1979) and glo-botruncanas (Globotruncana helvetica, G. schne-egansi, G. sigali; Buser, 1986b). The variegated scaglia is followed by 100 to at most 300 meters of Volce limestone Formation. Characteristical for the Volce limestone is alternation of thin layers of biomicrite, calci-rudite and calcarenite with frequent intermediate chert sheets and nodules. The calciruditic beds often show graded bedding and lamination (Ogorelec et al., 1976). These beds were deposited by turbidity flows at basin margins, whereas the biomicritic sheets of mudstone type result from quiet pelagic phases. Thus, Volce limestone can be recognized as carbonate flysch or allodapic limestone. Autochthonous fossils are pelagic, mainly globotruncanas and radiolarians, while among the washed-in particles fragments of ru-dist valves, of echinoderms and of other bivalves occur. The most common globotruncanas are Globotruncana arca, G. calcarata, G. conica, G. elevata and G. lineiana lineiana (determined by L. Sribar, in Ogorelec et al., 1976) that occur from Upper Turonian to Campanian. North of Kobarid the Volce limestone passes into, or is replaced by, red marly limestone of the scaglia type (Ogorelec, 1970; Kušcer et al., 1974; Buser, 1986b; Šmuc, 2005) known as scaglia rossa, which contains in addition to species of globotruncanas, occurring in Volče limestone, also other ones (Radoicic & Buser, 2004). Above the Volče limestone and red scaglia again an up to 600 meters thick packet of flysch beds occurs. In fragments of coarse-grained flysch breccia of Senonian age that overlies the Volče limestone numerous corals were determined on Banjščice plateau (Turnšek & Buser, 1976). The flysch basin gradually shifted from Campanian on more and more southward, to Goriška Brda, to Trieste area and Istria (Buser, 1986b). Eastern Alps In surroundings of Zreče and Stranice near Slovenske Konjice a reef limestone with numerous rudists lies between clastites, consisting of claystones, siltstones, marlstones and a coal seam (Plenicar, 1971, 1993, 2005). In marlstones solitary corals are also frequent (Turnšek, 1994). Development of these beds has been compared by authors (Hamrla, 1988; Turnšek, 1994; Plenicar, 1971, 2009) to Gosau development of Cretaceous in the Northern Alps. Limestones of the Gosau facies are not considered in the present monography since they were not a subject of our researches. Literatura - References AGIP S.p.A. (Sartorio D. & Venturini S.) 1988: Southern Tethys Biofacies. AGIP, 235 p., S. Donato Milanese. Anderle, N. 1970: Stratigraphische und tektonische Probleme im Bereich des österreichischen Anteiles der Westkarawanken zwischen Rosenbach und Thörl unter Berücksichtigung der alpinen Orogenese. Geologija, 13: 116-132. 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Paleogeography, Palelclimatology, Paleo-ecology, 220/3-4: 333-360. Wilson, J.L. 1975: Carbonate Facies in Geologic History. Springer Verl., Berlin: 471 p. Zankl, H. 1971: Upper Triassic carbonate facies in the Northern Limestone Alps. In: Müller, G. (ed.): Se-dimentology of Parts of Central Europe, Guidebook. 8. Int. Sedim. Congress, Heidelberg: 147-185. Žalohar, J. & Celarc, B. 2010: Geološka zgradba Kamniško-Savinjskih Alp. V: Hitij T. et al. (eds.): Kraljestvo Tetide, Okameneli svet triasnih vretenčarjev Kamniško-Savinjskih Alp. Scopolia Suppl. 5, 43-53. TABLE - PLATES Tabla 1 - Plate 1 Zgornji perm - Upper Permian 1 Rekristaliziran mikritni apnenec s terigenimi zrni kremena in sljude. Bazalna plast zgornjeperm-skega zaporedja. Čadovlje pri Tržiču, X nikoli, preparat je obarvan z alizarinskim barvilom Recrystallized micritic limestone with terrigenous grains of quartz and mica. Basal layer of the Upper Permian succession. Čadovlje at Tržič, XN, alizarin red staininig 2 Biomikritni wackestone s številnimi preseki skeletnih alg vrste Gymnocodium bellerophontis in foraminiferami. Alge in foraminifere so bile v času diageneze izlužene, moldične pore pa so zapolnjene z avtigenim kremenom (belo). Masore pri Spodnji Idriji. Preparat je obarvan z alizarinskim barvilom Biomicritic wackestone with numerous algae of Gymnocodium bellerophontis species. Algae and foraminifers were leached during early diagenesis and moldic pores were filled with authigenic quartz (white). Masore at Spodnja Idrija, alizarin red staining 3 Biomikritni algni packstone s polži in fragmenti ehinodermov. Masore pri Spodnji Idriji Biomicritic algal packstone with gastropods and echinoderm fragments. Masore at Spodnja Idrija 4 Rekristaliziran gimnokodijski packstone s foraminifero Hemigordius sp. in ploščico ehinoderma. Javorjev dol pri Sovodnju. Značilni facies Žažarske formacije Recrystallised gymnocodian packstone with foraminifer Hemigordius sp. and echinoderm plate. Javorjev dol at Sovodenj. Characteristic facies of Žažar Formation 5 Žila sadre v mikritnem dolomitu. Karavanški cestni predor, 802. m, X nikoli Gypsum vein in micritic dolomite. Karavanke road tunnel, 802. m, XN 6 Kristali anhidrita v sparitnem dolomitu. Karavanški cestni predor, 670. m, X nikoli Anhydrite crystals in sparry dolomite. Karavanke road tunnel, 670. m, XN Tabla 1 - Plate 1 Tabla 2 - Plate 2 Zgornji perm - Upper Permian 1 Izpran gimnokodijski packstone s ploščicami ehinodermov. Struga Idrijce pri Spodnji Idriji Washed gymnocodian packstone with echinoderm plates. Idrijca river bed at Spodnja Idrija 2, 3 Rekristaliziran biomikritni packstone. Skeleti alg in foraminifer so bili v času diageneze izluženi, moldične pore pa so bile zapolnjene z avtigenim kremenom. Masore pri Spodnji Idriji. Preparat je obarvan z alizarinskim barvilom, sl. 2 - presevna svetloba, sl. 3 - X nikoli Recrystallised biomicritic packstone. Algal and foraminiferal skeletons were leached during early diagenesis and moldic pores were later cemented by authigenic quartz. Masore at Spodnja Idrija. Alizarin red staining, Fig. 2 in plane-polarized light, fig. 3 - XN 4 Prečni presek korale Waagenophyllum indicum v mikritni osnovi. Preko koralitov poteka stilolitni šiv. Malenski vrh nad Poljanami Transverse section of Waagenophyllum indicum coral in micritic matrix. Coralites are crossed by a stylolite. Malenski vrh above Poljane 5 Mikritni dolomit s presekom alge Permocalculus fragilis. Kalcitni skelet alge je bil v času diageneze izlužen (moldična poroznost), nato pa zapolnjen z anhidritom. Karavanški cestni predor, 650. m, X nikoli Micritic dolomite with Permocalculus fragilis algae. Calcitic algal skeleton was leached during early diagenesis (moldic porosity) and later cemented by anhidrite. Karavanke road tunnel, 650. m, XN Tabla 2 - Plate 2 Tabla 3 - Plate 3 Zgornji perm in permsko/triasna meja -Upper Permian and Permian/Triassic boundary 1 Rekristaliziran biomikritni wackestone s preseki foraminifere Climacammina sp. in skeleti alg. Javorjev dol pri Sovodnju Recrystallized biomicritic wackestone with Climacammina sp. foraminifer and algae. Javorjev dol at Sovodenj 2 Oolitni dolomit (oosparit) s še opazno prvotno strukturo kamnine. Izlužene moldicne pore po ooidih sta v pozni diagenezi zapolnila sparitni kalcit in kremen. Potok Košutnik pri Tržicu. Preparat je obarvan z alizarinskim barvilom Oosparitic dolomite with preserved primary oolitic texture. Leached moldic pores after ooids were cemented by sparry calcite and some quartz during late diagenesis. Košutnik creek at Tržic. Alizarin red staining 3, 4 Oolitni grainstone. Vecino ooidov je zajela poznodiagenetska dolomitizacija. Struga Idrijce pri Spodnji Idriji, Tesero horizont na P/T meji. Preparat je obarvan z alizarinskim barvilom Oolitic grainstone. Most of ooids were subjected to dolomitization during late diagenesis. Idrijca river bed at Spodnja Idrija, Tersero horizon at P/T boundary. Alizarin red staining 5 Sparitni dolomit (grainstone) z ohranjeno oolitno strukturo. Pore zapolnjuje poznodiagenetski sparitni kalcit. Redka terigena zrna kremena. Talnina premogovnika Velenje. Preparat je obarvan z alizarinskim barvilom Sparry dolomite (grainstone) with preserved oolitic structure. Intergranular pores are cemented by late diagenetic sparry calcite. Some terrigenous quartz grains. Footwall of Velenje coal mine. Alizarin red staining 6 Sparitni dolomit s slabo ohranjeno prvotno oolitno teksturo in z gnezdi sfalerita. Pb-Zn rudišce Trebelno pri Mokronogu, permsko/triasna meja Sparry dolomite with poorly preserved primary oolitic structure and with sphalerite crystals. Pb-Zn mine Trebelno at Mokronog, Permian/Triassic boundary Tabla 3 - Plate 3 Tabla 4 - Plate 4 Zgornji perm - Upper Permian 1 Satasti mikrosparitni dolomit. Pore, nastale z izluževanjem evaporitov, zapolnjuje kalcitni cement (rdeče). Javorjev dol pri Sovodnju. Preparat je obarvan z alizarinskim barvilom Microsparitic cellular dolomite. Vugs, caused by leaching of primary evaporite minerals are cemented by calcite (red). Javorjev dol at Sovodenj. Alizarin red staining 2 Gimnokodijski apnenec (packstone) s posameznimi foraminiferami in ploščicami ehinodermov. Rejc na Vojskarski planoti Gymnocodian packstone with some foraminifers and echinoderm plates. Rejc on Vojsko plateau by Idrija 3 Permocalculus fragilis in kopuče cianobakterij v mikritni osnovi - algni floatstone. Mažgon pri Jagrščah Algal floatstone with Permocalculus fragilis and microbial clusters. Mažgon at Jagršče 4 Sparitni dolomit z znaki dedolomitizacije (kalcitizacije). Najvišji horizont zgornjepermske Žažar-ske formacije. Javorjev dol pri Sovodnju Sparry dolomite, displaying dedolomitization (calcitization). Uppermost horizon of the Upper Permian Žažar Formation. Javorjev dol at Sovodenj 5 Mikritni dolomit (mudstone) z redkimi kalcitiziranimi radiolariji. Bazalne plasti Karavanške formacije. Čadovlje pri Tržiču Micritic dolomite (mudstone) with radiolarians. Basal beds of Karavanke Formation. Čadovlje at Tržič 6 Oolitni grainstone s sparitnim kalcitnim cementom. Tesero horizont na P/T meji. Masore pri Spodnji Idriji Oolitic grainstone with sparry calcite cement. Tesero horizon at the P/T boundary. Masore at Spodnja Idrija Tabla 4 - Plate 4 Tabla 5 - Plate 5 Spodnji trias - Lower Triassic 1, 2 Gastropodni wackestone. Številni preseki drobnih polžev. Redka zrna terigenega kremena (na sl. 1). Zalog na Bohorju Gastropod wackestone. Numerous sections of small gastropods. Rare grains of detrital quartz (on Fig. 1). Zalog at Mt. Bohor 3 Oolitni packstone. V enem od ooidnih jeder je opazen mikrogastropod. Apnenec je rahlo dolomiti-ziran. Lom pri Tržiču Oolitic packstone. Microgastropod can be seen in nucleus of one of ooids. Limestone is partly do-lomitized. Lom at Tržič 4 Biosparitni grainstone s številnimi gastropodi. Značilni facies spodnjetriasnega zaporedja. Cebine nad Trbovljami Biosparitic grainstone with numerous gastropods. Characteristic facies of Lower Triassic succession. Cebine at Trbovlje 5 Dolomitiziran bioosparitni packstone. Spodnji del preparata je obarvan z alizarinskim barvilom, zato je lepo viden obseg dolomitizacije. Podlipa pri Vrhniki Dolomitized bioosparitic packstone. Lower part of the thin-section is stained by alizarin red, displaying the extent of dolomitization. Podlipa at Vrhnika 6 Dolomitiziran gastropodni wackestone. Med polže je ujet tudi večji ooid, ki je rdeče obarvan s he-matitom. Laško Dolomitized gastropod wackestone. Among gastropods some ooids are present. Their reddish color is due to hematite pigment. Laško Tabla 5 - Plate 5 Tabla 6 - Plate 6 Spodnji trias - Lower Triassic 1, 4 Oosparitni grainstone (detajl). Ooidi so zaradi železovih hidroksidov obarvani rdečkasto. Na sl. 4 so vidna zajedanja med posameznimi ooidi zaradi raztapljanja apnenca v času diageneze. Kamnolom Kisovec pri Zagorju Oosparitic grainstone (detail). Ooids are reddish stained due to ferroan hydroxides. Kisovec quarry at Zagorje 2 Oosparitni dolomitni grainstone z medzrnskimi porami, nastalimi pri dolomitizaciji (belo). Izlake Oosparitic dolomitic grainstone with intergranular pores, formed during dolomitization (white). Izlake 3 Oosparitni grainstone. Apnenec je zajela vadozna diageneza; jedra ooidov so bila izlužena in kasneje zapolnjena s sparitnim kalcitom. Laško Oosparitic grainstone. Sediment was affected by vadose diagenesis. Ooid nuclei were leached and moldic pores were later cemented by sparry calcite. Laško 5 Oosparitni grainstone - detajl. Jedra večine ooidov so selektivno dolomitizirana; viden je tudi obrobni kalcitni cement. Vzorec je obarvan z alizarinskim barvilom. Masore pri Spodnji Idriji Oosparitc grainstone - detail. Ooid nuclei show selective dolomitization, rim calcite cement is evident too. Alizarin red staining. Masore at Spodnja Idrija 6 Oosparitni dolomitni packstone. Ooidi so opazni le po konturah in večjih dolomitnih zrnih. Ledina nad Sevnico Oosparitic dolomitic packstone. Primary rock structure is recognized by ooid contours and larger dolomite crystals. Ledina over Sevnica Tabla 6 - Plate 6 Tabla 7 - Plate 7 Spodnji trias - Lower Triassic 1 Rekristaliziran in dolomitiziran mikritni wackestone s preseki foraminifere Earlandia. Bazalne plasti tik nad P/T mejo. Masore pri Spodnji Idriji Recrystallized and dolomitized micritic wackestone with foraminifer Earlandia. Basal beds just above the P/T boundary. Masore at Spodnja Idrija 2 Meandrospira pusilla v rekristaliziranem mikrosparitnem apnencu (mudstone) z redkimi terigeni-mi zrni kremena. Tehovec pri Katarini nad Medvodami Meandrospira pusilla in recrystallized microsparitic limestone (mudstone) with rare terrigenous quartz grains. Tehovec by Katarina above Medvode 3 Izpran oopelmikritni dolomit - packstone. Številni ooidi so pomešani med pelete. Medzrnska poroznost, nastala pri pozni dolomitizaciji. Rimske Toplice Washed oopelmicritic dolomite - packstone. Numerous ooids are mixed among pellets. Intergranular porosity caused by late dolomitization. Rimske Toplice 4 Biosparitni packstone, ki ga sestavljajo ploščice ehinodermov. Vrhnji del spodnjetriasnega zaporedja. Zakamnik nad karavanškim cestnim predorom Biosparitic packstone composed of echinoderm plates. Upper part of Lower Triassic succession. Zakamnik above the Karavanke road tunnel 5 Biosparitni dolomitni grainstone, ki ga sestavljajo same ploščice ehinodermov. Lom pri Tržiču Biosparitic dolomitic grainstone, composed solely of echinoderm plates. Lom at Tržič 6 Pelmikritni packstone z velikim intraklastom (spodaj) in ooidi. Dedjek pri Polhovem Gradcu Pelmicritic packstone with one large intraclast (below) and ooids. Dedjek at Polhov Gradec Tabla 7 - Plate 7 Tabla 8 - Plate 8 Srednji trias (anizij) - Middle Triassic (Anisian) 1 Izpran intrabiosparitni packstone. Kamnino gradijo pretežno foraminifere in ehinodermi. Baba nad Cerknim Washed intrabiosparitic packstone. Foraminifers and echinoderm plates are the main rock constituents. Baba over Cerkno 2 Biopelmikritni packstone s foraminifero Meandrospira dinarica. Talnina premogovnika Velenje Biopelmicritic packstone with foraminifer Meandrospira dinarica. Footwall of Velenje coal mine 3 Kontura školjčne lupine v mikrosparitnem dolomitu. Todraž pri Gorenji vasi, vrtina P3/169 m Microsparitic dolomite with poorly preserved bivalve shell. Todraž at Gorenja vas, borehole P3/169 m 4 Fragmenti školjčnih lupin, inkrustrirani z ovoji cianobakterij - bafflestone. Detajl stromatolitne plasti. Geopetalna struktura z internim mikritom v medprostorih. Todraž pri Gorenji vasi, vrtina P3/157 m Molluscan fragments, encrusted by cyanobacteria - bafflestone. Detail of stromatolite layer. Geo-petal fabric with internal micrite in some pores. Todraž at Gorenja vas, borehole P3/157 m 5 Detajl izsušitvene pore z geopetalno strukturo (interni mikrit) v stromatolitnem dolomitu. Todraž pri Gorenji vasi, vrtina P3/142 m Shrinkage pore in stromatolitic dolomite - detail with geopetal fabric (internal micrite). Todraž at Gorenja vas, borehole P3/142 m 6 Detajl izsušitvene pore v stromatolitnem dolomitu z dvema generacijama cementov - obrobni cement pripada dolomitu z evhedralnimi zrni, osrednji del por pa zapolnjuje sparitni kalcit (rdeče). Preparat je obarvan z alizarinskim barvilom. Kamnolom Kotredež pri Zagorju Shrinkage pore in stromatolitic dolomite - detail with two generations of cement: euhedral dolomite crystals as rim cement (generation A) and sparry calcite (red, generation B). Alizarin red staining, Kotredež quarry near Zagorje Tabla 8 - Plate 8 Tabla 9 - Plate 9 Srednji trias -anizij) - Middle Triassic -Anisian) 1 Intrabiosparitni grainstone s preseki skeletnih alg. Stena pod Blejskim gradom Intrabiosparitic grainstone with skeletal algae. Bled castle wall 2 Preseki dasikladacejskih alg v grebenskem apnencu. Stena pod Blejskim gradom Sections of Dasycladal algae in reefal limestone. Bled castle wall 3 Izsušitvena pora v mikritnem dolomitu - detajl. Dve generaciji cementa - obrobni kalcit generacije A -rdeče) in sparitni dolomit generacije B -belo). Preparat je obarvan z alizarinskim barvilom. Todraž pri Gorenji vasi, vrtina P3/138 m Shrinkage pore in micritic dolomite - detail. Two generations of cement - rim calcite cement of generation A -red) and sparry dolomite of generation B -white). Alizarin red staining. Todraž at Gorenja vas, borehole P3/138 m 4 Mikrosparitni dolomit -mudstone). Pore, nastale pri poznodiagenetski dolomitizaciji in žilo zapolnjuje kalcit -rdeče). Vzorec je obarvan z alizarinskim barvilom, kamnolom Kotredež pri Zagorju Microsparitic dolomite mudstone. Pores, formed during late diagenesis and a vein are cemented by calcite -red). Alizarin red staining. Kotredež quarry at Zagorje 5 Biosparitni grainstone sestavljajo fragmenti alg -opazne po konturah in mikritnih ovojih) in redke foraminifere. Rudnik Črna pri Kamniku Biosparitic grainstone with algal fragments -recognized by contours and micritic envelopes) and some foraminifers. Črna mine at Kamnik 6 Sparitni dolomit, impregniran s sfaleritnimi kristali. Rudnik Topla pri Mežici Sparry dolomite, impregnated by sphalerite crystals. Topla mine near Mežica Tabla 9 - Plate 9 Tabla 10 - Plate 10 Srednji trias (ladinij) - Middle Triassic (Ladinian) 1, 2 Rekristaliziran intrasparitni packstone. Mikritni intraklasti so zaradi tektonike sploščeni in dajejo kamnini videz trakaste teksture. Na sl. 2 so prisotni tudi fragmenti ehinodermov (puščica). Recrystalized intrasparitic packstone. Micritic intraclasts are due to tectonics flat and give appearance of ribbon structure to the rock. Some echinoderm fragments on fig. 2. 1 - Kamna Gorica 2 - Kotredež pri Zagorju 3 Mikritni apnenec (wackestone) s tankolupinskimi školjkami in radiolariji. Kamnolom Kamna Gorica Micritic wackestone with thin-valved bivalves and radiolarians. Kamna Gorica quarry 4 Intramikritni apnenec, v katerem so pomešani drobci vulkanskih kamnin. Psevdoziljske plasti. Kotredež pri Zagorju Intramicritic limestone with fragments of volcanic rocks. Psevdozilja beds. Kotredež at Zagorje 5 Drobnozrnata konglomeratna breča, ki jo sestavljajo dolomitni drobci in kalcitno vezivo (rdeče). Preparat je obarvan z alizarinskim barvilom. Miklajč na Vojskarski planoti Fine-grained conglomeratic breccia, composed of dolomite grains and calcite matrix (red). Alizarin red staining. Miklajč on Vojsko plateau 6 Laminiran roženec s skeleti radiolarijev. Plast znotraj karbonatno - tufskega zaporedja. Kobilji curk pri Robu Laminated chert with radiolarian tests. Layer within carbonate - volcanic succession. Kobilji curk at Rob Tabla 10 - Plate 10 Tabla ll - Plate ll Srednji trias (zgornji ladinij) - Middle Triassic (Upper Ladinian) 1 Bioklastični framestone z dazikladacejnimi algami vrste Diplopora sp. Velika planina - Pod Frato Bioclastic framestone composed of dasycladacean algae of Diplopora sp. Velika planina - Pod Frato 2, 4 Preseki alge Diplopora sp. v apnencu tipa grainstone (sl. 2) in v izpranem mikritu (sl. 4). Sl. 2 - Velika planinna, sl. 4. - Okrešelj v Savinjskih Alpah Sections of algae Diplopora sp. in grainstone (Fig. 2) and in washed micrite (Fig. 4). Fig. 2 - Velika planina, Fig. 4 - Okrešelj in Savinja Alps 3 Gastropodi v biosparitnem apnencu tipa grainstone. Njihovi skeleti so opazni po mikritnih ovojih. Velika planina, odcep za Konja Gastropods in biosparitic grainstone. Their shells can be recognized by micritic coatings. Velika planina, turning towards Konj 5 Bioklastični grainstone s preseki dazikladacejnih alg in cianobakterij, ki obraščajo nekatere algne skelete. Ostenje pod Prisojnikom Bioclastic grainstone with dasycladacean algae and clusters of cyanobacteria. The latter overgrew some of algal skeletons. Prisojnik rock wall, Julian Alps Tabla 11 - Plate 11 Tabla 12 - Plate 12 Zgornji trias (karnij) - Upper Triassic (Carnian) 1, 2 Biomikritni packstone s preseki školjčnih lupin. Sl. 2 - detajl. Kamnolom Drenov grič pri Vrhniki Biomicritic packstone with bivalve shells. Fig. 2 - detail. Drenov grič quarry at Vrhnika 3, 4 Mikritni wackestone s posameznimi ostrakodi in školjčnimi lupinami. Sl. 3 - Limbarska gora nad Moravčami, sl. 4 - kamnolom Drenov grič pri Vrhniki Micritic wackestone with ostracods and bivalve shells. Fig. 3 - Limbarska gora above Moravče, Fig. 4 - Drenov grič quarry at Vrhnika 5 Alga Poikiloporella duplicata v stromatolitnem apnencu. Ščura nad Spodnjo Trebušo Poikiloporella duplicata algae in stromatolitic limestone. Ščura above Spodnja Trebuša 6 Sferoidalni onkoidni packstone. Gačnik na Vojskarski planoti Spheroidal oncoidal packstone. Gačnik on Vojsko plateau Tabla 12 - Plate 12 Tabla 13 - Plate 13 Zgornji trias (karnij) - Upper Triassic (Carnian) 1 Stromatolitni dolomit z izsušitvenimi porami. V večji pori sta opazni dve generaciji cementa - obrobni cement A in sparitni dolomit B. Borovnica Fenestral stromatolitic bindstone. Two generations of cement are present in fenestrae - rim cement of generation A and sparry dolomite of generation B. Borovnica 2 Mikritni apnenec z velikimi izsušitvenimi porami, v katerih opazujemo dve generaciji cementa - obrobni cement A in sparitni kalcit B ter geopetalno strukturo internega mikrita. Črna pri Kamniku Micritic limestone with shrinkage pores. Two generations of cement are present - rim cement A and sparry calcite B. Geopetal texture of internal micrite. Črna at Kamnik 3 Ploščice ehinodermov (rdeče) v dolomikritni osnovi. Pri dolomitizaciji kamnine so te ohranile prvotno kalcitno sestavo. Vzorec je obarvan z alizarinskim barvilom. Tamar Echinoid plates (red) in dolomicritic matrix. Their primary calcitic composition was preserved during dolomitization. Alizarin red staining, Tamar 4 Izpran pelmikritni packstone. Ščura nad Spodnjo Trebušo Pelmicritic packstone. Micritic matrix is mostly washed. Ščura above Spodnja Trebuša 5 Sparitni dolomit. Pore, nastale pri dolomitizaciji apnenca, zapolnjuje sparitni kalcit (rdeče). Vzorec je obarvan z alizarinskim barvilom. Tamar Sparry dolomite. Vugs, formed during dolomitization of primary calcite are cemented by sparry calcite. Alizarin red staining. Tamar 6 Sparitni dolomit s polji poznodiagenetskega kalcita. Vzorec je obarvan z alizarinskim barvilom, Krma v Julijskih Alpah Sparry dolomite with fields of late diagenetic calcite cement. Alizarin red staining. Krma in Julian Alps Tabla 13 - Plate 13 Tabla 14 - Plate 14 Zgornji trias (cordevol) - Upper Triassic (Cordevolian) 1, 2 Selektivna dolomitizacija pizoida v biosparitnem grainstonu. Na sl. 2 pizoid prečka stilolitni šiv. Krma v Julijskih Alpah Selective dolomitization of a pisoid in biosparitic grainstone. Pisoid on Fig. 2 is cut by stylolite. Krma in Julian Alps 3 Presek rdeče alge Solenopora cassiana. Apnenec je zajela poznodiagenetska dolomitizacija. Krma v Julijskih Alpah Transve section of red algae Solenopora cassiana. Limestone was affected by late diagenetic dolo-mitization. Krma in Julian Alps 4 Moldično poro po neznanem organizmu v biosparitnem grainstonu zapolnjujeta obrobni dolomitni cement generacije A (beli evhedralni kristali), osrednji del pore pa sparitni kalcit (rdeče). Vzorec je obarvan z alizarinskim barvilom. Krma v Julijskih Alpah Moldic vug in biosparitic grainstone (caused after an unknown organism) is cemented by two generations of cement - dolomite rim cement A (white, euhedral crystals) and sparry calcite in the central part (red). Alizarin red staining. Krma in Julian Alps 5 Sparitni dolomit z evhedralnimi conarnimi kristali, delno kalcitiziran (rdeče) in prepreden z avti-genim kremenom (belo). Vzorec je obarvan z alizarinskim barvilom. Gnezdo v grebenskem apnencu. Kamnolom v Hotavljah Dolosparite with euhedral conar crystals, partly calcitized (red) and cut by authigenic quartz (white). Alizarin red staining. Lens in reefal limestone. Hotavlje quarry 6 Sparitni dolomit z evhedralnimi conarnimi kristali. Leča v grebenskem apnencu kamnoloma Lesno Brdo pri Vrhniki Dolosparite with euhedral conar crystals. Lens in reefal limestone of quarry Lesno Brdo at Vrhnika Tabla 14 - Plate 14 Tabla 15 - Plate 15 Zgornji trias (karnij) - Upper Triassic (Carnian) 1, 2 Ogrodje grebenskega apnenca sestavljajo členkaste spongije vrste Alpinothalamia slovenica. Hu-dajužna Reef framework formed by encrusting sphyntozoan sponges Alpinothalamia slovenica. Hudajužna 3 Vzdolžni presek členkaste spongije vrste Solenolmia manon v grebenskem apnencu tipa framestone. Hudajužna Longitudinal section of sphynctozoan sponge Solenolmia manon in reefal framestone. Hudajužna 4 Kristali pirita v grebenskem spongijskem apnencu. Desno zgoraj je ploščica ehinoderma. Hu-dajužna Pyrite crystals in reefal spongiostromate limestone. Echinoid plate in upper right corner. Huda-južna 5 Detajl vzdolžnega preseka členkaste morske gobe Colospongia dubia v grebenskem apnencu. Hu-dajužna Detail of longitudinal section of sphyntozoan sponge Colospongia dubia in reefal framestone. Hu-dajužna 6 Prečni preseki korale Margarosmilia richthofeni v grebenskem apnencu tipa framestone. Corde-vol-jul. Pokljuka (zbirka D. Turnšek) Transversal section of Margarosmilia richthofeni coral in reefal framestone. Cordevolian-Julian. Pokljuka (D. Turnšek collection) Tabla 15 - Plate 15 Tabla 16 - Plate 16 Zgornji trias - karnij (jul in tuval) - Upper Triassic - Carnian (Julian and Tuvalian) 1,2 Onkoidno-ooidni grainstone s številnimi bioklasti. Posamezni ooidi in fragmenti moluskov so inkrustirani s cianobakterijami. Apnenec je tudi delno piritiziran. Helenski potok pri Mežici, 2. klastični horizont Oncoidal-ooidal grainstone with numerous bioclasts. Some ooids and molluscan fragments are encrusted by cyanobacterian mats. Limestone is partly pyritized. Helena creek at Mežica, 2nd clastic horizon 3,5 Onkoidno-oolitni packstone (rudstone). Osnova apnenca je rahlo izpran laporni mikrit. E - ploščice ehinodermov. Helenski potok pri Mežici, 2. klastični horizont Oncolitic-oolitic packstone (rudstone). Matrix of limestone is a partly washed marly micrite. E -echinoderm plates. Helena creek at Mežica, 2nd clastic horizon 4 Oolitni grainstone. V jedrih nekaterih ooidov so ploščice ehinodermov. Pikov vrh nad Helensko grapo pri Mežici Oolitic grainstone. Nuclei of some ooids are echinoderm plates. Pikov vrh above Helena creek at Mežica 6 Neskeletne alge s filamenti v stromatolitni plasti. Številne izsušitvene pore, zapolnjene s sparitnim kalcitom. Dolenja Trebuša - Čepovan Nonskeletal algae with filaments in stromatolitic layer. Numerous small fenestrae are cemented by sparry calcite. Dolenja Trebuša - Čepovan Tabla 16 - Plate 16 Tabla 17 - Plate 17 Zgornji trias - karnij (jul in tuval) - Upper Triassic - Carnian (Julian and Tuvalian) Globljemorski razvoj - Deep water environment 1 Lapornat wackestone s kalcitiziranimi radiolariji in drobirjem tankolupinskih moluskov. Kozja dnina v Vratih pod Triglavom Marly wackestone with calcitised radiolarians and fragments of thin-walled molluscans. Kozja dnina in Vrata below Triglav 2 Pelmikritni packstone z velikimi in drobnimi peleti ter redkimi terigenimi zrni kremena (belo). Belca v zahodnih Karavankah Pelmicritic packstone with pelets and rare terrigenous quartz grains (white). Belca valley in western Karavanke Mts. 3, 5 Biomikritni packstone z radiolariji in filamenti pelagičnih organizmov. Belca v zahodnih Karavankah Biomicritic packstone with radiolarians and pelagic filaments. Belca valley in western Karavanke Mts. 4 Biomikritni packstone s fragmenti moluskov in foraminiferami. Belca v zahodnih Karavankah Biomicritic packstone with mollusc fragments and foraminifers. Belca valley in western Karavanke Mts. 6 Spikulitni packstone z delno kalcitiziranimi spikulami spongij. Belca v zahodnih Karavankah Spiculite packstone with partly calcitized sponge spicules. Belca valley in western Karavanke Mts. Tabla 17 - Plate 17 Tabla 18 - Plate 18 Zgornji trias (norij in retij) - Upper Triassic (Norian and Rhaetian) Medplimsko okolje - Intertidal environment 1, 2 Stromatolitni loferit z drobnimi izsušitvenimi porami. Nekatere pore na sl. 1 so zapolnjene z internim mikritom. Sl. 1 - Grudnica pri Čepovanu, Sl. 2 - Begunjščica nad Ljubeljem Stromatolitic fenestral limestone - loferite. Some fenestra on fig. 1 are filled with internal micrite. Fig. 1 - Grudnica at Čepovan, Fig. 2 - Mt. Begunjščica above Ljubelj road pass 3, 4 Laminirana stromatolitna tekstura z ohranjeno strukturo cianobakterij. Sl. 3 in 4 - Dolenja Trebuša - Čepovan Laminated stromatolitic texture with preserved cyanobacteria. Figs. 3 and 4 - Dolenja Trebuša -Čepovan 5 Izsušitvene pore v mikritni osnovi - loferit. Pore kažejo geopetalno strukturo z internim mikritom in gravitacijskim cementom (puščice). Apnenec je delno zajela poznodiagenetska dolomitizacija. Dachsteinski apnenec, Smrekova draga na Trnovskem gozdu Shrinkage pores in micritix matrix - loferite. Geopetal texture is visible in fenestrae, evident by internal micrite and stalactitic cement (arrows). Limestone is partly affected by late diagenetic dolomitization. Dachstein limestone , Smrekova draga on Trnovski gozd 6 Detajl s sl. 5 Detail from fig. 5 Tabla 18 - Plate 18 Tabla 19 - Plate 19 Zgornji trias (norij in retij) - Upper Triassic (Norian and Rhaetian) Medplimsko okolje - Intertidal environment 1 Stromatolitni dolomit. Izsušitvene pore so bile v pozni diagenezi zapolnjene s sparitnim kalcitom (rdeče). Vzorec je obarvan z alizarinskim barvilom. Begunjščica nad Ljubeljem Stromatolitic dolomite. Shrinkage pores were filled by sparry calcite (red) during late diagenesis. Alizarin red staining. Mt. Begunjščica above Ljubelj road pass 2 Izsušitvena pora v izpranem pelmikritnem packstonu. Poro zapolnjuje interni mikrit, gravitacijski cement (puščica) in sparitni kalcit. Dachsteinski apnenec, Begunjščica Shrinkage pore in washed pelmicritic packstone. Pore is filled by internal micrite, gravitational cement (arrow) and sparry calcite. Dachstein limestone, Mt. Begunjščica 3 Mikritni mudstone z redkimi intraklasti in izsušitvenimi porami - loferit. Čepovan Fenestral mudstone with rare intraclasts and shrinkage pores - loferite. Čepovan 4 Stromatolitni dolomit - bafflestone z izsušitvenimi porami. Glavni dolomit. Borovnica Stromatolitic dolomite - bafflestone with shrinkage pores. Main dolomite. Borovnica 5 Laminiran dolomit z izsušitvenimi razpokami, ki kažejo na medplimsko okolje in z drobnimi izsušitvenimi porami. Dolenjske Toplice, vrtina V8/335 m Laminated dolomite with desiccation cracks and fine shrinkage pores. Dolenjske Toplice, borehole V8/335 m 6 Pelmikritni loferit z izsušitvenimi porami, ki jih zapolnjuje sparitni kalcit. Smrekova draga na Trnovskem gozdu Pelmicritic loferite with shrinkage pores, filled by sparry calcite. Smrekova draga on Trnovski gozd Tabla 19 - Plate 19 Tabla 20 - Plate 20 Zgornji trias (norij in retij) - Upper Triassic (Norian and Rhaetian) 1 Grainstone s številnimi preseki alge Thaumatoporella parvovesiculifera in peleti. Smrekova draga na Trnovskem gozdu Algal grainstone with algae Thaumatoporella parvovesiculifera and pellets. Smrekova draga on Trnovski gozd 2 Korozijska votlina z internim mikritom, v katerega so bile naplavljene lupine ostrakodov. Polov-nik pri Bovcu Solution cavity filled by internal micrite with washed in ostracod fragments. Mt. Polovnik at Bovec 3 Izpran pelmikritni packstone z izsušitvenimi porami - loferit. Pore zapolnjuje sparitni kalcit. Grudnica pri Čepovanu Washed pelmicritic packstone with shrinkage pores - loferite. Fenestrae are filled by sparry calci-te. Grudnica at Čepovan 4 Laminiran dolomit z izsušitvenimi porami in razpokami ter strukturami po stromatolitnih fila-mentih. Medplimsko okolje. Borovnica Laminated dolomite with shrinkage pores, desiccation cracks and structures, after stromatolitc filaments. Supratidal environment. Borovnica 5 Presek alge (solenopore) v izpranem intrabiomikritnem apnencu. Javorški vrh na Trnovskem gozdu Section of algae (Solenopora) in washed intrabiomicritic limestone. Javorški vrh on Trnovski gozd 6 Rekristalizirani koraliti v pelmikritnem apnencu - framestone. Moldične pore po koralitih zapolnjuje sparitni kalcit. Dachsteinski apnenec, Čepovan - Lokovec Coralite contours in recrystallized pelmicritic framestone. Moldic pores are cemented by sparry calcite. Dachstein limestone, Čepovan - Lokovec Tabla 20 - Plate 20 Tabla 21 - Plate 21 Zgornji trias (norij in retij) - Upper Triassic (Norian and Rhaetian) 1 Vadozni pizoidi, inkrustirani s cianobakterijami in s sparitnim cementom v medprostorih. Glavni dolomit. Koprivnik pri Kočevju Vadose pisoids, encrusted by cyanobacteria. Sparry dolomite between the pisoids. Main dolomite. Koprivnik at Kočevje 2 Vadozni pizoidi v intramikritnem dolomitu z izsušitvenimi porami. Trenta Vadose pisoids in the intramicritic dolomite with shrinkage pores. Trenta 3 Večkratno preraščanje algnega onkoida, inkrustiranega z ovoji cianobakterij. Glavni dolomit. Spodnja Trebuša - Čepovan Multiple owergrowth of algal oncoide, encrusted by cyanobacteria. Main dolomite. Spodnja Tre-buša - Čepovan 4 Onkoid v pelmikritnem packstonu, ki ga je zajela poznodiagenetska dolomitizacija. Begunjščica Algal oncoid in fenestral pelmicritic packstone, affected by late dolomitization. Mt. Begunjščica 5 Intramikritni dolomit z izsušitvenimi porami (A) prehaja v horizont z vadoznimi pizoidi (B), te pa prerašča stromatolitni bafflestone z izsušitvenimi porami (C). Korozijske votline med pizoidi zapolnjuje več generacij dolomitnega cementa (kokardna struktura). Glavni dolomit. Krn v Julijskih Alpah Intramicritic dolomite with shrinkage pores (A) pass to horizon with vadose pisoids (B), ower-grown by stromatolitic bafflestone with shrinkage pores (C). Solution cavities in pisoid horizon are filled with two generations of sparry dolomite (cockade texture). Main dolomite. Mt. Krn in Julian Alps Tabla 21 - Plate 21 Tabla 22 - Plate 22 Zgornji trias (norij in retij) - Upper Triassic (Norian and Rhaetian) 1 Spongija Cheilosporites v mikritnem apnencu - framestone. Dachsteinski apnenec. Nomenj pri Bohinjski Bistrici Cheilosporites sponge in micritic framestone. Dachstein limestone. Nomenj at Bohinjska Bistrica 2 Grebenski apnenec - framestone s koralami in s korozijskimi votlinami. Te zapolnjujeta dve generaciji sparitnega kalcita. Nomenj pri Bohinjski Bistrici Reef framestone with corals and small solution cavities, filled with two generations of sparry cal-cite. Nomenj at Bohinjska Bistrica 3,4 Gastropodni grainstone. Hišice polžev so ohranjene po mikritnih ovojih. Dachstainski apnenec. Čepovan - Lokavec Gastropode grainstone. Gastropod shells are preserved after micritic envelopes. Dachstein limestone. Čepovan - Lokavec Tabla 22 - Plate 22 Tabla 23 - Plate 23 Spodnja jura (lias) - Lower Jurassic (Lias) 1 Biomikritni mudstone z lupinami moluskov in s foraminiferami. Preserje pri Borovnici Biomikritic mudstone with bivalve shells and some foraminifers. Preserje at Borovnica 2 Alga Paleodasycladus mediterraneous v biosparitnem apnencu - grainstone. Preserje pri Borovnici Paleodasycladus mediterraneous algae in biosparitic grainstone. Preserje at Borovnica 3 Intrapelmikritni packstone z izsušitvenimi porami. V večji pori je viden gravitacijski cement (puščica). Javorški vrh na Trnovskem gozdu Intrapelmicritic packstone with shrinkage pores. In a larger pore gravitational cement (arrow) is visible. Javorški vrh on Trnovski gozd 4 Školjčne lupine v intramikritnem packstonu. Dežnikasta poroznost pod lupino, pore zapolnjuje sparitni kalcit. Javorški vrh na Trnovskem gozdu Bivalve shells in intramicritic packstone. Umbrella porosity under some shells; pores are filled with sparry calcite. Javorški vrh on Trnovski gozd 5 Moldična poroznost po fragmentu debelolupinske školjke v oosparitnem apnencu. Pora je zapolnjena s sparitnim kalcitom. Javorški vrh na Trnovskem gozdu Moldic porosity after thick-walled shell fragment in oosparitic limestone. The pore was later filled by sparry calcite. Javorški vrh on Trnovski gozd 6 Ooidi z mikritno strukturo, naplavljeni v pelsparitni packstone. Racna gora pri Ložu Ooids with micritic structure, washed in pelsparitic packstone. Racna gora at Lož Tabla 23 - Plate 23 Tabla 24 - Plate 24 Spodnja jura (lias) - Lower Jurassic (Lias) 1 Oolitni grainstone s školjčnimi lupinami, ki so na konveksni strani inkrustirane z ovoji cianobak-terij. Dežnikasta poroznost pod lupinami školjk. Dolenjske Toplice, vrtina V6/120 m Oolitic grainstone with bivalve shells. On the convex side they are encrusted by cyanobacterial mats. Umbrella porosity under shells. Dolenjske Toplice, borehole V6/ 120 m 2 Ooidi v mikritni osnovi - packstone. Različna struktura ovojev (mikritna in radialna struktura kalcita). Grčarevec - Kalce Ooids in micritic matrix - packstone. Micritic and radial-fibrous texture of ooid envelopes. Grčarevec - Kalce 3 Oosparitni grainstone s teksturo »polmeseca«, ki je rezultat meteorske diageneze in izluževanja evaporitnih ali aragonitnih kristalov. Geopetalna struktura. Javorški vrh na Trnovskem gozdu »Half moon« ooids in oospatitic grainstone. Nuclei in most ooids have dropped to the bottom of the concetric outer layers, forming geopetal fabric. Such ooids are product of evaporite or arago-nite solution process during meteoric diagenesis. Javorški vrh on Trnovski gozd 4 Oosparitni grainstone z različno velikimi ooidi z radialno strukturo. Nekateri ooidi so zdrobljeni in ponovno »regenerirani«. Gozd pri Colu Oosparitic grainstone. Ooids of different diameter have radial-fibrous envelopes. Some ooids are broken and show »regeneration«. Gozd at Col 5 Oosparitni grainstone. Jedra nekaterih ooidov so ploščice ehinodermov. Javorški vrh na Trnovskem gozdu Oosparitic grainstone. Echinoid plates serve as nuclei in some ooids. Javorški vrh on Trnovski gozd 6 Sparitni dolomit z ohranjeno strukturo ooidov. Onek pri Kočevju Sparry dolomite with preserved primary ooid structure. Onek at Kočevje Tabla 24 - Plate 24 Tabla 25 - Plate 25 Spodnja jura (lias) - Lower Jurassic (Lias) Oolitni apnenec - grainstone, ki ga je zajela selektivna poznodiagenetska dolomitizacija. Ta je osredotočena na mikritna jedra ooidov. Ploščice ehinodermov kot jedra nekaterih ooidov. Vrhpeč pri Trebnjem Oolitic grainstone affected by selective late diagenetic dolomitization, focused on micritic nuclei of ooids. Echinoid plates in some ooid nuclei. Vrhpeč at Trebnje Oosparitni grainstone, ki ga je zajela selektivna poznodiagenetska dolomitizacija. Ta prodira iz cementa v ooide. Vrhnika - Logatec Oosparitic grainstone, affected by selective late diagenetic dolomitization, prograding from pores into ooid grains. Vrhnika - Logatec Detajl oosparitnega apnenca. Opazni sta dve generaciji cementa - obrobni cement A (puščica) in sparitni kalcit B. Javorški vrh na Trnovskem gozdu Detail of oosparitic limestone. Two generations of cement - rim cement A (arrow) and sparry cal-cite are evident. Javorški vrh on Trnovski gozd Oosparitni grainstone z značilno mešano zgradbo ooidov - mikritnimi jedri in radialnimi kristali v zunanjih ovojih. Verd pri Vrhniki Oosparitic grainstone with typical mixed ooid composition - micritic ooid nuclei are owergrown with radial-fibrous calcite lamellae. Verd at Vrhnika Oolitni apnenec - grainstone. Zaradi tektonike so ooidi rahlo deformirani. Izstopa obrobni cement. Krka (zbirka S. Dozeta) Oolitic grainstone. Ooids are slightly deformed due to tectonics. Rim cement is most evident. Krka (S. Dozet collection) Oosparitni grainstone s stalaktitičnim cementom (puščica) pod nekaterimi ooidi, ki kaže na diage-nezo v meteorskem okolju. Grčarevec - Kalce Oosparitic grainstone. Stalactitic cement under some ooids (arrow) is indicating diagenesis in meteoric environment. Grčarevec - Kalce 1 2 3 4 5 6 Tabla 25 - Plate 25 Tabla 26 - Plate 26 Spodnja jura (lias) - Lower Jurassic (Lias) 1 Bioosparitni grainstone z ooidi, iglicami ehinodermov in rekristaliziranimi koraliti. Kozjak pri Dobrnicu (zbirka S. Dozeta) Bioosparitic grainstone with ooids, echinoid spines and recrystallized coralites. Kozjak at Dobrnic (S. Dozet collection) 2 Ooidi, naplavljeni v pelsparitni packstone. Racna gora pri Ložu Ooids washed into pelsparitic packstone. Racna gora at Lož 3 Intrabiosparitni grainstone s foraminifero (prehodna oblika med Mayncina sp. in Lituosepta sp.) Javorški vrh na Trnovskem gozdu Foraminifer in intrabiosparitic grainstone (transitional form from Mayncina sp. in Lituosepta sp.) Javorški vrh on Trnovski gozd 4 Lumakela drobnih brahiopodov v biosparitnem grainstonu. Javorški vrh na Trnovskem gozdu Lumachelle of fine brachiopod valves in biosparitic grainstone. Javorški vrh on Trnovski gozd 5 Rekristaliziran presek spongije - detajl. Kamnolom Vrhpec pri Trebnjem Section of recrystallized sponge - detail. Vrhpec quarry at Trebnje 6 Sparitni dolomit z odprtimi medzrnskimi porami, ki so nastale pri pozni dolomitizaciji kamnine. Prvotna oolitna tekstura je še ohranjena. Bistra pri Vrhniki Sparry dolomite with open intergranular pores, formed during the late dolomitization. Primary oolitic structure is still evident. Bistra at Vrhnika Tabla 26 - Plate 26 Tabla 27 - Plate 27 Zgornja jura - Upper Jurassic 1 Biomikritni apnenec - packstone s številnimi algami, moluski in ooidi. V večjih skeletih alg sta vidna stalaktitični cement (puščica) in interni mikrit. Ambrus v Suhi Krajini (zbirka S. Dozeta) Biomicritic limestone - packstone with numerous algae, molluscan shells and smal ooids. In larger algal fragments stalactitic cement (arrow) and internal micrite are evident. Ambrus in Suha Krajina (S. Dozet collection) 2 Detajl vzorca s slike 1 Detail of the sample on Fig. 1 3 Preseki alge Clypeina jurassica v intrapelmikritnem apnencu. Zgornja jura - malm, Krnica na Trnovskem gozdu Clypeina jurassica algae in intrapelmicritic matrix. Upper Jurassic - Malm, Krnica on Trnovski gozd 4 Fragmenti alge Clypeina jurassica v drobnozrnatem oolitnem apnencu - grainstone. Drobci alg so obdani z oolitnimi ovoji. Zgornja jura - malm. Krnica na Trnovskem gozdu Clypeina jurassica fragments in fine grained oolitic grainstone. Algal fragments are coated by oolitic envelopes. Upper Jurassic - Malm. Krnica on Trnovski gozd 5 Presek alge Clypeina jurassica v pelmikritni osnovi. Apnenec je zajela poznodiagenetska dolomi-tizacija. Vrhnika - Logatec Algae Clypeina jurassica in pelmicritic matrix. Limestone was affected by late diagenetic dolomi-tization. Vrhnika - Logatec Tabla 27 - Plate 27 Tabla 28 - Plate 28 Zgornja jura - Upper Jurassic 1 Biointrasparitni grainstone. Večja školjčna lupina (puščica) je inkrustirana z ovoji cianobakterij. Krnica na Trnovskem gozdu Biomicritic grainstone. Molluscan shell (arrow) is encrusted by cyanobacteria. Krnica on Trnovski gozd 2 Intraoosparitni grainstone. Nekateri intraklasti so prevlečeni z oolitnimi ovoji. Vrhnika - Logatec Intraoosparitic grainstone. Some intraclasts are coated with oolitic laminae. Vrhnika -Logatec 3 Intrapelmikritni packstone z izsušitvenimi porami - loferit. Oolitni ovoji okrog večjih intrakla-stov. Krnica na Trnovskem gozdu Intrapelmicritic packstone with shrinkage pores - loferite. Oolitic laminae around bigger intraclasts. Krnica on Trnovski gozd 4 Intrabiosparitni apnenec z velikimi tintininami - packstone. Vrhnika - Logatec, stara cesta (Snežni grič) Intrabiosparitic packstone with large tintinnids. Vrhnika - Logatec, old road (Snežni grič) 5 Intrapelmikritni packstone z izsušitvenimi porami - loferit. Racna gora pri Ložu Intrapelmicritic fenestral packstone - loferite. Racna gora at Lož Tabla 28 - Plate 28 Tabla 29 - Plate 29 Zgornja jura (malm) - Upper Jurassic (Malm) Grebenski razvoj - Reef facies 1 Koraliti razvejane kolonijske korale Stylosmilia corallina. Malm, Kal nad Kanalom, negativni odtis (zbirka D. Turnšek) Corallites of dendroid colonial coral Stylosmilia corallina. Malm, Kal nad Kanalom, negative imprint (D. Turnšek collection) 2 Korala Dermosmilia laxata v mikritni osnovi. Zatišni greben. Col na Trnovskem gozdu, negativni odtis (zbirka D. Turnšek) Dermosmilia laxata coral in micritic matrix. Inner-reef facies. Col on Trnovski gozd, negative imprint (D. Turnšek collection) 3 Presek korale Fungiastrea. Otlica na Trnovskem gozdu Section of Fungiastrea coral. Otlica on Trnovski gozd 4 Presek korale Clausastraea pseudoconfluens. Kal nad Kanalom, negativni odtis (zbirka D. Turnšek) Section of Clausastraea pseudoconfluens coral. Kal nad Kanalom, negative imprint (D. Turnšek collection) 5 Presek stromatoporoida Ellipsactinia. Turški klanec na Trnovskem gozdu, negativni odtis Ellipsactinia stromatoporoid. Turški klanec on Trnovski gozd, negative imprint Tabla 29 - Plate 29 Tabla 30 - Plate 30 Jura in spodnja kreda - Jurassic and Lower Cretaceous Globljemorski razvoj - Deeper-marine facies 1 Biomikritni packstone s številnimi ploščicami ehinodermov, posameznimi foraminiferami in redkimi zrni glavkonita (zeleno). Dogger. Mangart, talnina manganskega horizonta Biomicritic packstone with numerous echinoderm plates. Some foraminifers and glauconite grains (green) are present too. Dogger. Mt. Mangart, footwall of manganese horizon 2 Radiolarijski spikulit - packstone. Mikritna osnova je močno okremenjena. Dogger-Malm. Bavšica pri Bovcu. X nikoli Radiolaria-bearing spiculitic packstone. Micritic matrix is heavily silicified. Dogger-Malm. Bavšica at Bovec. XN 3 Krinoidni packstone s ploščicami ehinodermov. Dogger. Mangart Crinoidal packstone with echinoderm plates. Dogger. Mt. Mangart 4 Aptihi in kalpionele v mikritni osnovi - wackestone. Tithonij-berriasij. Čisti vrh v Trenti Aptychus-bearing wackestone with some calpionellids. Tithonian-Berriasian. Čisti vrh in Trenta 5, 6 Kalpionele v mikritni osnovi - wackestone. Na sl. 6 so prisotni še radiolariji. Berriasij Calpionellid wackestone. In Fig. 6 some radiolarians are present too. Berriasian 5 - Vas na Skali v Trenti 6 - Bavšica pri Bovcu Tabla 30 - Plate 30 Tabla 31 - Plate 31 Srednja jura (dogger) - Middle Jurassic (Dogger) Globljemorski razvoj, manganski horizont -Deeper-marine environment, manganese horizon 1 Manganove skorje obraščajo ploščico ehinoderma. Ravni Laz pri Bovcu Manganese crusts on echinoid plate. Ravni Laz at Bovec 2 Manganovi mikrogomolji v biomikritnem apnencu - packstone. Ravni Laz pri Bovcu Mn-micronodules in biomicritic packstone. Ravni Laz at Bovec 3 Biomikritni packstone s ploščicami ehinodermov, drobci školjčnih lupin, foraminifer in juvenilnih amonitov. Dolina Triglavskih jezer Biomicritic packstone with echinoid plates, shell debris, foraminifers and juvenile ammonites. Triglav lakes valley 4 Biomikritni apnenec z juvenilnimi amoniti in ehinodermi. Dolina Triglavskih jezer Biomicritic limestone - packstone with juvenile ammonites and echinoids. Triglav lakes valley 5 Detajl Fe-Mn gomolja s conarno »stromatolitno« teksturo. Jezero v Lužnici pod Krnom Detail of Fe-Mn nodule showing zonar »stromatolitic« structure. Jezero v Lužnici below Mt. Krn 6 Krinoidni apnenec. Ploščice ehinodermov so obdane z manganovimi ovoji. Dolina Triglavskih jezer Crinoidal packstone. Echinoderm plates with manganese encrustations. Triglav lakes valley Tabla 31 - Plate 31 Tabla 32 - Plate 32 Spodnja kreda - Lower Cretaceous 1 Pelmikritni packstone. Valanginij. Dvor pri Žužemberku Pelmicritic packstone. Valanginian. Dvor at Žužemberk 2 Drobni onkoidi v rahlo izpranem pelmikritnem packstonu. Hauterivij. Dvor pri Žužemberku Small oncoids in pelmicritic, partly washed packstone. Hauterivian. Dvor at Žužemberk 3, 4 Favreinski apnenec - packstone s številnimi prečnimi in vzdolžnimi preseki mikrokoprolitov raka Favreina salavensis. Berriasij. Logatec - Vrhnika Packstone with numerous radial and longitudinal sections of microcoprolite of decapod crabs Fa-vreina salavensis. Berriasian. Logatec - Vrhnika Fig. 4 - detail 5 Biomikritni apnenec s problematičnim mikrofosilom Bacinella irregularis. Barremij. Sviščaki pod Snežnikom Microproblematic fossil Bacinella irregularis in biomicritic limestone. Barremian. Sviščaki at Snežnik 6 Biomikritni wackestone s preseki alge Salpingoporella dinarica. Aptij. Trnovo pri Novi Gorici Algal wackestone with Salpingoporella dinarica. Aptian. Trnovo at Nova Gorica Tabla 32 - Plate 32 Tabla 33 - Plate 33 Spodnja kreda - Lower Cretaceous 1 Dolomitni romboedri s conarno rastjo v mikritnem apnencu. Poznodiagenetska dolomitizacija. Valanginij. Kočevski Rog - Podturn Dolomite rhombohedrons with porphyrotopic zonar fabrics in micritic matrix. Late diagenetic dolomitization. Valanginian. Kočevski Rog - Podturn 2 Stromatolitni apnenec - bindstone z izsušitvenimi porami. Aptij. Snežnik Stromatolitic boundstone with shrinkage pores. Aptian. Mt. Snežnik 3 Intraoosparitni packstone. Jedra več ooidov predstavljajo foraminifere. Albij. Nadrt na Hrušici (zbirka J. Ježa) Intraoosparitic packstone. Foraminifers as nuclei in some ooids. Albian. Nadrt on Hrušica (J. Jež collection) 4 Biomikritni mudstone/wackestone z lupinami ostrakodov. Albij. Nadrt na Hrušici (zbirka J. Ježa) Biomicritic mudstone/wackestone with ostracod slells. Albian. Nadrt on Hrušica (J. Jež collection) 5 Koraliti grebenske korale Dermosmilia cretacica. Barremij - sp. aptij. Osojnice na Banjški planoti (zbirka D. Turnšek) The colony of reef-forming coral Dermosmilia cretacica. Barremian - Lower Aptian. Osojnice on Banjšice plateau (D. Turnšek collection) 6 Laminiran mikritni apnenec z neizrazito stromatolitno strukturo in s stilolitnimi šivi. Valanginij. Dvor pri Žužemberku Laminated micritic limestone with indistinctive stromatolitic texture and stylolites. Valanginian. Dvor at Žužemberk Tabla 33 - Plate 33 Tabla 34 - Plate 34 Spodnja in zgornja kreda - Lower and Upper Cretaceous 1 Orbitolina Mesorbitolina subconcava v pelmikritnem apnencu tipa wackestone. Albij. Trnovo pri Novi Gorici Mesorbitolina subconcava in pelmicritic wackestone. Albian. Trnovo at Nova Gorica 2 Presek alge Thaumatoporella parvovesiculifera v pelbiomikritnem apnencu - packstone. Turonij. Nanos (zbirka J. Ježa) Thaumatoporella parvovesiculifera in pelbiomicritic packstone. Turonian. Mt. Nanos (J. Jež collection) 3 Orbitoline v intrabiosparitnem apnencu - grainstone. Spodnji cenomanij. Sabotin (zbirka J. Ježa) Intrabiosparitic grainstone with orbitolinas. Lower Cenomanian. Mt. Sabotin (J. Jež collection) 4 Intraklasti, foraminifere in peleti v izpranem apnencu tipa packstone. Redke izsušitvene pore. Cenomanij. Nadrt na Hrušici (zbirka J. Ježa) Washed intrabiopelmicritic packstone with rare shrinkage pores. Cenomanian. Nadrt on Hrušica (J. Jež collection) 5 Oolitni boksit. Santonij - turonij. Nanos - Podraška bajta (zbirka J. Ježa) Oolitic bauxite. Santonian - Turonian. Mt. Nanos - Podraška bajta (J. Jež collection) 6 Foraminiferni miliolidni apnenec - packstone. Santonij (Lipiška formacija). Rodik pri Kozini Foraminiferal miliolid packstone. Santonian (Lipica Formation). Rodik at Kozina Tabla 34 - Plate 34 Tabla 35 - Plate 35 Zgornja kreda - Upper Cretaceous 1 Izpran biopelmikritni packstone s foraminifero Dicyclina schlumbergeri. Santonij - campanij -Lipiška formacija). Gabrk pri Sežani Foraminifer Dicyclina schlumbergeri in washed biopelmicritic packstone. Santonian - Campanian -Lipica Formation). Gabrk at Sežana 2 Izpran miliolidni packstone. Santonij - campanij -Lipiška formacija). Gabrk pri Sežani Washed miliolid packstone. Santonian - Campanian -Lipica Formation). Gabrk at Sežana 3 Mikritni apnenec - mudstone z izsušitvenimi porami - loferit. Maastrichtij -Liburnijska formacija). Suhadole pri Štorjah Mudstone with shrinkage pores - loferite. Maastrichtian -Liburnia Formation). Suhadole at Štorje 4 Močno izpran mikritni apnenec - packstone. Maastrichtij -Liburnijska formacija). Vremski Britof Washed micritic packstone. Maastrichtian -Liburnia Formation). Vremski Britof 5, 6 Algni wackestone s številnimi preseki vrste Decastronema -ex. Aeolisaccus) kotori -sl. 5) in D. barattoloi -sl. 6) ter posamezne foraminifere -Fleuryana adriatica). Turonij - Santonij -Sežanska Formacija) Wackstone with numerous sections of Decastronema -ex. Aeolisaccus) kotori -fig. 5), D. barattoloi -fig. 6) and some foraminifers -Fleuryana adriatica). Turonian - Santonian -Sežana Formation) 5 - Veliki Medvedjak pri Sežani 6 - Nanos -zbirka/collection of J. Jež) Tabla 35 - Plate 35 Tabla 36 - Plate 36 Zgornja kreda - Upper Cretaceous 1 Biomikritni wackestone s presekom rudistne lupine, ki jo je zajela intenzivna endolitizacija. Ma-astrichtij. Liburnijska formacija. Senadole pri Štorjah Biomicritic wackestone with a section of rudist shell, affected by intensive endolitization. Ma-astrichtian. Liburnia Formation. Senadole at Štorje 2, 3 Debelozrnat biokalkarenit iz drobcev rudistnih školjk. Coarse-grained biocalcarenite, composed of rudist shell fragments. 2 - Turonij /Turonian. Kopriva pri Dutovljah 3 - Cenomanij/Cenomanian. Nadrt na Hrušici -zbirka/collection of J. Jež) 4 Biopelmikritni packstone s številnimi preseki foraminifere Orbitoides media Maastrichtij. Pre-stranek pri Postojni Biopelmicritic packstone with numerous sections of foraminifer Orbitoides media Maastrichtian. Prestranek at Postojna 5 Biopelmikritni packstone s številnimi kalcisferami in posameznimi pelagičnimi foraminiferami. Coniacij. Komenski apnenec znotraj Sežanske formacije. Lipa pri Komnu Biopelmicritic packstone with numerous calcispheres and some pelagic foraminifers. Coniacian. Komen limestone in Sežana Formation. Lipa at Komen 6 Korala Eugyra lanckoronensis aptijske starosti. Primerek je presedimentiran v zgornjekredno flišno brečo. Kanalski Lom na Banjšicah -zbirka D. Turnšek) Eugyra lanckoronensis coral of Aptian age, resedimented into Upper Cretaceous flysch breccia. Kanalski Lom on Banjšice plateau -D. Turnšek collection) Tabla 36 - Plate 36 Tabla 37 - Plate 37 Zgornja kreda - Upper Cretaceous Komenski apnenec - Komen limestone 1, 2 Laminiran mikritni apnenec, bogat z organsko snovjo. Laminated micritic limestone, rich in organic matter. 1 - Coniacij / Coniacian. Skopo pri Dutovljah / Skopo at Dutovlje 2 - Cenomanij / Cenomanian. Škrbina pri Komnu / Skrbina at Komen 3 Biomikritni apnenec - wackestone z miliolidami in drugimi foraminiferami (Pastrikella balcanica), bogat z organsko snovjo. Cenomanij. Tomačevica pri Komnu Biomicritic wackestone with miliolids and other foraminifers (Pastrikella balcanica), rich in organic matter. Cenomanian. Tomačevica at Komen 4 Laminiran biomikritni wackestone s foraminiferami in neskeletnimi algami. Cenomanij. Mali Dol pri Komnu Laminated biomicritic wackestone with foraminifers and nonskeletal algae. Cenomanian. Mali Dol at Komen 5, 6 Intramikritni apnenec -packstone s pigmentom organske snovi, algo Thaumatoporella parvovesi-culifera in foraminiferami. Coniacij Intramicritic packstone with organic matter, algae Thaumatoporella parvovesiculifera and fora-minifers. Coniacian 5 - Skopo pri Dutovljah / Skopo at Dutovlje 6 - Konjske stope pri Tomaju Tabla 37 - Plate 37 Tabla 38 - Plate 38 Zgornja kreda - Upper Cretaceous 1 Mikritni apnenec - wackestone z oogoniji haracej. Maastrichtij. Kozina Charophyta gyrogonites in micritic wackestone. Maastrichtian. Kozina 2 Izpran biomikritni apnenec - packstone s foraminiferami Rhapydionina liburnica, Dicyclina schlumbergeri in številnimi miliolidami. Maastrichtij. Vremski Britof Washed biomicritic packstone with foraminifers Rhapydionina liburnica, Dicyclina schlumbergeri and miliolids. Maastrichtian. Vremski Britof 3, 4 Rapidioninski apnenec - packstone s foraminiferami Rhapydionina liburnica (prečni in vzdolžni preseki). Maastrichtij. Foraminiferal packstone with transversal and longitudinal sections of Rhapydionina liburnica. Maastrichtian 3 - Tabor pri Štorjah / Tabor at Štorje ^ 4 - Senadole pri Štorjah / Senadole at Štorje 5 Mikritni apnenec s številnimi kalcitnimi prizmami in kolonijo Paronipora sp. (ex. Microcodium). Pedogeni karbonat z rizolitnimi tvorbami. Kredno/terciarna meja. Sopada pri Sežani Micritic limestone with numerous calcitic elements and a colony of Paronipora sp. (ex. Microcodium). Pedogenic carbonate with rhizoids. Cretaceous/Tertiary boundary. Sopada at Sežana 6 Intramikritni apnenec z večjimi izsušitvenimi porami, v katerih nastopa stalaktitični cement. Kredno/terciarna meja. Štorje pri Sežani Intramicritic limestone. Stalactitic calcite cement in some shrinkage pores. Cretaceous/Tertiary boundary. Štorje at Sežana Tabla 38 - Plate 38 Tabla 39 - Plate 39 Kreda - Cretaceous Globljemorski razvoj - Deeperwater environment 1 Spikulit - močno okremenjen mikritni packstone s številnimi spikulami spongij. Senon. Koritnica pri Bovcu Spiculite - silicified micritic packstone with numerous sponge spicules. Senonian. Koritnica at Bovec 2 Detajl vzorca s slike 1 Detail of sample from fig. 1 3, 4 Foraminiferni wackestone s številnimi globotrunkanami, drobirjem pelagičnih foraminifer in kal-cisferami. Senon Foraminiferal wackestone with numerous globotruncanas, pelagic foraminifers debris and calci-spheres. Senonian 3 - Koritnica pri Bovcu / Koritnica at Bovec 4 - Volčanski apnenec. Kolovrat nad Tolminom / Volče limestone. Kolovrat above Tolmin 5 Biokalkarenit z odlomki rudistnih lupin in ehinodermov, redka drobna zrna terigenega kremena. Bazalni del plasti Volčanskega apnenca. Senon. Drežnica pri Kobaridu Biocalcarenite, composed of rudist fragments, echinoderm plates and some terrigenous quartz grains. Basal part of Volče limestone beds. Senonian. Drežnica at Kobarid 6 Radiolarijski packstone - radiolarit. Albij. Bavšica pri Bovcu Radiolarian packstone - radiolarite. Albian. Bavšica at Bovec Tabla 39 - Plate 39 GEOLOGIJA 54/2 - dodatek / supplement, 2011 www.geologija-revija.si UVOD KRATEK PREGLED LITOLOGIJE IN RAZVOJA MEZOZOJSKIH KARBONATNIH KAMNIN SLOVENIJE ZGORNJI PERM TRIAS SPODNJI TRIAS SREDNJI TRIAS Anizij Ladinij ZGORNJI TRIAS Karnij Norij in retij Dinarska karbonatna plošča Slovenski bazen Julijska karbonatna plošča Vzhodne Alpe KREDA Dinarska karbonatna plošča Globljemorski razvoj Vzhodne Alpe MICROFACIES OF MESOZOIC CARBONATE ROCKS OF SLOVENIA LITERATURA - REFERENCES TABLE - PLATES Slike na naslovni strani - Cover photo: 1 - Zgornjekredni rapidioninski apnenec. Tabor pri Štanjelu 1 2 Upper Cretaceous Rhapydionina limestone. Tabor at Štanjel 34 2 - Spodnjejurski oosparitni grainstone. Trnovski gozd __l__l Lower Jurassic oosparitic grainstone. Trnovski gozd 3 - Poznodiagenetsko dolomitiziran spodnjekredni apnenec. Kočevski Rog Lower Cretaceous limestone dolomitized in late diagenesis. Kočevski Rog 4 - Srednjejurski apnenec z manganovimi gomolji. Bovec Middle Jurassic limestone with manganese nodules. Bovec ISSN 0016-7789 Geološki zavod Slovenije Geological Survey of Slovenia www.geo-zs.si 5 7 33 45 57 9770016778002