Mikrofacies Mezozojskih Karbonatnih Kamnin Slovenije

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

Geolo{ki zavod Slovenije, Dimi~eva ul. 14, SI-1000 Ljubljana; e-mail: bojan.ogorelec�geo-zs.si

Klju~ne 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 – ~arovnija, nam pri~ara morje plitvo, plažo, ocean globine.

Izvle~ek

Karbonatne kamnine mezozojske starosti so v Sloveniji precej raz{irjene, 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 razli~nih sedimentacijskih okoljih, zna~ilnih za karbonatne kamnine, tako v odprtih in zati{nih delih karbonatnega {elfa, lagunah in na obrežnih ravnicah, na razli~nih vrstah grebenov, pregibih in v bazenu. Ve~krat so karbonatno sedimentacijo spremljali tudi dotoki terigenega materiala in produkti vulkanskih aktivnosti. Med diagenetskimi procesi raziskanih karbonatnih kamnin imata najve~ji obseg dolomitizacija in okremenitev. V prispevku je predstavljenih 250 mikroskopskih posnetkov zna~ilnih apnencev in dolomitov s slovenskega prostora. V uvodnem delu, v katerem so za orientacijo dodani shematski litostratigrafski stolpci, je na kratko predstavljen geolo{ki 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. 4 Bojan OGORELEC

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 plo{~a ...... 21 Slovenski bazen ...... 25 Julijska karbonatna plo{~a ...... 25 Vzhodne Alpe ...... 26

KREDA ...... 26 Dinarska karbonatna plo{~a ...... 26 Globljemorski razvoj ...... 31 Vzhodne Alpe ...... 32

MICROFACIES OF MESOZOIC CARBONATE ROCKS OF SLOVENIA ...... 33

LITERATURA – REFERENCES ...... 45

TABLE – PLATES ...... 57 Mikrofacies mezozojskih karbonatnih kamnin Slovenije 5

Carbonate rocks are born ... (James N.P., 1979)

Ob 50. obletnici izida klasifikacije karbona- rov in cestnih usekov, v zadnjih letih pa tudi z tnih kamnin (Folk 1962, Dunham 1962, Ham (ed.) raziskavami za novo Formacijsko geolo{ko karto 1962). Slovenije v merilih 1 : 50.000 in 1 : 25.000. Teži{~e oziroma predmet predstavljene mo- UVOD nografije je, kot pove njen naslov, mikrofacies. Medtem, ko ima pojem facies že dolgo zgodovi- Karbonatne kamnine mezozojske starosti gra- no, odkar ga je sredi 19. stoletja, kot eno najbolj dijo okrog 40 % slovenskega ozemlja (Buser & pomembnih definicij v geologijo uvedel Gressly Komac, 2002). V tej, preko 5.000 metrov debeli (1838), pa je ime mikrofacies približno sto let skladovnici apnencev in dolomitov, ki jih le me- mlaj{e. Prvi ga je leta 1943 predlagal Brown za stoma prekinjajo klasti~ne sedimentne kamnine, tisti del kamnine, ki ga vidimo v preparatu pod vulkaniti in piroklastiti, zasledimo skoraj vse mikroskopom. Kasneje se je ta pojem med geo- facialne razvoje, zna~ilne tako za plitvomorska logi zakoreninil in mo~no raz{iril, {e posebno karbonatna okolja kot za globljemorska okolja. po svetovnem naftnem kongresu v Parizu leta Na majhnem prostoru je razvito celotno zapo- 1951, za kar je posebej zaslužen Cuvillier (1952, redje sedimentnih kamnin v stratigrafskem raz- 1962). Danes pojem mikrofacies opisuje združ- ponu od devona do kvartarja. Ta raznolikost je v bo vseh sedimentno-petrografskih in paleontolo precej{nji meri posledica dejstva, da je slovenski {kih zna~ilnosti v obmo~ju mikroskopskega me- prostor sti~i{~e treh velikih geotektonskih enot – rila preparata. Vezan je predvsem na karbonatne Alp, Dinaridov in Panonskega bazena. Intenzivna kamnine – apnence in dolomite. tektonska dogajanja, dviganje in spu{~anje tere- Kasneje so k poznavanju mikrofaciesa v sve- na, so povzro~ila, da se lahko ob {tevilnih prelo- tu najve~ prispevali Carozzi (1960, 1989), Folk mih in narivih stikajo razli~ni razvoji posameznih (1962) in Dunham (1962), slednja s klasifikacija- formacij, isto~asno pa s tem ve~krat niso opazni ma karbonatnih kamnin, Ham (1962) in Bathurst bo~ni prehodi med razli~nimi okolji sedimentaci- (1971), posebno pa Flügel (1978, 1982, 2004), je. V vsakem pogledu je na{e ozemlje lahko »mala ki je sistemati~no zbral vse dotedanje vedenje o zbirka« razvojev mezozojskih karbonatnih kam mikrofaciesu in raziskovalnih metodah ter pred- nin na prostoru nekdanje zahodne Tetide. stavil nove, poglede na prakti~en pomen mikro- ^eprav iz naslova publikacije ni razvidno, facialnih raziskav karbonatnih kamnin. Knjiga zbrano gradivo presega okvire mezozoika, saj so Microfacies of Carbonate Rocks (Flügel, 2004) je vklju~eni tudi zgornjepermski apnenci in dolomi- bogato dokumentirana s fotografijami zna~ilnih ti. Ti so v objavo zajeti zato, ker se z njimi pri~enja fosilov pod mikroskopom. Nekaj predstavljenih zvezna karbonatna sedimentacija na enoviti Slo- vzorcev v teh publikaciji izvira tudi iz slovenske- venski plo{~i, ki je obstajala od zgornjega perma ga prostora. Wilson (1975) je na osnovi Flüglovih do sredine anizija (Buser, 1989). idej (1972) izdelal in v prakso uvedel pojem stan- K pripravi monografije je avtorja vodila želja dardni mikrofacies (SMF – Standard Microfacies po predstavitvi rezultatov mikrofacialnih analiz Type), ki sloni na 24 osnovnih vrstah mikrofaciesa ve~ desetletnih raziskav apnencev in dolomitov ter devetih zna~ilnih okoljih nastanka karbonat slovenskega ozemlja. Te raziskave so v prvih le- nih kamnin. Poseben odmev je Wilsonova klasifi- tih potekale predvsem v sklopu izdelave Osnovne kacija mikrofaciesa doživela v naftni geologiji in geolo{ke karte SFRJ v merilu 1 : 100.000, ki je bila v ra~unalni{ki informatiki sedimentnih kamnin. zaklju~ena leta 1989, nadalje projekta Mezozoik S sedimentacijskimi okolji in modeli karbonatnih v Sloveniji, v zadnjem ~asu pa preko geolo{kih kamnin so se v zadnjem obdobju poleg omenjenih projektov v okviru nacionalnega raziskovalnega avtorjev intenzivno ukvarjali {e Milliman (1974), programa Javne agencije za raziskovalno dejav- Reading (1978), James (1979), Scholle s sodelavci nost Republike Slovenije. Precej podatkov je bilo (1983), Tucker & Wright (1990), Bosellini (1991), zbranih tudi pri raznih aplikativnih raziskavah, James & Kendall (1992), Einsele (1992) ter drugi kot so raziskave rudi{~ živega srebra v Idriji ter (npr. Elf-Aquitaine 1975; AGIP 1988). svinca in cinka v Mežici, nadalje iz globokih geo V Sloveniji se je pojem mikrofacies pojavil že termalnih in naftnih vrtin, kamnolomov, predo- dokaj zgodaj, saj ga že leta 1961 omenjata E. Flü- 6 Bojan OGORELEC

gel in A. Ramov{ pri opisu zgornjetriasnega dach gresa (Drobne,1979). Celovit in zgo{~en prikaz steinskega apnenca z Begunj{~ice. Poudarek v biostratigrafije in litologije zgornjepermskih in tem ~lanku je na opisu fosilne flore in favne ter mezozojskih kamnin je prikazan v Geologiji Slo- na primerjavi z ustreznim apnencem v Severnih venije (Pleni~ar, M., Ogorelec, B. & Novak, M., Alpah. Na žalost ta objava ni dokumentirana s ur., 2009) in sicer v poglavjih, ki zajemajo zgor- slikami. nji perm (Skaberne et al., 2009), trias (Dozet & Leta 1966 je Rajka Radoi~i} izdala za tisti ~as, Buser, 2009), juro (Buser & Dozet, 2009) ter kre- izvrsten in bogato ilustriran ter obsežen prispe- do (Pleni~ar, 2009). Pregleden prikaz geolo{kih vek o mikrofaciesu jurskih plasti v Dinaridih, ki razvojev po geotektonskih enotah je zajet v delih zajema tudi opise in slike ve~ vzorcev apnencev iz S. Buserja (1979a), P. Mio~a (2003) in U. Premruja južne Slovenije. (2005). Ko govorimo o faciesu karbonatnih kam Po tem za~etku je pri {tudiju mikrofaciesa nin, moramo omeniti tudi pregledne prispevke o karbonatnih kamnin v Sloveniji pri{lo do deset njihovih facialnih razvojih (Pleni~ar & Pavlovec, letnega zati{ja. Apnenci so bili takrat predmet 1984), o njihovih facialnih zna~ilnostih (Pleni~ar predvsem paleontolo{kih analiz in stratigraf- & Premru, 1975), kamninah kot možnih mati~nih skih dolo~itev v okviru Osnovne geolo{ke karte plasteh za nastanek ogljikovodikov (Ogorelec et (OGK). Mo~an zagon sedimentologiji in pri tem al., 1996) ter o njihovi izotopski sestavi (Ogorelec tudi mikrofacialnim raziskavam predstavlja ob- et al., 1999b). dobje po letu 1973, ko je zaživel projekt Mezozoik Osnovna namena publikacije sta dva. V prvi v Sloveniji. V okviru le-tega je pri{lo do celovitih vrsti je ta namenjena {tudentom geologije, ki se raziskav triasnih, jurskih in krednih formacij s prvi~ sre~ujejo s pojmom mikrofacies ter tujim teži{~em na apnencih in dolomitih. Tovrstne razi raziskovalcem zaradi spoznavanja na{ih karbo- skave so se sicer s formalno druga~nimi naslovi v natnih kamnin in njihove primerjave s sosednji- okviru raznih projektov nadaljevale, tako da se je mi ozemlji. Koristna pa bo lahko tudi drugim, saj na Geolo{kem zavodu Slovenije v dvajsetih letih mikrofacies v mnogo~em povezuje sedimentologe zbralo in preiskalo preko 25.000 mikroskopskih s paleontologi, regionalnimi geologi in tektoniki. preparatov. Njihov izbor predstavlja potrebno Zaradi bolj{e preglednosti gradiva je v uvodnem osnovo in material za pri~ujo~o publikacijo. delu podan zgo{~en litolo{ki opis celotne skla- V zbranem gradivu je prikazan le mikrofa- dovnice mezozojskih in zgornjepermskih kamnin cies, ki ga prepoznamo v zbruskih apnencev in v Sloveniji. dolomitov slovenskega prostora. Makrofosili ter Gradivo je vsebinsko razdeljeno po geolo{kih izolirana mikroflora in mikrofavna (npr. radio- obdobjih, pri ~emer je teži{~e publikacije slikov- lariji, konodonti, nanoplankton, pelodi in dru- no gradivo z 250 fotografijami mikroskopskih go) zato niso zajeti v slikovnem materialu, zelo preparatov. Uvodni tekst, dopolnjen z nekateri- skromno pa tudi v literaturi. Ve~ina ~lankov in mi litolo{kimi stolpci ter literaturo, predstavlja publikacij, ki so bile natisnjene v {estdesetih in le potrebno ogrodje, da kamnine postavimo v ~as sedemdesetih letih prej{njega stoletja, obravna- in prostor. Tuja literatura je zelo okrnjena, citira- va litologijo, paleontologijo, regionalni razvoj ali na samo zaradi primerjave karbonatnih kamnin stratigrafijo mezozojskih karbonatnih kamnin na slovenskega s sosednjima, alpskim in dinarskim slovenskem. Posebej to velja za tolma~e k posa- prostorom. meznim listom OGK 1 : 100.000. Ve~ sedimento- Glede na to, da prihaja do tiska pri~ujo~e logije je zajete v tolma~ih k novej{im geolo{kim publikacije prav ob 50. obletnici za karbonatno kartam, meril 1 : 50.000 (Jurkov{ek et al., 1996) sedimentologijo pomembnega dogodka, namre~ ali 1 : 25.000 (Jurkov{ek, 2010; ^ar, 2010), del- izida enega temeljnih del petrografije apnencev no tudi v publikaciji Geological development in in dolomitov – Klasifikacije karbonatnih kamnin Slovenia and Croatia – Guidebook, ki je iz{la ob (Ham, 1962), se avtor na ta na~in pridružuje pra- priliki 16. evropskega mikropaleontolo{kega kon- znovanju tega jubileja. Mikrofacies mezozojskih karbonatnih kamnin Slovenije 7

Narava vedno eno iz drugega ustvarja in ni~ ne nastane prej, predno drugo ne preide. (Titus Lucretius Caro (99–55 pn{. – »De rerum natura«)

KRATEK PREGLED LITOLOGIJE IN RAZVOJA MEZOZOJSKIH KARBONATNIH KAMNIN SLOVENIJE

Po odložitvi kopenskih klasti~nih kamnin, je prostor Slovenije v zgornjem permu zajela obse- žna transgresija morja in za~ela se je sedimentacija karbonatnih kamnin. Ozemlje je bilo vse od zgornjega perma do sredine anizija sestavni del enotne, plitve karbonatne plo{~e, poznane kot Slovenska plo{~a (Buser, 1989), ki se je razteza- la {e v Furlanijo, Istro in na prostor Panonske- ga bazena. V aniziju je ta plo{~a razpadla in se razdelila na Dinarsko karbonatno plo{~o na jugu in Julijsko karbonatno plo{~o na severu, lo~il pa ju je Slovenski bazen (Cousin, 1973; Buser, 1989). Karbonatna sedimentacija se je v ve~jem ali manj{em obsegu na obeh plo{~ah nadaljevala vse do zgornje krede, ko je pri{lo do razpada Skladi Dachsteinskega apnenca na Kaninu Dinarske karbonatne platforme in nastanka ve~ Dachstein limestone on Mt. Kanin vmesnih fli{nih bazenov. Na sliki 2 je prikazan litolo{ki razvoj zgornje- V zadnjem ~asu se kot približni sinonim za permskih in mezozojskih karbonatnih kamnin v Dinarsko karbonatno plo{~o uporabljajo izra- posameznih paleogeografskih enotah – na Dinar- zi Karbonatna platforma zunanjih Dinaridov ski in Julijski karbonatni plo{~i, v Slovenskem (Grandi} et al., 1999), Jadransko-Dinarska karbo- bazenu ter posebej v Severnih Karavankah, ki natna platforma (Gu{i} & Jelaska, 1993) ali eno- ležijo severno od Periadriatskega lineamenta. stavno Jadranska karbonatna platforma (Gu{i} Na sliki 3 so shematsko predstavljena njihova & Jelaska, 1990, Veli} et al., 2002; Vlahovi} et sedimentacijska okolja. Zaradi mo~ne tektoni- al., 2005; Jež, 2011), glede na to, da je bila to ke in z njo povezane narivne zgradbe slovenske- najve~ja karbonatna plo{~a na Jadranski mi ga ozemlja, so lahko odnosi med posameznimi kroplo{~i v obdobjih jure in krede. V pri~ujo~i litolo{kimi enotami in geolo{kimi formacijami monografiji {e vedno uporabljam »star« izraz Di- prikazani le shematsko. narska karbonatna plo{~a.

Sl. 1. Pregledna in poenostavljena geolo{ka karta Slovenije (priredil M. Pleni~ar) Fig. 1. Simplified overview geological map of Slovenia (adapted by M. Pleni~ar) 8 Bojan OGORELEC

Sl. 2. Shematski prikaz razvoja zgornjepermskih in mezozojskih plasti v razli~nih paleogeografskih enotah Slovenije. Apnen~ev in dolomitni razvoj sta nazna~ena z barvami (po podatkih Osnovne geolo{ke karte 1 : 100.000 (ve~ji 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). Mikrofacies mezozojskih karbonatnih kamnin Slovenije 9

Sl. 3. Sedimentacijska okolja zgornjepermskih in mezozojskih karbonatnih kamnin v Sloveniji Fig. 3. Sedimentary environments of Upper Permian and Mesozoic carbonate rocks in Slovenia 10 Bojan OGORELEC

V nadaljevanju slede zelo zgo{~eni opisi lito- doarmenskega tipa. Za zaprti {elf in lagune so logije po posameznih geolo{kih obdobjih s pou- zna~ilni razli~ki algnega biomikritnega apnenca darkom na karbonatnih formacijah in njihovih tipa packstone, za sabke pa satasti dolomiti in mikrofacialnih ter diagenetskih zna~ilnostih. evaporitni minerali, od katerih sta zastopana sa- Glede na to, da so triasne plasti v Sloveniji naj- dra in anhidrit. bolj raz{irjene ter isto~asno tudi najbolj pestro V biomikritnem apnencu so prisotne forami- razvite, jim je v monografiji namenjenega najve~ nifere (Agathamina sp., Glomospira sp., Hemi- prostora. gordius sp., Reichelina sp., Climacammina sp., Geinitzina sp., Ammovertella sp., Ichtyolaria sp., Staffella sp.), skeletne alge Gymnocodium ZGORNJI PERM bellerophontis, Vermiporella nipponica, Permo- calculus fragilis, Velebitella triplicata, Mizzia ve- Zgornjepermske plasti so v Sloveniji zastopa- lebitana, M. cornuta), brahiopidi, ehinodermi in ne s karbonatnimi kamninami. Litolo{ko so pre- polži (Bellerophon sp.), lokalno pa se pojavljajo cej pestro razvite. V zahodnem delu Posavskih {e manj{e kopu~e koral vrste Waagenophyllum gub – med Ljubljano, Škofjo Loko in Idrijo do- indicum (Ramov{, 1958, 1986a; Buser et al., 1988; sežejo debelino do 250 metrov. Tod prevladujeta Skaberne et al., 2009). plastovit, temno siv do ~rn apnenec in laporast Permsko-triasna (P/T) meja je zaznamovana apnenec nad dolomitom, vmes pa se ve~krat po- z nenadnim izginotjem {tevilnih fosilnih vrst, javljajo tanke pole skrilavega laporovca. Po kraju predvsem alg in foraminifer ter s spremembo Žažar pri Vrhniki so poimenovane kot Žažarska izotopske sestave ogljika v apnencih in dolomi- formacija (Ramov{, 1958), ki je ekvivalent Belero- tih. Spodnjetriasni karbonati so obogateni z do fonski formaciji v Alpah (Heritsch, 1934; Buser et 5 ‰ lažjim izotopom ogljika kot zgornjepermski (Dolenec T. et al., 1995, 1999a,b,c, 2004). Tik pod P/T mejo se ponekod pojavlja tanj{a 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). Paleontolo{ko je bila P/T meja v Sloveniji v zadnjih letih dokazana na osnovi konodontne cona- cije (Kolar-Jurkov{ek & Jurkov{ek, 2007; Kolar- -Jurkov{ek et al., 2011) in foraminifer (Nestell et al., 2011). Takoj nad permsko/triasno mejo je zna~ilna drobna foraminifera Earlandia. Med diagenetskimi procesi, ki so zajeli zgornjepermske karbonatne kamnine, ima dale~ naj ve~ji obseg dolomitizacija, v manj{i meri pa sta prisotni {e okremenitev in dedolomitizacija. Ob dedolomitizaciji je pri{lo v plasteh z evaporitnimi minerali do izlo~anja epsomita, kar je lepo vidno v idrijskem rudniku živega srebra. Zna~ilni mikrofacies algnega apnenca Žažarske formacije. Zgornji perm. Dolina Idrijce pri Masorah. Merilo 1 mm Pretežni del dolomita je zgodnjediagenetske- ga zna~aja in je nastal po evaporitnem modelu Characteristic algal limestone facies of Žažar Formation. Up- per Permian. Idrijca valley at Masore. Scale 1 mm dolomitizacije (Shinn & Ginsburg, 1964). Na ari- dno klimo v zgornjem permu kažejo poleg sadre 18 al., 1988; Kolar-Jurkov{ek et al., 2011). V vzhod in ahidrita tudi izotopske analize δ O (Pol{ak & nem delu Posavskih gub, pri La{kem, Izlakah, Pezdi~, 1978; Dolenec T. et al., 1981; Ogorelec et Sevnici in na Bohorju so zgornjepermske pla- al., 1999b) ter visoke vsebnosti Na+ za karbonate sti debele le do nekaj deset metrov in so razvite (Ogorelec & Rothe, 1979). pretežno dolomitno. V bazalnih plasteh, tik nad Obdobje zgornjega perma je bilo zaradi spe klastiti Grödenske formacije, vsebujeta apnenec cifi~nih sedimentacijskih razmer in klime ugodno in dolomit {e precej terigene primesi kremena in za nastanek stratiformnih rudi{~ svinca in cinka. sljude. Apnenec je v splo{nem izredno bogat s fo- Taka nahajali{~a so pogosta v vzhodnih Posavskih sili, predvsem s skeletnimi algami, ehinodermi in gubah in sicer v vrhnjem delu zgornjepermskega foraminiferami. Delež karbonata v apnencu se gi- zaporedja (Puharje pri Šo{tanju, Iskra, 1969) ter blje med 85 in 97 %. na meji med zgornjim permom in spodnjim tria- V Južnih Karavankah je zgornjepermsko zapo- som (Mokronog, Bohor, Ledina pri Sevnici, Dro- redje razvito dolomitno, kot Karavan{ka formaci- venik et al., 1980). ja, ki je debela do 300 metrov (Buser et al., 1988). Zgornjepermske plasti slovenskega prostora Za spodnji del te formacije je zna~ilen do 80 m imajo v splo{nem enak ali zelo podoben mikrofa- debel paket satastega dolomita (Rauhwacke). cies kot ga kažejo apnenci in dolomiti iste starosti Sedimentacijsko okoje zgornjepermskih pla- na sosednjih ozemljih – npr. v Karnijskih Alpah sti je bil zelo plitev in zaprt {elf z lagunami in (Buggisch, 1974; Buggisch et al., 1976; Holser & sabkami, ki je imel povezavo s {ir{im prostorom Schönlaub, 1991; Magaritz & Holser, 1991; Noé, Tetide. Na to kaže univerzalna flora in favna in- 1987), v Dolomitih (Bosellini & Hardie, 1973), na Mikrofacies mezozojskih karbonatnih kamnin Slovenije 11

Sl. 4. Litolo{ki stolpci zgornjepermskih plasti v Sloveniji (Buser et al.,1988) Fig. 4. Lithological columns of Upper Permian beds in Slovenia (Buser et al., 1988)

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 raz{irjene, saj zavzemajo skoraj eno ~etrti- no njenega ozemlja in skupno debelino celo do 3800 metrov (Buser, 1979), pri ~emer karbonatne kamnine mo~no prevladujejo nad klasti~nimi in piroklasti~nimi razli~ki (sl. 2). Kažejo izredno pestro litologijo z zna~ilnostmi alpskega razvoja znotraj Tetide, podobnega ali enakega tistemu v Severnih Alpah. V spodnjem triasu je karbonatno sedimentacijo na plitvem {elfu spremljal dotok terigenega, ve~ji del drobnozrnatega materiala s kopnega, v spodnjem aniziju pa so karbonati povsem prevla- dovali. Koncem anizija (Buser, 1989), na Idrij- skem pa že v srednjem aniziju (^ar, 1985, 2010), se je pri~ela Slovenska karbonatna plo{~a 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 raz{iril {e na ozemlje Julijske karbonatne plo{~e, proti Dinarski karbonatni plo{~i pa je obstajal vse do Sl. 5. Litologija in izotopska sestava karbonatnega ogljika na konca krede. permsko-triasni meji v profilu Masore pri Idriji. Opazen je iz- 13 Podrobnej{i opisi paleogeografskega razvoja razit padec δ C na meji (Dolenec, T. et al., 2004) Fig. 5. Lithology and stable isotope composition of carbonate triasa na celotnem prostoru Slovenije, paleotek- carbon across the Permian-Triassic boundary in the Masore tonike in biostratigrafske raz~lenitve so podani section at Idrija (Dolenec, T. et al., 2004) predvsem v delih: Buser, 1979, 1980b, 1988, 1996; 12 Bojan OGORELEC

Sl. 6. Dana{nji položaj geotektonskih enot v zahodni in osrednji Sloveniji in raz{irjenost sedimentov nekdanje Jadranske in Dinarske karbonatne plo{~e 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 obliko- van tak paleogeografski prostor na Slovenskem v ~asu triasa imamo na Bahamskem oto~ju (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 litolo{kega razvoja triasnih kamnin v Sloveniji z izbranimi strati- grafskimi stolpci.

SPODNJI TRIAS (induanij in olenekij)

Debelina spodnjetriasnega zaporedja je dokaj razli~na. Giblje se med 40 in 500 metri, v Južnih Karavankah pa doseže tudi do 600 metrov (Bu- ser, 1980a). Plasti so na celotnem slovenskem prostoru južno od Periadriatskega lineamenta precej enotno razvite. V spodnjem delu zapore dja, ki je debelo do 250 metrov, se menjavajo klastiti in karbonati, posebej pa na terenu izstopajo oolitne plasti. Dolomit in apnenec spodnjega dela spodnjega triasa, imata zaradi primesi terigenega kremena in sljude pe{~en izgled. Nekarbonatni Sl. 7. Bahamski {elf z osrednjim globokim jarkom, oceanskim delež mestoma doseže tudi 50 %. Klastite sestav jezikom (Tongue of the Ocean – TOC). Dimenzije tega jarka la- ljajo rde~kasti glinavci, laporovci in meljevci. hko primerjamo s Slovenskim bazenom, ki je v ~asu od anizija Apnenec je po sturkturi najve~krat biomikrit ali do zgornje krede potekal preko osrednje Slovenije (http:// pelmikrit. Odlagal se je v zelo plitvem, zati{nem www.keysdisease.blogspot.com/) delu {elfa, ki je imel ob~asno zna~ilnosti lagun in Fig. 7. Bahama shelf with the central Tongue of the Ocean trough (TOC). Its size is comparable to the Slovenian basin litorala. Ve~krat je popolnoma ali delno dolomi- which existed in the central part of Slovenia from Anisian to tiziran, zna~ilne zanj pa so tudi bioturbacijske Upper Cretaceous (http://www.keysdisease.blogspot.com/) teksturne oblike. Tanj{e le~e ter gnezda sadre in Mikrofacies mezozojskih karbonatnih kamnin Slovenije 13

Spodnjetriasni oolitni dolomit. Hematitni pigment je obarval ooide rde~kasto. 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 vi{ja. Zna~ilna zanje je rde~kasta barva, kot posledica hema titnega pigmenta. Jedra ooidov je ve~krat zajela kasnodiagentska dolomitizacija, ki se kaže v do 300 μm velikih dolomitnih romboedrih. Med ooidi so pogosto pome{ane plo{~ice ehinodermov ter drobne hi{ice polžev, opisanih kot vrsti Natica gregaria in Holopella gracilior, ve~krat pa so prisotne tudi drobna zrna kremena in sljude. V vrhnjem delu spodnjetriasnega zaporedja se delež terigene komponente zmanj{uje. Prevladu- je temnej{i biomikritni ali pelmikritni laporasti apnenec (mudstone do packstone) nad svetlej{im dolomitom. Med fosili so zastopane foraminifere, v nekaterih plasteh so {tevilni ostrakodi, plo{~ice ehinodermov in drobne {koljke, prisotni pa so tudi konodonti (Kolar-Jurkov{ek & Jurkov{ek, 1995, 1996, 2007). Za stratigrafijo tega dela spod njetriasnih plasti, je med foraminiferami najbolj pomembna Meandrospira pusilla. Severno od Periadriatskega lineamenta, posebno v okolici ^rne na Koro{kem, so spodnje triasne plasti razvite pretežno klasti~no, glede na to, da pripada prostor Severnih Karavank vzhod noalpskemu geotektonskemu bloku. Razvite so kot pe{~enjaki, skrilavi meljevci in konglomerati tipa »Buntsandstein« (Mio~, 1983) in so brez fosilnih ostankov (Štrucl, 1971). Spodnjetriasne plasti slovenskega prostora kažejo v velikem delu enak ali zelo podoben mi- Sl. 9. Shematski stolpec zgornjepermskih in spodnjetriasnih krofacies, kot ga imajo kamnine iste starosti na plasti na Žirovskem (Ogorelec & Grad, 1986) sosednjih ozemljih – npr. Werfenske plasti v Se- Fig. 9. Schematic column of Upper Permian and Lower Trias- vernih Alpah (Mostler & Rössner, 1984), v Kar- sic beds of Žiri area (Ogorelec & Grad, 1986) nijskih Alpah (Holser & Schönlaub, 1991), v Do- lomitih (Assereto et al., 1972), na Madžarskem (Nagy, 1968; Haas, 2001), na avstrijskem delu Juž- anhidrita kažejo na lokalne in ob~asne evaporit nih Karavank (Anderle, 1970), na Svilaji v dal- ne pogoje sedimentacije. Na idrijsko-žirovskem matinski Zagori (Š~avni~ar et al., 1983; Jelaska et ozemlju je v najvi{jem delu spodnjetriasnega za- al., 2003) in drugod, kar kaže na zares obsežno in poredja razvit t.i. pasnati apnenec (Mlakar, 1969; enotno sedimentacijsko okolje v ~asu spodnjega Kolar-Jurkov{ek et al.; 2011). triasa. 14 Bojan OGORELEC Mikrofacies mezozojskih karbonatnih kamnin Slovenije 15

. , - { T SREDNJI TRIAS , ari ov b m a , 2008; , 2008; , 2002), , 2002), , 1987), , 1987), , 2001), , 2001), , 1979), , 1979), R { Anizij – Trži~ - - – Trži~ ar olenec enow 8 ov & S D ovak m - ed., 2011), 2011), ed., - Anizijske plasti so v Sloveniji razvite precej a et al., 1984), et al., 1984), el orelec – Trnovski 53 – Trnovski N & ^ & g g R – Šmarjetna – Šmarjetna 49 ilvester enotno, ve~ji del kot plastovit dolomit, ki kaže O uc S lü 1969),

m oljak F pogoste znake medplimske sedimentacije s stro- Š P & {,1998, orelec & 1989), g

, matoliti in izsu{itvenimi porami (Grad & Ogore- ov skra O I m user ozet , 1990b), , a lec, 1980; Dolenec et al., 1981). Apnenec je raz- B othe R D – Belca v et al., 1984), 42 – Belca v

R vit v manj{em obsegu kot biomikrit. Med fosili ozet ek . &. { D & prevladujejo foraminifere (Meandrospira dinari- T ,

– Mokrice ( Mokrice – 11 ca, Pilammina densa, Glomospirella irregularis, urkov

60 – Begunj{~ica ( G. grandis, G. semiplana, Trochammina sp.), me- J orelec – Todraž pri Gorenji pri Gorenji 1970, 1971), 25 – Todraž , 56 – Kobla ( ), g olenec al. 1981), 38 – Hudajužna ( stoma so prisotne tudi alge (Physoporella pau- O 33 – Idrija - Cerkno ( D

( et ), ciforata). V severnem delu Julijskih Alp je med trucl M. 2004), M. – Puharje - Šo{tanj ( ar – To{ko ~elo ( et al., 1998), 21 – To{ko , Š Mojstrano in Kranjsko Goro ohranjen masiven 7 ^ 1988; , 1997), ek , { , 2002 , grebenski apnenec, ki ga gradijo predvsem alge }, 1980/81 – Tamar ( et al., 1984), 45 – Tamar et al., 1993), 28 – Kranjska Gora ( i b ozet in trombolitne tvorbe (Ramov{, 1987). Enak raz olenec ole el a 2002), D g

B D B , urkov orelec voj kaže tudi grajska stena nad Blejskim jezerom J lü g & orelec F

O lügel g (F et al., 1993). ozet – Ko~evje ( Ko~evje – al., 2002), 48 et , 1975) O – Spodnja Idrija Spodnja – 37 – Cerkno ( D Debelina anizijskih plasti doseže do 600 met ek ar 2000), 16 – Rajndol pri Ko~evju ( { , b ), orelec – Vr{i~ ( et al., 1987), 41 – Vr{i~ &

ri rov. g Š ek ar O ozet { { urkov m D , 1978 . et al., 1999b , al., et . J e ~ & T urn D , io T ale , 1984), 32 – Peca ( g M i et al., 1999a), 24 – Mežica ( C , 1997;, , T. et al., 2004), 4 et al., , T. olenec trucl ek 1970; Š { D

59 – Batognica pri Krnu ( , orelec ), g – Borovnica - Bistra ( 52 – Borovnica 27 – Bled - grad (castle) ( ek O b olenec ), ), e urkov D J R – Vi{nja Gora ( 15 – Vi{nja - , 1996 55 – Laze pri Sevnici ( ,2009 { & ,2003 – Zadnja Smoleva ( olar user ov . et al., 1998, al., et . 1995), K T m

ozet , – Log pod Mangartom ( ., 1983), 44 – Log pod Mangartom a }, i & u D orelec R & B ~ , 1989), L et al., 1988, g

ek 36 – Idrija - ^ekovnik ( , ni & O { , 1980), 6 A ), ar olenec ar othe b { user orelec R D m ri B g et al., 2003), 31 – Mežica ( { & e

urkov Š O – Tehovec pri Polhovem Gradcu ( et al., 1980), 20 – Tehovec J orelec & , 1994 D ov 2010), 40 – Perbla pri Zatolminu ( g , m ar ek O { & a erne ar ^ { b R

ov Meandrospira dinarica v stromatolitnem dolomitu z izsu {it & orelec m ka , 1978, , a g venimi porami. Anizij. Zakamnik nad karavan{kim cestnim – Masore ( – Masore S rad ek R urkov O {

J predorom. Merilo 1 mm G

, 1969; ^ Meandrospira dinarica in stromatolitic dolomite with shrinkage pores. Anisian stage. Zakamnik above Karavanke high- urkov 1958), 3 J lakar , 1984.), 58 – Krn ( way tunnel. Scale 1 mm {, M ov et al., 2007), 62 – Ur{lja gora ( m a 35a – Rovte ( – Karavanke - cestni predor (road tunnel) ( (road 23 – Karavanke - cestni predor rne – Brsnina pri Jelendolu ( Brsnina pri Jelendolu – 10 Severno od Periadriatskega lineamenta izda- orelec R ), ), ^ g

, 1978), 26a – Križna gora ( nja v Topli pod Peco plastovit dolomit, ki je oru- O 14 – Mi{ji Dol - La{ko ( den s svin~evimi in cinkovimi minerali (Štrucl, – Preserje pri Borovnici ( pri Borovnici al., 1977), 51 – Preserje , 1990 , 1980 19 – Idrija - rudnik (mine) ( 1974). Nad njim leži temen mikritni apnenec z ), orelec et – Žažar ( – g 1979), 2

elen gomolji roženca. , 1988), 30 – Kamna Gorica ( ru et al., 2005), 43 – Menina ( O , J 39 – Zg. Idrijca ( et al., 1988), al., et m orelec – Javorjev dol - Sovodenj ( et al., 1990;

ek Sredi anizija je Slovenska plo{~a pri~ela raz- g 5 { re ~, 1992 ek O i P {

user padati. Tako se je sedimentacija od srednjega { artnik orelec u B g 1982), &

g triasa dalje odvijala na treh geotektonskih enotah M urkov 2001), O un

J , rad urkov – Helenski potok pod Peco ( Peco pod potok – Helenski 47 - v razli~nih okoljih. Na {ir{em Idrijskem je pri{lo J et al., 1988), et G

& P & do lokalnih okopnitev in nastanka debelej{ih et al., – Dolenja Trebu{a - êpovan ( 1989), 54 – Dolenja Trebu{a , olar user ek konglomeratnih in pe{~enih plasti (âr & âdež, orelec K { B g othe – Ko{utnik ( – 1977; âr, 2010). Za globlji razvoj anizija, ka O 9 R urn al., 1982), al., rovenik

T kr{nega poznamo v Karavankah pri Trži~u, na D 1987; et & , Idrijskem in v vzhodnih Posavskih gubah, so zna – Lesno Brdo ( , 1979), 35 – Lesno Brdo ,M. & ek 1981), { olar urkov ek

– Dolenjske Toplice ( 50 – Dolenjske Toplice ~ilni amoniti in konodonti (K -J { , , 1991), 13 – Bohor ( , 1979; , 1974,, ozet artnik et al. 2008, 2009), 57 – Kobari{ki Stol ( ), 1999), 18 – Želimlje ( orelec } , i

~ 1983, 1991). g g D er ~ f olenec urkov O , 1978), 26 – Kisovec pri Zagorju ( et al., et un – Mangart ( , 1997), 61 – Mangart ni oži J D ozet P trucl R A , ,1979 chä ek Š , D { a S Ladinij orelec olenec olar urn & g T D K , 2008

O Ladinijske plasti so litolo{ko med najbolj pi- .,1999 ~ sanimi, saj se hitro menjavajo razli~ni litolo{ki aryan oži – Rejc - Vojskarska planota ( Vojskarska Rejc - – 12 – Orlica ( 22 – Dednik pri Polhovem Gradcu ( – Borovnica ( 34 – Borovnica – Topla ( 29 – Topla – Mežica ( 46 Lom ( Lom Sl. 8. Shematski prikaz litolo{kega razvoja zgornjepermskih in triasnih karbonatnih kamnin v Sloveniji, s stolpci objekti, k i so zajeti tem delu. in this work. in Slovenia with columns and objects, presented carbonate rocks of lithostratigraphic development Upper Permian and Triassic Fig. 8. Schematic presentation 1 et al D Karavankah ( 1961, R gora ( vasi ( gozd - Lokve ( 17 - Ple{e ( tipi. Izdanjajo na ve~ krajih v osrednji Sloveniji, 16 Bojan OGORELEC

Sl. 10. Poenostavljen prikaz paleogeografskega razvoja v Sloveniji v obdobju med anizijem in koncem triasa s položajem koralno-spongijskih grebenov (Turn{ek 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 (Turn{ek et al., 1984)

na {ir{em Idrijskem in Cerkljanskem, v predgorju (Gori~an, 1997; Gori~an & Buser, 1990; Skaberne Julijskih Alp in v Karavankah, v ve~jem obsegu et al., 2003). Med makrofosili so pomembni amo- pa severno od Periadriatskega lineamenta, pred- niti in {koljke (Jurkov{ek, 1983, 1984; Ramov{ & vsem na pogorju Pece. Jurkov{ek, 1983; Ramov{, 1989). V piroklastitih Rezultat intenzivne tektonike v ~asu idrijske najdemo na Idrijskem tudi manj{e grebenske kope tektonske faze (Buser, 1980b) je mo~na razko (âr, 2010). sanost ozemlja v osrednji Sloveniji. V globljih V Kamni{ko-Savinjskih Alpah je iz zgornjega jarkih je pri{lo do vulkanskih izlivov spilitno-ke- ladinija zanimiva Koro{i{ka formacija. Leži nad ratofirske asociacije (bazalti, kremenovi kerato- zrnatim dolomitom in zelenim tufom. Apnenec firji, porfir,…) ter sedimentacije njihovih tufov in je rahlo bituminozen, ~rn biomikrit z gomolji ro- tufitov (Buser, 1979; Dozet & Buser, 2009). Ne- ženca. Med fosili so prisotne {koljke (Jurkov{ek, kateri tektonski bloki so okopneli, na kar kaže- 1984), amoniti in skeleti rib ter plazilcev (Celarc, jo debele plasti pobo~nih bre~ in konglomeratov. 2004a; Celarc & Žalohar, 2010). V Južnih Karavankah in v delu Julijskih Alp je to V Severnih Karavankah je na obmo~ju Me- Ugovi{ka bre~a (Buser, 1986b; Jurkov{ek, 1987), žice obstajal v ~asu ladinija in cordevola preko na Idrijskem pa konglomerat med Idrijo in Rov- 1000 metrov debel kompleks masivnega, me- tami ter Stopni{ki konglomerat (Mlakar, 1969; stoma plastovitega apnenca in dolomita, zna- âr & âdež, 1977; âr & Skaberne, 2003; âr, nega kot Wettersteinski apnenec (Štrucl, 1970, 2010). Na Dinarski in Julijski karbonatni plo{~i 1971). Najbolj zna~ilen tak masiv je pogorje Pece. so se zaradi ob~asne povezave z bazenom lokal- Apnenec je oruden s cinkovo in svin~evo rudo no odlagali temni apnenci z roženci in vmesni- (Štrucl, 1971, 1984; Brigo et al., 1977; Drove- mi plastmi tufov, v osrednjem delu Slovenske- nik et al., 1980). Spodnji del Wettersteinske for- ga bazena pa Psevdoziljske plasti, za katere je macije je bolj masiven in kaže grebenski razvoj zna~ilno menjavanje temnih skrilavih glinavcev, s koralami in hetetidami (Turn{ek, 1997; Bole, pe{~enjakov in tufov; apnenci so podrejeni. Apne- 2002), njen vrhnji del, ki je že cordevolske starosti, nec je po strukturi ponavadi biomikritni mudsto- pa se je ve~ji del odlagal v medplimskem okolju ne ali wackestone, med fosili pa so poleg tankih odprtega {elfa in vsebuje pogoste stromatolitne lupin mehkužcev zastopani predvsem konodonti in loferitne plasti. Proti jugu prehaja Wetter- (Kolar-Jurkov{ek, 1983, 1991; Kolar-Jurkov{ek steinski apnenec v temne glinavce in laporovce & Placer, 1987; Placer & Kolar-Jurkov{ek, 1990; z redkimi polami apnenca. Te plasti, znane kot Kolar-Jurkov{ek & Rižnar, 2006) in radiolariji Partna{ka formacija, so nastajale v zaprtem in Mikrofacies mezozojskih karbonatnih kamnin Slovenije 17 nekoliko globljem delu {elfa. Mestoma so v tem paketu prisotne tudi le~e in gomolji evaporitnih mineralov, predvsem sadre (Štrucl, 1971; Mio~ 1973).

ZGORNJI TRIAS

Karnij Karnijske plasti so najbolj raz{irjene v zahod ni Sloveniji. Znotraj njih stratigrafsko lo~imo plasti cordevolske, julske in tuvalske podstop nje. Zastopane so v plivomorskem in globlje- morskem razvoju. Celotno karnijsko obdobje je trajalo 14 milijonov let. Mo~no okremenjen sparitni dolomit. Vzorec je z dna najgloblje V novej{em obdobju se pojem cordevolska pod- vrtine v Sloveniji (Ljut-1 pri Ljutomeru, 4025 m). Domnevno stopnja opu{~a (Celarc, 2004b; Lucas et al., 2010), triasna starost. Merilo 1 mm ker naj bi te plasti po fosilni združbi pripadale že Sparry dolomite, intensely silicified. Sample from the bot- spodnjemu delu julske podstopnje. Glede na pose- tom of the deepest borehole in Slovenia (Ljut-1 at Ljutomer, ben, bolj grebenski facies masivnega apnenca in 4025 m). Presumably Triassic age. Scale 1 mm dolomita, kakr{en je poznan iz obdobja najnižjega dela karnija v Sloveniji, in glede na tradicijo pri Brdo pri Vrhniki (Ramov{, 1995, 2000). V dolomitu izdelavi Osnovne geolo{ke karte, pa je cordevol- in apnencu so na vseh omenjenih obmo~jih med ska podstopnja v pri~ujo~i monografiji ohranjena fosili najbolj pogoste skeletne alge (Diplopora {e kot samostojna stratigrafska enota. annulata, Diplopora annulatissima, Gyroporella Kamnine cordevolske starosti so razvite le ladinica), ki so mestoma kamenotvorne (Ramov{, karbonatno, ve~ji del kot svetel, masiven zrnat 1988, 1992; Dozet, 1979, 2004; ^ar, 2010). dolomit, v katerem je prvotna struktura kamnine Poseben, plastovit razvoj dolomita poznamo ohranjena le poredko. Po fosilih, predvsem dazi- na Vojskarski planoti v Zgornji Idrijci in v Ga~ neku, kjer v 40 metrov debelem profilu zasledimo kladacejskih algah in koralah sklepamo, da pred- teksture, ki so zna~ilne za litoralno medplimsko stavlja cordevolski dolomit nekdanje grebene, okolje (^ar, 2010). katere je kasneje intenzivno zajela dolomitizaci- Na obmo~ju Severnih Karavank se je v cor- ja. Apnenci cordevolske starosti grade ve~ji del devolu nadaljevala sedimentacija plastovitega Ramov{, Mežakle in Pokljuke v Julijskih Alpah ( apnenca in dolomita v vrhnjem delu Wetterstein- 1988; Ramov{ & Turn{ek, 1984; Turn{ek & Buser, ske formacije. 1989) ter obsežne predele v Kamni{ko-Savinjskih Debelina cordevolskega dolomita in apnen- Alpah (Krvavec, Velika planina, Menina – Pre- ca je lahko precej razli~na in doseže v razli~nih mru, 1974, 2005; Ramov{ & Šribar, 1993; Celarc tektonskih enotah Slovenije od nekaj deset do 2004a; Žalohar & Celarc, 2010), v manj{ih krpah 600 metrov. pa se pojavljajo tudi na Idrijskem, prostoru med Kamnine julske in tuvalske podstopnje so Cerknim in Ljubljano ter v vzhodnih Posavskih pestro, pretežno karbonatno razvite. Med apnen- gubah. Zaradi paleozakrasevanja in lokalnih ci in dolomiti se pojavljajo plasti laporovca emerzij (Buser, 1980b) je apnenec ve~krat obar- ter vložki klastitov in tufov. Njihova debelina van rde~kasto in vsebuje žepe rde~e gline in bo- zna{a med 100 in 400 metri. Klastiti in tufi ima- ksita. Tak apnenec je zanimiv kot okrasni kamen. Pridobivajo ga v kamnolomih Hotavlje in Lesno

Biomikritni apnenec s foraminiferami in {kolj~nimi lupinami. Zna~ilen facies plasti julsko-tuvalske starosti. ^rna voda v Biosparitni apnenec s preseki alge Diplopora annulata. Corde- Tamarju. Merilo 0,5 mm vol. U{ivec na Veliki planini. Merilo 1 mm Biomicritic limestone with foraminifers and bivalves. Char- Biosparitic limestone with Diplopora annulata algae. Corde- acteristic facies of Julian-Tuvalian beds. ^rna voda in Tamar volian substage. U{ivec on Velika planina. Scale 1 mm valley. Scale 0.5 mm 18 Bojan OGORELEC jo od severa proti jugu na Dinarski karbonatni plo{~i vedno ve~ji obseg, tako da na Idrijskem in Ko~evskem že prevladujejo nad karbonati (Ciga- le, 1978; Dozet, 1990a). V nasprotju s cordevolskim dolomitom, so se julske in tuvalske plasti odlagale na zaprtem plitvem {elfu, pogosto v lagunah. Temna barva apnenca in piritni pigment kažeta na redukcij- ske razmere v sedimentacijskem okolju. Apnenec je pogosto laporast in ima mestoma budinaža- sto teksturo. Delež organske snovi se v popre~ju giblje okrog 1 % in doseže najve~ do 4 %, njen izvor pa je ve~ji del terestri~en (Ogorelec et al., 1996a). Po strukturi je apnenec mikriten in biopelmikriten tipa mudstone do packstone, med fosili pa prevladujejo tankolupinske {koljke (Jelen, 1990; Jurkov{ek, 1994), skeletne in neskeletne alge (Poikiloporella duplicata, Clypeina besici), ostrakodi in drobne foraminifere (Nodosaria ordinata, Glomospira sp., Diplotremina astrofimbriata, Lamelliconus multispirus, Ammodiscus parapriscus, Frondicularia pupiformis) (Oblak, 2001) ter {koljke vrste Triadomegalodon idrianus (^ar, 2010). Na nekoliko bolj razgibano okolje kažejo posamezni ooidi in onkoidi. Apnenec je pogosto zajela tako zgodnje- kot poznodiagenetska dolomitizacija ter karstifikacija z žepi in plastmi bok sitov (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 ve~ metrov debele plasti tufskega glinavca. Ta dolomitni paket postopno preide v svetlej{i, pla- stnat dolomit brez vmesnih lapornih pol, v Glavni dolomit. Starost tega dolomita je dolo~ena z do nekaj cm velikimi megalodontidnimi {koljkami, foraminiferami, algami (Poikiloporella duplicata) ter konodonti (Kolar-Jurkov{ek, 1991). Poseben razvoj julsko-tuvalskega zaporedja so Amfiklinske plasti, ki so na Cerkljanskem in v Ba{ki grapi debele do 250 metrov (Buser, 1986b). Zanje je zna~ilno menjavanje temno sive- ga do ~rnega laporastega biomikritnega apnenca, skrilavega laporovca, kremenovega pe{~enjaka, apnen~evih konglomeratov ter tufov in tufitov. V tem kompleksu se na {ir{em Cerkljanskem pojavljajo na ve~ mestih od nekaj pa do 40 metrov debeli grebeni (Senowbari-Daryan & Schäfer, 1979; ^ar et al. 1981; Turn{ek et al., 1984), katere gradijo predvsem spongije in v manj{i meri korale (Turn{ek, 1997). Po teksturnih zna~ilnostih apnencev in po postopni zrnavosti v plasteh sklepamo na sedimentacijo Amfiklinskih plasti na pregibnem delu karbonatnega {elfa proti Sloven- skemu bazenu (Turn{ek et al., 1984). V Julijskih Alpah opazujemo tako plitvomorski kot globljemorski razvoj julskih in tuvalskih plasti. Plitvomorski razvoj opazujemo npr. v Ta- marju in Logu pod Mangartom (Ogorelec et al., 1984; Jurkov{ek, 1987). Apnenec, ki je biomikriten (wackestone do packstone), vsebuje {tevilne skelete foraminifer, drobnih megalodontidnih in Sl. 11. Razvoj karnijskih plasti v meži{kem rudi{~u in Helen- ski grapi pod Peco (prirejeno po Pungartniku in sod., 1982). drugih {koljk ter plo{~ic ehinodermov; ve~krat je Fig. 11. Development of Carnian beds in Mežica mine and dolomitiziran. Pogosto je laporast (do 15 % ne- Helena gorge at the foot of Mt.Peca (adapted after Pungartnik karbonatne primesi, ve~inoma glina in organska et al., 1982). Mikrofacies mezozojskih karbonatnih kamnin Slovenije 19 snov). Za globljemorski razvoj je zna~ilen gost biomikritni apnenec z gomolji roženca. V favni prevladujejo tankolupinske {koljke, kalcitizira- ni radiolariji in naplavljene plo{~ice ehinodermov (Ogorelec et al., 1984; Jurkov{ek 1987). V teh plasteh so bili na Kozji dnini pod Triglavom najdeni fosilna riba Birgeria sp. (Jurkov{ek & Ko- lar-Jurkov{ek, 1986), ~rv Valvasoria carniolica (Kolar-Jurkov{ek & Jurkov{ek, 1997) in {tevilni drugi fosili (Dobruskina et al., 2001; Bitner et al., 2010), v zahodnih Karavankah pa alga Clypeina besici (Kolar-Jurkov{ek & Jurkov{ek, 2003), ma- kroflora D( obruskina et al., 2001), foraminifere in konodonti (Kolar-Jurkov{ek et al., 2005). Julske in tuvalske plasti so v Severnih Kara- Sl. 12. Razli~ni tipi ciklotem v Dachsteinskem apnencu na vankah pri Mežici zastopane z do 350 metrov de- Krnu (Ogorelec & Buser, 1997) belim zaporedjem apnenca in dolomita (sl. 11), ki Na levi je klasi~na loferska ciklotema po Fischerju (1964). je razvito v 20 ciklotemah loferskega tipa, zna~ilni 1 – megalodontide; 2 – korale in onkoidi; 3 – apnenec z zanje pa so trije klasti~ni horizonti skrilavca, me- izsu{itvenimi porami (loferit); 4 – laminit; 5 – stromatolit; 6 – tempestitne plasti (»nadplimski konglomerat«); 7 – korozijske ljevca in laporovca (Štrucl, 1970, 1971; Pungart votline; 8 – emerzijska bre~a z rezidualno karbonatno glino nik et al., 1982). Klasti~ne horizonte povezujemo z evstati~nimi fazami in humidnim klimatskim Fig.12. Various types of cyclothems in the Dachstein limestone sunkom, znanim kot CPE (Carnian Pluvial Event on Mt. Krn, Julian Alps (Ogorelec & Buser, 1997). – Kolar-Jurkov{ek & Jurkov{ek, 2010). Nekatere Classical Lofer cyclotheme after Fischer (1964) is on the left. plasti so izredno bogate s fosili (Jurkov{ek 1978; 1 – Megalodontids; 2 – Corals and oncoids; 3 – Limestone with shrinkage pores (loferite); 4 – Laminite; 5 – Stromatolite; 6 – urkov ek olar urkov ek aim J { & K -J { , 1997; K et al., Tempestite layers (»flat pebble conglomerate«); 7 – Solution 2006; Jurkov{ek et al., 2002; Kolar-Jurkov{ek & cavity; 8 – Emersion breccia with residual carbonate clay Jurkov{ek, 2009, 2010). Na bolj razgibano okolje znotraj plitvega {elfa kažejo posamezne oolitne plasti in onkoidi.

Norij in retij Kamnine norijske in retijske starosti so v Slo- veniji zastopane v treh razvojih. Na obeh karbonatnih plo{~ah, Julijski in Dinarski, se pojavljata Glavni dolomit in njegov lateralni razli~ek Dach steinski apnenec, v Slovenskem bazenu pa sta razvita Ba{ki dolomit in Železnikarski apnenec (sl. 13). Glavni dolomit in Dachsteinski apnenec zavzemata precej{en obseg in sta najbolj razpro- stranjeni 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 ve~jem delu razvit na Julijski platformi, medtem ko na Dinarski karbonatni platformi prevladuje dolomit. Debelina Ba{kega dolomita je tri do {tirikrat tanj{a in je ocenjena na najve~ 400 metrov (Buser, Loferitni dolomit z izsu{itvenimi porami prera{~a stromato- 1986b). litna plast, nad njo pa je mikritni dolomit. Zna~ilen facies Dachsteinski apnenec je debeloplastnat in kaže medplimskega okolja. Dachsteinski apnenec, norij. Grudnica zna~ilen loferski razvoj, kakr{en je poznan iz Se- nad Slapom ob Idrijci. Merilo 1 cm vernih Alp (Fischer, 1964; Zankl, 1971; Piller & Loferitic dolomite with shrinkage pores, overgrown by stromatolite layer and micritic dolomite. Characteristic facies Lobitzer, 1979; Piller, 1981), Dolomitov (Bosel- of the intertidal environment. Dachstein limestone, Norian. lini, 1967; Bosellini & Rossi, 1974) ali Madžarske Grudnica above Slap ob Idrijci. Scale 1 cm (Haas, 1994). Posamezne cikloteme (sl. 12) sestav ljajo do 2 metra debele plasti biomikritnega in lieri, Galeanella sp.), alge (Macroporella retica) biosparitnega apnenca, katerega prekinjajo tanke in ehinodermi. V nekaterih plasteh so velike me- stromatolitne in loferitne plasti ter lokalno tudi galodontidne {koljke kamnotvorne. Dachstein- medplastovne bre~e z glinenim vezivom. ski apnenec se je odlagal na plitvem, odprtem in Med fosili so najbolj pogoste foraminife- priobrežnem {elfu, z ob~asnimi medplimskimi in re (Triasina hantkeni, Aulotortus gr. sinuosus, nadplimskimi pogoji (Ogorelec, 1988; Ogorelec A. permodiscoides, A. friedli, Miliolipora cuvil & Rothe, 1992; Dozet & Ogorelec, 1990). Plasti, 20 Bojan OGORELEC

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 ve~krat dolomitizirane. Na Julijski karbonatni plo{~i se znotraj formacije Dachsteinskega apnenca pojavljajo ve~ji grebenski masivi (Begunj{~ica, Pokljuka, Bo- hinj) ali manj{i grebeni z bogato koralno favno (Turn{ek & Ramov{, 1987; Turn{ek & Buser, 1991; Turn{ek, 1997). Ob~asno je na obeh, Dinarski in Julijski karbonatni plo{~i pri{lo do kratkotrajnih okopnitev njunih posameznih delov. V takih primerih se je razvil paleokras. Slednji je posebno lepo razvit na Kaninskem pogorju in na Krnu (Babi}, 1980/81; Ogorelec & Buser, 1996). Ena- ko favno in mikrofacies, kot ju opazujemo v grebenskem apnencu slovenskega dela Alp, kažejo tudi norijsko-retijski grebeni v Severnih Alpah Korozijska votlina s kokardno teksturo sparitnega kalcita na- (Zankl, 1971; Flügel, 1981; Piller, 1981; Stanton kazuje paleozakrasevanje. Dachsteinski apnenec v Smrekovi & Flügel, 1989; Flügel & Koch, 1995; Turn{ek et Dragi na Trnovskem gozdu. Merilo 5 cm al., 1999). Solution cavity filled with sparry calcite of cockade textu- Glavni dolomit kaže monoton, popolnoma reindicating paleokarstification. Dachstein limestone from dolomiten razvoj. Zanj je zna~ilno cikli~no me- Smrekova Draga on Trnovski gozd. Scale 5 cm njavanje debelej{ih dolosparitnih in biomikrit nih plasti s tanj{imi stromatolitnimi plastmi, dolomit in Železnikarski apnenec (Buser, 1979; loferiti, mestoma tudi z nadplimskim konglo- Ramov{, 1970; Gale, 2010). Karbonatni sediment meratom in emerzijskimi bre~ami. Med fosili so v obeh formacijah je mikriten, z zelo redkimi zastopane velike megalodontide, foraminifere fosili, drobnimi foraminiferami (Roži~, 2006, in alge. Lokalno so prisotne tudi plasti in le~e z 2008; Roži~ & Kolar-Jurkov{ek, 2007; Buser & onkoidi in vadoznimi pizoidi (Ogorelec, 1988; Ogorelec, 2008; Roži~ et al., 2009; Gale, 2010) in Dozet, 1991). Glavni dolomit se je, sprva kot konodonti (Kolar-Jurkov{ek, 1982, 1991, 2011), apnenec, odlagal na zelo plitvem zaprtem {elfu zna~ilne za obe formaciji pa so vmesne plasti in z obsežnimi medplimskimi ravnicami, v plitvej gomolji roženca. {em delu {elfa kot Dachsteinski apnenec. Dolomi- tizacija je bila zgodnjediagenetska z »evaporative pumping« modelom (Illing et al., 1965), kasneje JURA pa je kamnino zajela {e kasnodiagenetska dolomitizacija. Tudi dolomit kaže ve~krat znake pa- Prostor Slovenije je, enako kot v srednjem in leozakrasevanja. Manj{e in ve~je korozijske votli- zgornjem triasu, tudi v juri pripadal trem geotek- ne zapolnjuje conarni sparitni cement, ve~krat je tonskim enotam, ki isto~asno predstavljajo tudi vmes tudi rde~ interni mikrit. razli~na sedimentacijska okolja. Južna Slovenija V istem obdobju, ko sta se odlagala na plat- je bila sestavni del Dinarske karbonatne plo{~e, formi Dachsteinski apnenec in Glavni dolomit, za katero sta zna~ilni plitvomorska sedimentacija sta v bazenu in njegovem obrobju nastajala Ba{ki in velika debelina karbonatnih kamnin, ki v juri Mikrofacies mezozojskih karbonatnih kamnin Slovenije 21

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 plo{~o omejeval Slovenski bazen, severno od njega pa je obstajala Julijska karbonatna plo{~a. Ta je v dog gru razpadla, tako da se je bazen raz{iril tudi na ta prostor.

Dinarska karbonatna plo{~a Prehod zgornjetriasnega Glavnega dolomita in Dachsteinskega apnenca v jurske plasti ni oster. Ponekod je na kontaktu razvit do nekaj deset metrov debel paket intraformacijske bre~e (npr. ^epovan, Gr~arevec), ki je nastala v kratkotrajnih emerzijskih fazah (Buser, 1979b; Ogorelec & Rothe, 1992; Jurkov{ek et al., 1996). Stroma- toliti, ki so zna~ilni za Glavni dolomit, postopno izginjajo, {e vedno pa so v spodnjeliasnih plasteh pogoste teksturne oblike litoralnega okolja – izsu{itvene 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 razli~na okolja znotraj karbonatnega {elfa (Buser, 1979b; Orehek & Ogorelec, 1979, 1981; Strohmenger & Dozet, 1990, Dozet, 1992a,b). Na Trnovskem gozdu, Hru{ici, Loga{ki planoti in na Gorjancih se je sedimentacija odvijala na odprtem delu {elfa z vi{jo energijo. Prevladujejo oolit ni apnenci (Buser, 1973,1978; Strohmenger et al., 1987; Ogorelec & Dozet, 2000), ki lahko dosežejo debelino tudi ve~ sto metrov. Med njimi se ponekod pojavljajo plasti z velikimi onkoidi. Lokalno so pogoste litiotidne {koljke, ki gradijo lumakele (Buser, 1978; Buser & Debeljak, 1996, Debeljak & Buser, 1998; Ramov{, 2000). Med fosili, ki jih opazujemo v zbruskih spod njejurskih - liasnih plasti, sta pomembni algi Paleodasycladus mediterraneus in Sestrospha- Sl. 15. Spodnjeliasne plasti v Preserju pri Borovnici era liasina, med foraminiferami pa so dolo~ene (Ogorelec, 2009) vrste Orbitopsella praecursor, Involutina liassi- Fig.15. Lower Liassic beds in Preserje near Borovnica ca, Agerella martana, Trocholina turris, Pseudo- (Ogorelec, 2009) 22 Bojan OGORELEC Mikrofacies mezozojskih karbonatnih kamnin Slovenije 23

, o er ek ek & { { g g och O en K 1992), 1992), , 1990 urn m , T urkov elwalle J ozet troh othe D et al., 1994), et al., 1994),

D S R et al., 1981), 1981), et al., , 2008, 2010), 2010), 2008, , ek ek & & { { er rötsch g – Dolenja – Dolenja 2005), 47 33 – Sabotin ( , urn , 1990, G T en ), urkov orelec – Podhosta, , 1991), 25 – Podhosta, oni m J g ozet ar mb O b D – Bistra pri Verdu ( Verdu pri Bistra – 13 troh , 2011 – Banj{ka planota ( ri – Slovenski vrh - , 1979), 29 – Slovenski vrh - S Š icca ež & ar J R b er & , 2005), 44 – Kozina ( ri g Š , 2009), , ar en et al., 1996; al., et ~ ozet

m – Julijske Alpe - Trenta ( 20 – Julijske Alpe - Trenta 1978), 51 D ek ), ~, { leni P troh orelec Oolitni apnenec. Spodnjeliasne plasti v Preserju pri Borovni- 2004) ani et al., 1995 ; et g S

, p

O ci. Merilo 1 mm u – Kanalski vrh - Levpa ( – ^epovan - Lokve ( urkov Z J , 1966, 1969, 1972, 1997; , 1966, 1969, 1972,

user Oolitic limestone from the Lower Liassic succession in Pre- 1996; liese 37 28 – Logatec ( – Nanos - Nadrt ( – Nanos - Nadrt , g ek }, 1980/81},

), serje at Borovnica. Scale 1 mm i } & u { ek i b – Krka - Mali Korinj ( { P b a } & B a i urn B B ~ 1990), T

, 1991 , , urkov 1980/81), 9 – Kras ( Kras – 41 , J adoi ., 1995), 32 , 1978), 24 – Delnice ( R u ~ & rötsch L orelec

ar g et al., 1995; et al., G ani ~ orelec p ar O , 1991), , g 1974 ; u b O Z ar ri & , 1990c, 1999), 6 leni ~ – Mala gora - Kompolje ( Š ansen P & H och } & – Preserje pri Borovnici ( Borovnici pri Preserje – 12 et al., i – Trnovski gozd ( gozd Trnovski – ozet

leni b K P D a

er 16 rehek – Batognica pri Krnu ( B {~ & O ), u 1992), ar , K b , 1992a,b), 3 et al., 1998; ri 36 – Kanalski vrh ( Š , 1995 othe och R ozet

et al., 1989; K D ozet & 2011), et al., 1995, 2007; 1995, et al.,

och D , K 2007), 43 – Senože~e ( – Podbrdo - Zalilog ( et al., 1982a), 50 – Podbrdo ež ,

J ek orelec , 1981, orelec { g g user ar O , 2005, 2008, 2009), 19 b , 1988; O B ~ 1977, 1978; ri , Onkoidi v zgornjeliasnem apnencu. Prelaz Vahta na Gorjan- Š urkov och oži – JZ Slovenija ( JZ Slovenija – 40 J cih. Merilo 5 cm et al., 2006), 23 – Zalilog ( - och R K & K Oncoidal limestone of Upper Liassic succession. Vahta pass on

olar Gorjanci Mts. Scale 5 cm ozet orelec K – Suha Krajina ( 15 2008;

, D g – Racna gora pri Lo{kem Potoku ( et al., 1976, 1987b), 53 – Bovec ( O & cyclammina liassica in Haurania deserta (Šribar, ek { et al., 2011), et al., – Trnovo ( 27 – Trnovo

orelec 1979a in podatki iz razli~nih tolma~ev k Osnovni g ež ), orelec J g O geolo{ki karti 1 : 100.000). Številni so tudi, sicer 1980/81), , O urkov J

& za stratigrafijo manj pomembni, primerki alge 2011), 35a – Kali{e - Logatec ( 1980/81), 8

, , , 1990 , 1987), 31 – Nanos ( – Bohor, Kr{ko ( , 1965), 49 – Bohor, Thaumatoporella parvovesiculifera, ehinodermi, ež – Južna Slovenija (Ko~evska gora, Goteni{ka user J orelec ar

5 mikrogastropodi, {koljke, ostrakodi, mestoma B ozet g b ), O ri D orelec

– Prezid, Ko~evsko ( – Prezid, pa tudi drobni brahiopodi. V doggerskih plasteh g Š orelec , 2005), 22 – Bovec ( g O & sta dolo~eni foraminifera Mesoendothyra croati- O uc et al., 1996; – Kras - K/T meja (K/T boundary) ( boundary) (K/T meja K/T – Kras - 46 , 1996 m & ca in alga Selliporella donzelli. Na Hru{ici in na ek – Kobla ( Š & {

rehek Trnovskem gozdu so poredke kopu~e koral in pla- 18 ozet O och rehek D ),

K sti krinoidnega apnenca. O 1990; urkov , 1980/81), 2

J Na Notranjskem nastopa v spodnji in srednji , 1997, – Smrekova Draga na Trnovskem gozdu ( gozdu Trnovskem na Draga Smrekova – 1979), 11 juri temno siv biomikritni in pelmikritni apnenec, , et al., 2001), et al., et al., – Matarsko podolje - Hru{ica ( Hru{ica - Matarsko podolje –

orelec ki kaže na sedimentacijo v bolj zati{nih in zapr- g ozet ek 39 , 1985), 26 – Ko~evsko ( O { et al., 2002), 35 – Sabotin ( D relec tih delih {elfa z lagunami in ob~asno redukcijski- orelec o g g

& rehek gorelec & mi pogoji (O & O , 1981). Ve~krat se och O K urkov

2011), med apnencem pojavljajo le~e zrnatega dolomita. orelec J & O , g

rehek Na Ko~evskem zasledimo mestoma tudi tanj{e O orelec ež O J g plasti premoga (Dozet, 1998). Debelina spodnje- et al., 1987a, 1996b; & O rehek

O in srednjeliasnih plasti zna{a 200 do 400 metrov, – Doblar - vol~anski apnenec (Vol~e limestone) ( – Doblar - vol~anski apnenec (Vol~e

et al., 1992), 30 – Dutovlje ( zgornjeliasnih in doggerskih pa prav tako do 450 rehek orelec ek – Bela Krajina, Ko~evski Rog ( O – Travna gora - Jelenov žleb ( – Travna g – Vrhnika - Logatec ( Logatec - Vrhnika – , 1992), 14 { metrov (Buser, 1979b). O

– Gori{ka Brda ( et al., 1988, 1989, 1995), 48 – Gori{ka Brda V spodnjem malmu se je preko Trnovskega urn othe ne T R b

, 1976), 52 gozda, ki je v tem ~asu predstavljal severni rob 34 – Sabotin - Mrzlek ( ro , 1993), 7 – ^ebulovica ( – ^ebulovica , 1990), 45

& Dinarske karbonatne plo{~e, vlekel ve~ deset km ), D user Jugorje - Gorjanci (

B dolg in nekaj km {irok koralno-stromatoporidni – ozet user Ko~evje ( 17 – Laze pri Sevnici ( Ko~evski Rog ( Sl. 14. Shematski prikaz litolo{kega razvoja jurskih in krednih karbonatnih kamnin v Sloveniji z vrisanimi litostratigrafskimi stolpci in literaturnimi podatki. Sl. 14. Shematski prikaz litolo{kega razvoja jurskih in krednih data. in Slovenia with the position of lithostratigraphic sections and their reference carbonate rocks of lithologic development Jurassic and Cretaceous Fig. 14. Schematic presentation 1 D relec et al., 1987), 4 ( et al., 1990), 21 – Mangart 1988 & 42 – Komen ( – Matarsko podolje ( podolje Matarsko – 38 B vas ( – Trnovski gozd ( gozd Trnovski – 10 greben. Debel je do 500 metrov (Turn{ek, 1966, 24 Bojan OGORELEC

Gru~a alg vrste Clypeina jurassica v mikritnem apnencu. Zgornja jura – malm. Cestni usek med Vrhniko in Logatcem. Merilo 1 mm Algal limestone with Clypeina jurassica. Upper Jurassic – Malm. Old road cut between Vrhnika and Logatec. Scale 1 mm

1969, 1972, 1997; Turn{ek et al., 1981). Med grebeni, ki so se s prekinitvami vlekli {e v Suho Kra- jino in preko Gorjancev v Liko na Hrva{ko (Veli} et al., 2002) so se odlagale medgrebenske bre~e ter plastoviti apnenci s hidrozojem Cladocoropsic mirabilis. Za zgornji malm (kimmeridgij in tithonij) so zopet zna~ilni oolitni in biomikritni apnenci z algama Clypeina jurassica in Salpingoporella annulata (Buser, 1979b; Orehek & Ogorelec, 1981; Strohmenger & Dozet, 1990) ter z aberantnimi tintinidami (Ker~mar, 1961). Med foraminiferami

Sl. 16. Shematski profil jurskih plasti na Trnovskem gozdu (Orehek & Ogorelec, 1979) Fig. 16. Schematic columnar section of Jurassic beds on Malmski koralni greben. Selovec na Trnovskem gozdu Trnovski gozd (Orehek & Ogorelec, 1979) Malmian coral reef. Selovec on Trnovski gozd Mikrofacies mezozojskih karbonatnih kamnin Slovenije 25

Sl. 17. Shematski presek malmskega bariernega grebenskega kompleksa v Sloveniji s facialno conacijo in favnisti~nimi združbami (Turn{ek et al., 1981) Fig. 17. Schematic cross section of the Malmian barrier-reef complex in Slovenia showing its facies zonation and faunal associations (Turn{ek et al., 1981) so ugotovljene troholine (Trocholina alpina in gostim mikritnim apnencem tipa »biancone«, ki T. elongata), Protopeneroplis striata, Pfenderina vsebuje gomolje in pole roženca. V apnencu so salernitana, Kurnubia palestinensis, K. jurassica pogoste kalpionele in radiolariji. Enak apnenec in Nautiloculina oolithica (Šribar, Lj. – analize se je odlagal zvezno {e v spodnji kredi, berriasiju za OGK). Nekatere plasti kažejo znake litoralne in spodnjem valanginiju, tako da doseže celoten sedimentacije. Na Trnovskem gozdu je del karbo paket kalpionelidnih apnencev do 250 metrov natnega kompleksa popolnoma dolomitiziran. (Cousin, 1981; Buser, 1986, 1987; Jurkov{ek, 1987; Jurkov{ek et al., 1990). Slovenski bazen Julijska karbonatna plo{~a Jurske plasti v pelagi~nem razvoju so razvite na {ir{em prostoru Tolmina in Bovca, v predgorju Spodnjejurske plasti so razvite v plitvomor- Julijskih Alp in v zahodnem delu Južnih Kara- skem faciesu odprtega {elfa. V njih se menjavajo vank, v manj{em obsegu pa tudi v vzhodnem delu biosparitni, oolitni in mikritni apnenci, mesto- Posavskih gub. ma pa so prisotne tudi stromatolitne in loferitne Liasne plasti, ki dosežejo debelino do 300 me- plasti. Na kontaktu z zgornjetriasnimi karbonati trov, so zastopane s plo{~astim mikritnim apnen- so ponekod emerzijske bre~e in neptunski dajki, cem z gomolji roženca, med katerim so tudi tan- oboji zapolnjeni z rde~kastim glinastim vezivom ke plasti glinastega laporovca. Med fosili sta (Babi}, 1980/81; Jurkov{ek et al., 1990; ^rne et al., prisotni foraminiferi Ophthalmidium leischneri 2007). in Involutina liassica ter radiolariji in spongije. V zgornjem liasu je bila Julijska karbonatna Ob robovih bazena so se odlagali debelej{i pa- plo{~a razkosana na ve~ blokov, ki so bili razli~no keti apnen~evih bre~, ki so splazele po pregibu poglobljeni. Na njih se je pri~ela pelagi~na sedi- z roba {elfa (Roži~, 2006, 2008; Roži~ & Popit, mentacija ter kondenzacija sedimentov (Buser, 2006; Buser & Ogorelec, 2008). Med kosi bre~e 1986a; Jurkov{ek et al., 1990; Šmuc, 2005). Na so pome{ani tudi ooidi. Bre~a in plasti drobnej{ih Mangartu, Rombonu, v Trenti ter v Dolini Tri- kalkarenitov pogosto kažejo postopno zrnavost in glavskih jezer izdanjajo rde~kasti biomikritni laminacijo. Na Begunj{~ici so plo{~asti apnenci apnenci tipa »ammonitico rosso«, ki vsebujejo z roženci impregnirani z manganovimi oksidi in železove in manganove gomolje (Jurkov{ek et al., vsebujejo {tevilne amonite. 1990; Šmuc, 2005; Ogorelec et al., 2006). Opisani Doggerske in spodnjemalmske plasti se težko apnenci kažejo zelo podoben mikrofacies, kot je dolo~ijo s fosili, debele pa so le nekaj deset metrov. poznan s klasi~ne lokalnosti gomoljastih globlje- Zastopane so z glinastimi skrilavci, radiolariti in morskih apnencev v Severnih Alpah (npr. Adnet s plastmi mikritnega in biomikritnega apnenca z pri Salzburgu – Böhm et al., 1999). roženci (Buser, 1979b; Ogorelec & Dozet, 1997). Nad manganskim horizontom leži {e do nekaj Med fosili se pojavljajo foraminifera Globigerina deset metrov rde~ega in rjavkastega mikritnega helvetojurassica in radiolariji (Gori~an, 1997). apnenca z radiolariji in gomolji roženca dog Zgornji malm – tithonij je v do 50 metrov de- gerske in malmske starosti, nato pa berriasijski beli skladovnici zastopan z belim in svetlosivim apnenec z gomolji roženca tipa »biancone«. 26 Bojan OGORELEC

Biomikritni apnenec z lupinami moluskov in radiolarijev. Pe lagi~ni 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 ~asu segal tudi na prostor Julijske karbonatne plo{~e, pa kot fli{ne plasti z vmesnimi paketi globljemorskih apnencev. Debelina krednih Sl. 18. Globljemorski razvoj zgornjetriasnega Ba{kega plasti na Dinarski plo{~i doseže do 2000 metrov, v dolomita in jurskih plasti na Kobli (Buser & Ogorelec, 2008) bazenu pa do 800 metrov (Buser, 1989; Pleni~ar, Fig. 18. Deeper-marine development of Upper Triassic Ba~a 1979, 2009). Koncem krede je pri{lo na južnem dolomite and Jurassic beds on Mt. Kobla, Julian Alps Primorskem in v Istri do dolgotrajnej{e okopnit (Buser & Ogorelec, 2008) ve. V istem obdobju je Dinarska karbonatna plo {~a razpadla na ve~ manj{ih enot z vmesnimi Vzhodne Alpe fli{nimi bazeni, ki so se že od zgornje krede pa vse do konca paleogena postopno selili od severa ozi- V Severnih Karavankah so spodnjejurske roma Bov{kega proti jugu v osrednjo Istro (Buser, plasti v okolici Ur{lje gore razvite kot rde~kasti 1986b). Shematski prikaz razvoja krednih plasti plo{~asti in gomoljasti rde~kasti apnenci z le~ami je prikazan na slikah 2 in 3, posebej pa na sliki 14. roženca, ki so se odlagale v globljem morju (Ramov{ & Rebek, 1970; Mio~ & Šribar, 1975). Dinarska karbonatna plo{~a

KREDA Spodnjekredne plasti so v plitvomorskem raz voju najbolj raz{irjene na Dolenjskem, Notranj- ^eprav je bila kredna perioda v mezozojskem skem, Hru{ici in na zahodnem delu Trnovske- obdobju najdalj{a, saj je trajala kar 80 milijonov ga gozda. Razvite so dokaj monotono in kažejo let, je na slovenskem prostoru razvita dokaj mo- zna~ilnosti sedimentacije na zaprtem {elfu z lagu- notono, na Dinarski plo{~i kot debela skladovnica nami in ob~asnimi medplimskimi pogoji. Glede na apnencev in dolomitov, v Slovenskem bazenu, ki mikrofacies prevladujejo med apnenci tipi z mi- Mikrofacies mezozojskih karbonatnih kamnin Slovenije 27 kritno osnovo (mudstone do packstone) ter s fosili, ki so zna~ilni za bolj mirno okolje – foraminifere, ostrakodi, alge in moluski. Litolo{ko je prehod zgornjejurskih plasti v berriasijske postopen. Apnenec je po strukturi biopelmikriten, ve~krat z izsu{itvenimi porami in z laminacijo, mestoma rahlo laporast in zaradi sledov organske primesi ponavadi temnej{e sive barve. Nekatere apnen~eve plasti je zajela tudi zgodnja ali/in poznodiagenetska dolomitizacija. Slednja se kaže v dolomitnih romboedrih, pogosto s conarno zgradbo ter z manj{imi le~ami zrnatega dolomita. Šribarjeva (1979b) je celotno spodnjekredno zaporedje na Loga{ki planoti razdelila na osnovi mikrofosilne združbe v pet cenocon, enaka razdelitev pa je veljala tudi za prostor Trnovskega go Biomikritni apnenec z algo Salpingoporella dinarica. Facies plitvega zaprtega {elfa. Aptij-albij. Nanos. Merilo 1 mm zda (Koch, 1988; Koch et al., 1989) in za Ko~evsko Biomicritic limestone with Salpingoporella dinarica algae. (Dozet, 1990c; Dozet & Šribar, 1991): Shallow restricted shelf facies. Aptian-Albian. Nanos. Scale Za berriasijske in valanginijske plasti sta 1 mm zna~ilna in najbolj pomembna mikrokopro- lit Favreina salevensis in alga Salpingoporella pri{lo na Dinarski karbonatni plo{~i zaradi in- annulata. Favreine so mestoma tako {tevilne, da tenzivne tektonike do njene diferenciacije in do so kamnotvorne. Med foraminiferami se pojavlja spremembe paleookolja. To je privedlo do bolj vrsta Pseudocyclammina lituus. V vrhnjem delu pestrega faciesa in ve~ razlik v debelini posamez valanginijskih in v hauterivijskih plasteh so pri- nih cenocon znotraj posamezne serije (Koch et sotne alga Clypeina solkani, foraminiferi Pseudo- al., 1989). Lokalno je pri{lo tudi do kratkotrajnih textulariella salevensis in Orbitolinopsis capuen- okopnitev posameznih delov plo{~e. Na Krasu je sis, v ve~jem {tevilu pa so prisotni {e ostrakodi taka okopnitev nakazana z emerzijsko bre~o na in drobni moluski. Tudi v tem obdobju so poleg meji med Brsko in Povirsko formacijo (sl. 19) ozi- biomikritnih apnencev prisotni mikrofacialni tipi roma na meji med aptijem in albijem (Jurkov{ek s pogostimi izsu{itvenimi porami, ki kažejo na et al., 1996; Jurkov{ek, 2008, 2010; Koch & Ogo- podobne paleogeografske razmere kot v valangi- relec, 1987). Apnenec od valanginijske pa vse do niju – zaprt {elf z lagunami in medplimskimi rav- albijske starosti je pogosto dolomitiziran, delno nicami (Orehek & Ogorelec, 1979, 1981; Šribar, ali v popolnosti; dolomitizacija ima poznodiage- 1979b; Dozet & Šribar, 1991). netski zna~aj. Barremijski apnenec je zastopan z daziklada- V vrhnji del spodnjekrednih plasti, ki je albij- cejskimi algami vrste Salpingoporella muehlber- ske starosti, Šribarjeva (1979b ter Dozet & Šribar, geri, aptijski pa z vrsto Salpingoporella dinarica, 1991) pri{teva apnen~eve in dolomitne plasti z ki je v nekaterih plasteh na prehodu v albij iz- orbitolinami (Orbitolina ex gr. texana) ter fora- redno {tevilna. V aptiju vrsto S. dinarica sprem miniferami (»Valdanchella« dercourti). Dokaj po ljajo {e foraminifera Palorbitolina lenticularis, goste v tej cenoconi so tudi miliolide, med molu- miliolide ter {tevilni primerki mikroorganizma ski pa rekvienije. problemati~nega izvora Bacinella irregularis, za Vi{ji energijski indeks znotraj spodnjekred katerega se domneva, da pripada cianobakterij- nega zaporedja nakazujejo redke plasti z ooidi skim tvorbam (Flügel, 2004). V tem obdobju je in psevdooidi. Oboji so bili v mirnej{e okolje z mikritnim karbonatnim blatom naplavljeni in pome{ani s peleti in drobnimi fosili. Lokalno so obstajali tudi manj{i grebeni in biostrome koral, hidrozojev in alg. Iz berriasija in valanginija je znan tak koralni greben pri Zavrhu na Banj{ki planoti (Turn{ek & Buser, 1974), iz ~asa aptija in albija pa so opisani koralni grebeni iz Kanalske- ga vrha in okolice na Banj{ki planoti (Turn{ek & Buser, 1974; Grötsch, 1991; Grötsch et al., 1994) in s Ko~evske gore (Turn{ek et al., 1992). V aptiju je bil na Sabotinu manj{i algni greben, zgrajen v ve~jem 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 ~rnega biomikritnega in biopelmikritnega plo{~astega bitu- Rudistni apnenec. Štanjel na Krasu minoznega apnenca z gomolji roženca (»Trnovski Limestone with rudist bivalves. Štanjel na Krasu plo{~asti apnenec«, Pleni~ar & Buser, 1967), ki 28 Bojan OGORELEC

Sl. 19. Litostratigrafski stolpec krednih in paleogenskih plasti severnega dela Trža{ko-komenske planote (Jurkov{ek, 2010) Fig. 19. Lithostratigraphic column of Cretaceous and Paleogene beds of the northern part of Trieste-Komen plateau (Jurkov{ek, 2010) Mikrofacies mezozojskih karbonatnih kamnin Slovenije 29

vsebuje do 1,1 % Corg. Analize ve~ vzorcev kaže- jo, da ta apnenec lahko uvr{~amo med potencial- ne mati~ne kamnine za nastanek ogljikovodikov z nizko sposobnostjo njihovega generiranja (Ogo- relec et al., 1996a). Zgornjekredne plasti so se odlagale na bolj odprtem in plitvem {elfu z vi{jim energijskim in- deksom. Zna~ilne zanje so svetla barva apnencev, debele plasti in bogata rudistna favna (Pleni~ar, 2005; Pleni~ar & Jurkov{ek, 1996, 1998). Za- stopani so sicer vsi tipi apnencev, vendar pa sta tipa packstone in grainstone najbolj pogosta. V ve~jem obsegu zgornjekredne plasti izdanjajo na Trža{ko-komenski planoti in na Nanosu, v manj{em obsegu pa tudi na Javornikih, Dolenj- skem in Ko~evskem. Zaradi velikih debelin posameznih plasti, zanimivega izgleda in dobrih tehni{kih lastnosti kamna, so le-te zanimive kot arhitektonski kamen, ki ga predvsem na Krasu lomijo v {tevilnih kamnolomih. Dolomitnih plasti je precej manj kot v spodnjekrednem zaporedju. Kljub enoli~nemu litolo{kemu razvoju je mo- Rudistni rožasti apnenec (»fiorito«) (foto: B. Jurkov{ek) žno natan~no raz~leniti zgornjekredne plasti na Rudist ornamental limestone (»fiorito«) (photo: B. Jurkov{ek) osnovi fosilov, predvsem rudistov in foraminifer, (Šribar & Pleni~ar, 1990; Pleni~ar, 1960, 1979, in Rhapydionina liburnica (Šribar & Pleni~ar, 2005, 2009; Jež, 2011). Taka razdelitev je za pro- 1990). stor jugozahodne Slovenije prikazana na sl.19. Za Na obmo~ju Trža{ko-komenske planote so srednji in zgornji cenomanij je med foraminife- izdvojene formacije: Povirska formacija ceno- rami zna~ilna Broeckina (Pastrikella) balcanica, manijske starosti, Sežanska formacija zgornje- za zgornji turonij neskeletna alga Aeolisaccus ko- turonijske, coniacijske in santonijske starosti ter tori, za obdobje coniacija in spodnjega santoni- Lipi{ka formacija santonijske in campanijske ja foraminifera Pseudocyclammina sphaeroidea starosti (Jurkov{ek et al., 1996; Jurkov{ek, 2008, za zgornji santonij in campanij Keramospherina 2010; Jurkov{ek & Kolar-Jurkov{ek, 2007). Zno- tergestina, za maastrichtij pa Orbitoides media traj Repenske formacije, ki obsega spodnji tu-

Sl. 20. Zgornjekredne cenocone v jugozahodni Sloveniji (Šribar & Pleni~ar 1991) Fig. 20. Upper Cretaceous assemblage zones in south-western Slovenia (Šribar & Pleni~ar, 1991) 30 Bojan OGORELEC ronij, so v posameznih nivojih izredno {tevilne kalcisfere, ki so lahko celo kamenotvorne (kal- cisferski packstone) in kažejo na evstati~ni dvig morske gladine med cenomanijem in turonijem (Jenkyns 1985, 1991; Haq et al., 1987; Jurkov{ek et al., 1996; Jurkov{ek, 2010) oziroma na potopi- tev platforme. Sedimentolo{ko in mikrofacialno posebnost znotraj spodnjega dela Sežanske formacije predstavlja ve~ metrov debel horizont z velikimi onkoidi (Onkoidni apnenec, Jurkov{ek et al., 1996; Jurkov{ek, 2010). Ta onkoidni horizont je splo- {no raz{irjen in prepoznaven na celotni Dinarski karbonatni plo{~i (Gu{i} & Jelaska, 1990; Ti{ljar et al., 2002). Biosparitni apnenec s preseki foraminifer Rhapydionina li- Na prostoru Dinarske karbonatne plo{~e sta burnica in {tevilnih miliolid. Facies plitvega odprtega {elfa. obstajali v zgornji kredi dve izrazitej{i emerzij- Maastrichtij. Tabor pri Štorjah. Merilo 1 mm ski fazi, katerih posledica so stratigrafske vrzeli. Biosparitic limestone with foraminifers Rhapydionina libur- Prva taka faza, v obdobju zgornjega cenomanija nica and numerous miliolids. Shallow open shelf facies. Maas- do conijacija je obstajala na severnem robu plo{~e trichtian. Tabor at Štorje. Scale 1 mm in jo najbolj zasledimo na Sabotinu, medtem ko je imela proti Nanosu že manj{i obseg, le del conia- santonijsko-campanijski Lipi{ki formaciji pa se cija (Jež, 2011). Na Krasu te vrzeli ne opazujemo. pojavlja Tomajski apnenec (Jurkov{ek et al., 1996; Druga emerzijska faza je imela ve~ji ~asovni raz- Jurkov{ek, 2008, 2010). Po strukturi je Komenski pon, ponekod na Krasu precej manj{i obseg med apnenec biomikriten in biopelmikriten, pogosto z campanijem in maastrichtijem, proti jugu (Matar- milimetrsko laminacijo. Odlagal se je v plitvih za- sko podolje, Istra) pa je okopnitev obstajala že od prtih lagunah z anaerobnimi pogoji in z medplim- santonija pa vse do eocena (Drobne, 1979; Buser, skimi ravnicami. Te prepoznamo po natrganih 1980; Jurkov{ek et al.,1996; Otoni~ar, 2006, 2007; laminah (»flat pebble conglomerate«), stromato- Jež, 2011). Rezultat emerzijskih faz in zakraseva- litih in izsu{itvenih porah. Mikrofosilna združba nja so žepi boksitne gline. je skromna in nezna~ilna (foraminifere, ostrako- Na Trža{ko-komenski planoti so znotraj celot di, alge – predvsem Thaumatoporella parvovesi- nega zgornjekrednega zaporedja posebnost ~rni culifera), na ob~asno povezavo lagun z odprtim plo{~asti in bituminozni apnenci z rožencem, v morjem pa sklepamo po prisotnosti pelagi~nih literaturi poznani kot »komenski ribji skrilavci«, fosilov. Poleg rib so v apnencu prisotni {e drugi saj vsebujejo lokalno {tevilne fosilne ostanke rib makrofosili, kot so kopenske rastline, sakokome, (Gorjanovi}-Kramberger, 1895; Jurkov{ek et al., amoniti in drugi (Jurkov{ek & Kolar-Jurkov{ek, 1996: Jurkov{ek, 2010; Cavin et al., 2000; Palci et 1995, 2007; Dobruskina et al., 1999; Summesber- al., 2008). Prvotno so bili ti apnenci vezani na tri ger et al., 1996, 1999). Tomajski apnenec vsebuje horizonte znotraj albijsko-cenomanijskega, turo- tudi plasti biokalkarenita, ki kažejo ve~krat po- nijskega in senonijskega zaporedja (Buser, 1968), stopno zrnavost. Kalkarenit naj bi se odlagal kot novej{e raziskave pa so pokazale, da je takih ho- alodapi~ni apnenec v lokalnih poglobitvah zno- rizontov precej ve~. V intervalu od cenomanija traj anoksi~nih bazenov (Ogorelec et al., 1987). do santonija pripadajo Komenskemu apnencu, v Kljub ~rni barvi in vonju po bitumnu vsebuje Komenski apnenec skromen delež organskega C, ve~ji del do 0,8 % in le izjemoma do 1,7 %. Za njegovo naftno potencialnost je neugodna sestava organske snovi, saj je pretežno terestri~nega izvora (Ogorelec et al., 1996a, b). Kredno obdobje zaklju~ujejo apnenci Liburnij ske formacije, katera se nadaljuje {e v spodnji paleocen. Biosparitni rudistni apnenec se menjava z biomikritnimi razli~ki in mestoma s stromatolitnimi plastmi, haraceje pa kažejo na sedimentacijo v braki~nem palustrinskem okolju. V spodnjem delu Liburnijske formacije, ki jo ozna~ujejo Vremske plasti in je {e maastrichtijske starosti, je najbolj zna~ilna foraminifera Rhapydionina liburnica, ki jo spremljajo {e miliolide, rizokodiji, ostrakodi in moluski, predvsem giroplevre (Drobne, 1981; Dobro ohranjen skelet ribe Coelodus vetteri iz Komenske- Drobne et al., 1989,1995; Pleni~ar et al., 1992; ga apnenca. Zgornja kreda – coniacij, santonij. Komen (iz Hötzl & Pavlovec, 1979). Mestoma se v tem facie- Gorjanovi}-Kramberger, 1895). Dolžina ribe 23 cm Well preserved fish skeleton of Coelodus vetteri from Komen su pojavljajo tudi tanj{i sloji premoga, katerega so limestone. Upper Cretaceous–Coniacian, Santonian. Komen pred ~asom {e odkopavali (Vremski Britof, Lipica, (from Gorjanovi}-Kramberger, 1895). Lenght of sample 23 cm Se~ovlje; Hamrla, 1959). Mikrofacies mezozojskih karbonatnih kamnin Slovenije 31

Kredno-terciarna (K/T) meja je v Sloveniji – laporasti apnenci tipa »scaglia« albijske do razpoznavna na Krasu, kjer je bila raziskana v turonijske in »senonijske« starosti ter ve~ profilih, pri Dolenji vasi D( robne et al., 1988, – Vol~anski apnenec »senonijske« starosti. 1989, 1995, 1996, 2009), na Sopadi pri Štorjah Najstarej{e kredne plasti globljemorskega raz (Ogorelec et al., 2007), Kozini (Delvalle & Bu- voja pripadajo belemu mikritnemu apnencu tipa ser, 1990) in ^ebulovici (Ogorelec et al., 2001). »biancone« (mudstone in wackestone) z gomolji Na italijanski strani je raziskana pri Padri~ah roženca, ki predstavlja nadaljevanje sedimenta- (Padriciano, Brazzati et al., 1996) in pri Bazovi- cije iz vrhnjega dela jure. Gre za zgornji del 100 ci (Basovizza, Riccamboni, 2005). Njena geolo{ka do 250 metrov debelega paketa apnenca, kate- posebnost je v tem, da je razvita v plitvomorskem remu berriasijsko in spodnjevalanginijsko sta- faciesu, kar je posebnost in enkratnost v celotnem rost dolo~ajo kalpionele (Calpionella elliptica, mediteranskem prostoru. C. alpina, Tintinopsella hungarica) in radiolariji Meja poteka znotraj 0,2 do 2 metra debele emer- (Pleni~ar, 1979, 2009; Šribar, 1981; Buser, 1986). zijske bre~e, ki je nastala v medplimskem okolju Na prostoru Slovenskega bazena iz obdobja zaprte lagune, za katerega so zna~ilne izsu{itvene od valanginija do barremija zaenkrat niso zna- pore, strukture rizokodijev (Paronipora sp.), stro- ni nikakr{ni sedimenti, tako da pri~enja sedi- matolitne lamine in žepi boksita (Jurkov{ek et al., mentacija transgresijsko na plasteh »biancone« 1996; Ogorelec et al., 2007; Drobne et al., 2009). apnenca s fli{em {ele v aptiju, medtem ko pri~enja Apnenec tik pod mejo je svetel biomikrit in pel- sedimentacija fli{a in vmesnih apnen~evih bre~ mikrit (wackestone in packstone), ponekod pa v okolici Bohinja že v valanginiju (Budkovi~, rahlo laporast in temen biomikrit z giroplevrami 1978; Buser, 1986), njihova sedimentacija pa je in foraminiferami (Drobne et al., 1995; Pugliese trajala do konca spodnje krede. Starost tega fli{a et al., 1995). Biomikritni apnenec prevladuje tik je dolo~ena z nanoplanktonom (Buser & Pav{i~, nad mejo v spodnjem daniju in kaže vse znake 1978; Pav{i~ & Gori~an, 1987; Pav{i~, 1994). palustrinskega faciesa (Otoni~ar & Ko{ir, 1998; V spodnjem delu zgornje krede, cenomaniju Ogorelec et al., 2001; Ko{ir, 2004). Meja je poleg in turoniju, so se na {ir{em Tolminskem odlaga- spremembe biote zaznamovana tudi s spremem- li rde~kasti plo{~asti in laporasti apnenci, ki se bo izotopske sestave apnenca (izjemna, do 8 ‰ 13 menjavajo z laporji, polami rožencev in s kalka- obogatitev z lahkim izotopom δ C prav na meji, reniti, formacija pa je znana kot »pisana scaglia« Dolenec et al., 1995; Ogorelec et al., 1995, 2007), (Buser, 1986b). Na {ir{em obmo~ju Mangarta povi{ano vsebnostjo iridija (Hansen et al., 1995) se tovrstni sedimenti javljajo že v albiju (Šmuc, in prisotnostjo steklenih sferul (Gregori~ et al., 2005). Starost teh plasti je dolo~ena z nanoplank- 1998). tonom (Pav{i~, 1979) in globotrunkanami (Glo botruncana helvetica, G. schneegansi, G. sigali; Globljemorski razvoj krede Buser, 1986b). Pisani »scaglii« sledi od 100 do najve~ 300 me- Globljemorski razvoj sedimentnih kamnin se trov debela formacija Vol~anskega apnenca. Za je nadaljeval iz jure v kredno obdobje na pro- ta apnenec je zna~ilno menjavanje tankih plasti storu Slovenskega bazena, ki se je v tem ~asu {e biomikrita, kalcirudita in kalkarenita, vmes pa bolj raz{iril proti severu. Za to globlje okolje je so pogoste pole in gomolji roženca. Kalciruditne zna~ilen klasti~ni razvoj, predvsem fli{ z vmes- plasti pogosto kažejo postopno zrnavost in lami- leni ar nimi apnen~evimi bre~ami (P ~ , 1979, nacijo (Ogorelec et al., 1976). Plasti so se odlagale 2009). Fli{ se pojavlja v dveh debelej{ih pake- s turbiditnimi tokovi na obrobju bazena, biomi- tih – kot spodnja fli{na formacija, debela 100 do 400 metrov v aptiju in albiju (Cousin, 1970) ter kot zgornja, do 800 metrov debela fli{na formacija v zgornji kredi (Buser, 1986). Izvorni material za karbonatne bre~e so bili plitvomorski apnenci, ki so se trgali z roba Dinarske platforme in plazeli po pregibu, fli{ pa se je sedimentiral s severoza- hoda (Ogorelec, 1970; Ku{~er et al., 1974). Celot na debelina globljemorskega krednega zaporedja zna{a med 500 in preko 1000 metri, najbolj celo- vito pa so te plasti razvite v Slovenskem bazenu na Tolminskem (Buser, 1986a,b) in v vzhodnih Posavskih gubah, med Kr{kim in Gorjanci, medtem ko se v osrednji Sloveniji pojavljajo bolj frag mentarno. S stali{~a karbonatne sedimentologije in mikrofaciesa so znotraj krednega globljemorskega razvoja zanimivi le trije faciesi oziroma paketi Biomikritni laporasti apnenec (»scaglia«) z globotrunkanami, kamnin: radiolariji in kalcisferami. Pelagi~no okolje. Zgornja kreda – campanij. Koritnica pri Bovcu. Merilo 1 mm – beli in svetlosivi plo{~asti apnenci berriasij- Biomicritic marly limestone (»scaglia«) with globotruncanas, ske starosti, ki se nadaljujejo {e iz zgornje radiolarians and calcispheras. Pelagic environment. Upper jure, Cretaceous – Campanian. Koritnica at Bovec. Scale 1 mm 32 Bojan OGORELEC

Vzhodne Alpe

V okolici Zre~ in Stranic pri Slovenskih Ko- njicah leži med klastiti, katere sestavljajo glinavci, meljevci in laporovci ter premo{ka plast, grebenski apnenec s {tevilnimi rudisti (Pleni~ar, 1971, 1993, 2005). V laporovcih so pogoste tudi solitarne korale (Turn{ek, 1994). Razvoj teh plasti avtorji (Hamrla, 1988; Turn{ek, 1994; Pleni~ar, 1971, 2009) primerjajo z gosauskim razvojem krede v Severnih Alpah. Apnenci gosauskega faciesa v pri~ujo~i monografiji niso predstavljeni, ker niso bili zajeti v raziskave.

Zahvale Vol~anski apnenec zgornjekredne starosti (campanij – santonij). Alodapi~ni apnenec se je odlagal s turbiditnimi to- Predstavljena monografija oziroma slikovni atlas o kovi v pelagi~nem okolju. Kalkarenit s postopno zrnavostjo mikrofaciesu mezozojskih karbonatnih kamnin Slove- prehaja navzgor v mikritni apnenec. Doblar v So{ki dolini. nije je rezultat avtorjevega ve~ desetletnega terenskega Merilo 2 cm dela ter mikroskopskih raziskav apnencev in dolomi- Vol~e limestone of Upper Cretaceous age (Campanian – Santo- tov. Foraminifere in alge, ki se pojavljajo v {tevilnih nian). Allodapic limestone deposited by turbidites in pelagic vzorcih, je dolo~ila kolegica Ljudmila Šribar, ve~ vzor- environment. Calcarenite with graded bedding passing into cev koral, hidrozojev in spongij pa mi je prijazno po- micritic mudstone. Doblar in So~a valley. Scale 2 cm sredovala akademi~arka dr. Dragica Turn{ek. Obema velja iskrena zahvala. kritne pole tipa mudstone pa so produkt mirnih Atlas bi bil vsebinsko zagotovo bolj okrnjen, ~e pelagi~nih faz. Vol~anski apnenec tako lahko avtorju pri izbiri golic in stratimetrijskih profilov ne prepoznamo kot karbonatni fli{ ali alodapi~ni bi pomagali terenski geologi Geolo{kega zavoda Slo- apnenec. Avtohtoni fosili so pelagi~ni, predvsem venije. Za to sodelavo se prisr~no zahvaljujem da- globotrunkane in radiolariji, med naplavljenimi nes žal pokojnima prof. dr. Stanku Buserju in Karlu drobci pa se javljajo tudi odlomki rudistnih lupin, Gradu, nadalje dr. Bogdanu Jurkov{ku, Sa{i Orehek, dr. Ladislavu Placerju, mag. Bogoljubu Ani~i}u, Mar ehinodermov in drugih {koljk. Med globotrun- tinu Tomanu, Uro{u Premruju, dr. Stevu Dozetu, Ma kanami so najbolj pogoste Globotruncana arca, tevžu Dem{arju, doc. dr. Dragomirju Skabernetu, enako G. calcarata, G. conica, G. elevata in G. lineia- prof. dr. Jožetu ^arju z ljubljanske Univerze, kolegoma na lineiana (dolo~ila L. Šribar, v Ogorelec et al., iz rudnika Mežica Janku Ku{eju in Mihi Pungartniku 1976), ki so raz{irjene od zgornjega turonija do ter prof. dr. Romanu Kochu z Univerze v Erlangenu. Za campanija. Severno od Kobarida prehaja oziro- njihovo strokovno pomo~, diskusije in nasvete se jim ma nadome{~a Vol~anski apnenec rde~ laporast lepo zahvaljujem. apnenec tipa scaglia (Ogorelec, 1970; Ku{~er et Posebna zahvala velja tudi žal že pokojnemu An- dreju Stoparju, ki je vseskozi sodeloval z izdelavo ve~ al., 1974; Buser, 1986b; Šmuc, 2005), znan kot »scaglia rossa«, ki vsebuje poleg tistih globotrun- tiso~ mikroskopskih preparatov. V zadnjih letih se mu je pri izdelavi zbruskov pridružil Mladen Štumergar. kan, ki nastopajo v Vol~anskem apnencu, {e druge Celotna ra~unalni{ka obdelava slik in tabel je delo njihove vrste (Radoi~i} & Buser, 2004). Staneta Zakraj{ka, pri kon~ni pripravi monografije pa Nad Vol~anskim apnencem in rde~o scaglio so sodelovali {e Bernarda Bole, dr. Matevž Novak, dr. nastopa zopet do 600 metrov debel paket fli{nih Jernej Jež in Luka Gale. Prav lepa hvala tudi ostalim plasti. V kosih debelozrnate fli{ne bre~e senonij- neimenovanim, ki so kakorkoli pripomogli k izidu te ske starosti, ki leži nad Vol~anskim apnencem, publikacije. Hvala tudi ženi Heleni za njeno vzpodbu- so bile na Banj{ki planoti dolo~ene {tevilne ko- do in potrpežljivost pri mojem delu. rale (Turn{ek & Buser, 1976). Fli{ni bazen se je Za angle{ki prevod se lepo zahvaljujem prof. dr. Si od campanija dalje postopno pomikal ~edalje bolj monu Pircu, dr. Bogdanu Jurkov{ku, prof. dr. Jožetu proti jugu, na Gori{ka Brda, na Trža{ko ozemlje ^arju in dr. Matevžu Novaku pa za strokovno recenzijo tega dela in {tevilne nasvete, ki so privedli k izbolj{avi in v Istro (Buser, 1986b). in uravnoteženosti besedila in slikovnega gradiva. Veli- ka ve~ina vzorcev je bila raziskana v okviru programov in projektov, ki jih je financirala Javna agencija za ra ziskovalno dejavnost Republike Slovenije, Geolo{kemu zavodu Slovenije in Uredni{tvu Geologije pa se zahvaljujem za vso podporo pri realizaciji monografije. Mikrofacies mezozojskih karbonatnih kamnin Slovenije 33

Microfacies of Mesozoic Carbonate Rocks of Slovenia

At the 50th anniversary of publishing of car- Mežica lead and zinc deposit, further with deep bonate rocks classification (Folk 1962, Dunham geothermal and oil drilling, with quarries, tun- 1962, Ham (ed.) 1962). nels and road cuts, and more recently within research associated with the new Formation geologic map of Slovenia at the scales of 1 : 50,000 INTRODUCTION and 1 : 25,000. The focus and main object of the present mono Carbonate rocks of Mesozoic age constitute graph is, as indicated by its title, the microfacies. about 40 % of Slovenia's surface (Buser & Komac, Whereas the term facies has a long history, having 2002). In this more than 5000 meters thick suc- been introduced to geology as one of the most im- cession of limestones and dolomites, only locally portant conceptions in the first half of nineteenth interrupted by clastic deposits, volcanites and century by Gressly (1838), the term microfacies pyroclastics, almost all facial developments cha is rather new, about hundred years younger. The racteristic of shallow water carbonate environ- first researcher to propose it for the appearance ments as well as those of deeper seas and oceans of rock in thin-section under the microscope was can be recognized. In a small area the entire suc- Brown in 1943. Later this term got rooted among cession of carbonate rocks can be encountered geologists and it became widespread, especially over a stratigraphic range from Devonian to Qua- after the world oil congress in Paris in 1951, much ternary. Responsible for this diversity is to a large thanks to Cuvillier (1952, 1961). At present the extent the position of the Slovenian territory on term microfacies denotes all sedimentary-petro- the contact of three vast geotectonic units – Alps, graphic and paleontologic characteristics within Dinarides and Pannonian basin. As a result of the microscopic scale of the thin-section. It is intense tectonic activity, various developments principally associated with the carbonate rocks of individual formations can appear in contact – limestones and dolomites. Later major con- along faults and overthrusts, and therefore lateral tributions to the global knowledge of microfa- transitions between different sedimentary envi- cies were supplied by Carozzi (1960, 1989), Folk ronments are often not observable. Our territory (1962) and Dunham (1962), the latter two by their is by all means a true »little collection« of various classifications of carbonate rocks, Ham (ed.,1962) Mesozoic rocks developments in realm of the an- and Bathurst (1971), and especially by Flügel cient western Tethys. (1978, 1982, 2004) who systematically reviewed Although this is not evident from the title of all former aspects of microfacies and research the present publication, the assembled materials methods, presented new perspectives on practi- exceed the frames of Mesozoic, since also Upper cal relevance of microfacial examination of car- Permian limestones and dolomites are included. bonate rocks. His overview is richly documented The reason for their consideration in this publi- by photographs of characteristic fossils through cation is that by them the continuous carbonate microscope. Wilson (1975) on the basis of Flügel's sedimentation began on the integral Slovenian ideas from 1972 introduced into practice the con- platform, that comprised the entire Slovenian cept of standard microfacies (SMF – Standard territory, and existed from the Upper Permian to Microfacies Type), founded on 24 basic types of the middle of Anisian (Buser, 1989). microfacies and nine characteristic environments The author was led to writing this monograph of carbonate rock formation. Wilson's classifi- by the wish to present the results of microfacial cation has met with a most favorable reception analyses of several decades of research of lime- in oil geology and computer modelling of sedi- stones and dolomites from the Slovenian territory. mentary rocks. Sedimentary environments and This research was initially performed mostly in carbonate rocks modelling have been the object the frame of elaborating the Basic Geologic Map of intense research next to the above mentioned of SFR Yugoslavia at the scale of 1 : 100,000 that authors also by Milliman (1974), Reading (1978), lasted 25 years all to its conclusion in 1989, and James (1979), Scholle et al. (eds.,1983), Tucker & further within the project Mesozoic in Slovenia Wright (1990), Bosellini (1991), James & Kendall active in the eighties of former century, and more (1992), Einsele (1992) Elf-Aquitaine (1975), AGIP recently within a number of geologic projects in (1988) and others. frame of the national research programme of the In Slovenia the concept of microfacies ap- Public agency for research activity of Republic peared relatively early, having been mentioned Slovenia. An appreciable amount of data resulted already in 1961 by E. Flügel and A. Ramov{ in from various applied research, such as that con- description of the Upper Triassic Dachstein lime- nected with the Idrija mercury deposit and the stone from Mt. Begunj{~ica. Emphasis in that pa- 34 Bojan OGORELEC per was on description of fossil flora and fauna, (Ogorelec et al., 1996), and on their isotopic com- and comparison with equivalent limestone from position (Ogorelec et al., 1999b). the Northern Alps. Unfortunately this publica- The basic goal of the present publication is tion was not documented with illustrations. twofold. Principally it is destined to foreign re- In 1966 Rajka Radoi~i} published at that time searchers, to introduce them our carbonate rocks an excellent and richly illustrated voluminous and their comparison with those of neighboring treatise on microfacies of Jurassic beds in the Di- territories, and to geology students who for the narides which comprises also descriptions and first time encounter the notion of microfacies. It figures of several limestone samples from south- should be useful also to others, as the concep- ern Slovenia. tion of microfacies linking sedimentologists with After this start in microfacial studies of car- paleontologists, regional geologists and tectoni bonate rocks in Slovenia a ten years long inter- tians. To enable a better understanding of the mission followed. In those times limestones were materials, in the introductory part a summarized an object of largely paleontologic analyses and lithological description of the entire succession of stratigraphic determinations in the frame of map- Mesozoic rocks in Slovenia is given. ping for the Basic Geological Map of Yugoslavia. As to contents, the materials are presented ac- A strong impulse to sedimentology and with it cording to geological time with the main accent also to microfacial research was given in the times of publication put on figures with 250 photo- after 1973, when the project Mesozoic in Slovenia graphs of microscope thin-sections. The introduc- was started. In its frame started systematic inte- tory text, completed with additional lithologic gral research of Triassic, Jurassic and Cretaceous columns and references, serves only as a neces- s that was focused mainly in limestones and do- sary framework for putting the rocks in proper lomites. This kind of investigations, formally un- time and space. The foreign references are re- der different titles within the frame of various duced to a minimum, and they are intended pri- projects continued , so that over 25,000 thin-sec- marily to students to enable them comparisons of tions were made and examined at the Geological carbonate rocks from Slovenia with those of the Survey of Slovenia. They have served as a basis neighboring Alpine and Dinaric regions. and material for the present publication. Since the issuing of this publication coincides The collected material comprises only the mi- with the 50th anniversary of a very important crofacies as recognized in thin-sections of lime- event for the carbonate sedimentology, the pub- stones and dolomites of Slovenian territory. Ma lication of one of the basic texts on petrography crofossils and isolated microflora and microfauna of limestones and dolomites – of Classification of (e.g. radiolarians, conodonts, nanoplankton, pol- carbonate rocks (Ham, 1962), the author in this len and others) are therefore not contained in the way joins to the celebration of this jubilee. illustrative materials nor in the references. The majority of papers and publications issued in the sixties and seventies of the former century is con- A SHORT SUMMARY OF LITHOLOGY cerned with lithology, paleontology, regional de- AND CARBONATE ROCK velopments or stratigraphy of Mesozoic carbona DEVELOPMENT IN SLOVENIA te rocks in Slovenia. This is especially true for the explanatory notes to individual sheets of the Ba- After the deposition of continental clastic sic Geological Map 1 : 100,000. Sedimentology is rocks an extensive transgression of the sea in more extensively represented in the explanatory Upper Permian covered the territory of Slovenia notes to the more recent geologic maps at scales with carbonate rocks. The area was from Upper of 1 : 50,000 (Jurkov{ek et al., 1996) and 1 : 25,000 Permian to middle of Anisian a constituting part (Jurkov{ek, 2010; ^ar, 2010) as well as in the pub- of an uniform shallow carbonate platform, known lication Geological development in Slovenia and as the Slovenian platform (Buser, 1989) that ex- Croatia – Guidebook issued for the 16th European tended farther to Friuli, Istria and the Pannonian Micropaleontological Congress (Drobne, 1979). A basin region. In the Middle Anisian this platform complete listing of references for biostratigraphy disintegrated into the Dinaric carbonate platform and lithology of Upper Permian and Mesozoic in the south and the Julian carbonate platform in rocks appears also in The Geology of Slovenia the north, separated by the Slovenian basin (Cou (Pleni~ar, Ogorelec & Novak, 2009) in chapters sin, 1973; Buser, 1989). Carbonate sedimentation covering the Upper Permian (Skaberne et al., on these two platforms to greater or lesser extent 2009), Triassic (Dozet & Buser, 2009), Jurassic continued all to the Upper Cretaceous when the (Buser & Dozet, 2009) and Cretaceous (Pleni~ar, Dinaric carbonate platform disintegrated with 2009), while a succint overview of geologic deve forming of several intermediate flysch basins. lopments in individual geotectonic units appears On figure 2 the lithologic development of in works by S. Buser (1979a,b), P. Mio~ (2003) and Upper Permian and Mesozoic carbonate rocks U. Premru (2005). When considering facies of car- in Slovenija is shown in individual paleogeo- bonate rocks also several summary contributions graphic units – the Dinaric and Julian carbona- should be mentioned, on their facial developments te platforms, in the Slovenian basin, and sepa- (Pleni~ar & Pavlovec, 1984), facial characteristics rately in the actual Northern Karavanke Mts., (Pleni~ar & Premru, 1975), on these rocks as po- an area north of the Periadriatic lineament. On tential source rocks for genesis of hydrocarbons Fig. 3 schematic overview of corresponding sedi- Mikrofacies mezozojskih karbonatnih kamnin Slovenije 35 mentary environments is shown. Owing to strong and for sabkhas cellular dolomites and evapori tectonics and resulting nappe structure of Slove- tic minerals, of which gypsum and anhydrite are nian territory the relationships between indivi present. dual lithologic units and geologic formations can In the biomicritic limestone foraminifers be shown only schematically. (Agathamina sp., Glomospira sp., Hemigordius Lately new terms are used as approximate sp., Reichelina sp., Climacammina sp., Geinitzina synonyms for the Dinaric carbonate platform, sp., Ammovertella sp., Ichtyolaria sp., Staffella such as: Platform of the Outer Dinarides (Grandi} sp.), skeletal algae Gymnocodium bellerophontis, et al., 1999), Adriatic-Dinaric carbonate platform Vermiporella nipponica, Permocalculus fragilis, (Gu{i} & Jelaska 1993), or simply Adriatic car- Velebitella triplicata, Mizzia velebitana, M. cor- bonate platform (Gu{i} & Jelaska, 1990, Veli} et nuta), brachiopods, echinoderms and gastropods al., 2002; Vlahovi} et al., 2005; Jež, 2011) in re- (Bellerophon sp.) occur, locally also smaller patch spect that it was the broadest carbonate platform reefs with coral species Waagenophyllum indi- on the Adriatic microplate in Jurassic and Creta- cum (Ramov{, 1958, 1986a; Buser et al. 1988; Ska- ceous. However, in this monograph an »old« term berne et al., 2009). Dinaric carbonat platform is still used. The Permian-Triassic (P/T) boundary is mar In the following very condensed descriptions ked by a sudden disappearance of numerous fos- of lithology in particular geologic times are given sil species, especially of algae and foraminifers, with emphasis on carbonate formations and their and by a change of carbon isotopic composition microfacial and diagenetic characteristics. Since in limestones and dolomites. The Lower Triassic the Triassic beds are the most widespread in Slo- carbonates are enriched with the up to 5 ‰ ligh- venia and also of the highest diversity, the most ter carbon isotope with respect to the Upper Per- space in monography is devoted to them. mian ones (Dolenec T. et al., 1995, 1999a, b, c, 2004). Just below the P/T boundary in places a thin- UPPER PERMIAN ner bed of oolitic limestone appears (Dolenec, M. & Ogorelec, 2001; Dolenec M., 2004) that can Upper Permian beds in Slovenia are repre- be compared with the Tesero horizon in the Alps sented with carbonate rocks. Their lithology is di- (Assereto et al., 1972). Paleontologically the P/T verse. In western part of the Sava folds, between boundary in Slovenia was proved lately on ba- Ljubljana, Škofja Loka and Idrija, they attain a sis of the conodont zonation (Kolar-Jurkov{ek thickness of up to 250 meters. Bedded, dark grey & Jurkov{ek, 2007; Kolar-Jurkov{ek et al., 2011) to black limestone and marly limestone prevail and foraminifers (Nestell et al., 2011). Just above over dolomite with several thin sheets of inter- the Permian/Triassic (P/T) boundary the charac- calated shaly marlstone. They are named after teristic small foraminifer Earlandia occurs. the town of Žažar near Vrhnika the Žažar For- Among the diagenetic processes affecting the mation (Ramov{, 1958), which is an equivalent of Upper Permian carbonate rocks, dolomitization the Bellerophon Formation in the Alps (Heritsch, has by far the larges extent, and to a lesser extent 1934; Buser et al., 1988; Kolar-Jurkov{ek et al., silificication and dedolomitization are present 2011). In the eastern part of Sava folds, at La{ko, also. As a result of dedolomitization in beds with Izlake, Sevnica and on Mt. Bohor, the Upper Per- evaporitic minerals epsomite precipitated, which mian beds are just a few tens of meters thick, and can be observed in the Idrija mercury mine. occurring in a prevailingly dolomitic develop- The major part of dolomite is of early diage- ment. In the basal beds, just above the clastics netic origin, and it formed according to the eva of the Gröden (Val Gardena) formation, the lime- poritic model of dolomitization (Shinn & Gins- stone and dolomite still contain appreciable ter- burg, 1964). Aridic climate in Upper Permian is rigenous admixture, mostly of quartz and mica. indicated next to gypsum and anhydrite also by Limestone in general is extraordinarily rich with isotopic analyses of δ18O (Pol{ak & Pezdi~, 1978; fossils, especially skeletal algae, echinoderms and Dolenec et al., 1981; Ogorelec et al., 1999b) and foraminifers. The proportion of carbonate in the Na+ contents that are high for carbonates (Ogore- limestone varies between 85 and 97 %. lec & Rothe, 1979). In Southern Karavanke Mts. the Upper Per Owing to specific sedimentary conditions and mian succession occurs in a dolomitic develop- climate, the time of Upper Permian was favora- ment as the Karavanke Formation, which is up ble for formation of stratiform lead and zinc de- to 300 meters thick (Buser et al., 1988). For the posits. Such deposits are abundant in the eastern lower part of this formation also an up to 80 m Sava folds, namely in the upper part of the Upper thick horizon of cellular dolomite (Rauhwacke) is Permian sequence (Puharje near Šo{tanj, Iskra, characteristical. 1969) and at the boundary between the Upper The sedimentary environment of Upper Per- Permian and Lower Triassic (Mokronog, Bohor, mian beds was a very shallow and restricted shelf Ledina near Sevnica, Drovenik et al., 1980). with lagoons and sabkhas, connected to the wider The Upper Permian beds in Slovenia have in region of Tethys. This is indicated by the uni- general the same or very similar microfacies as the form flora and fauna of the Indo-Armenian type. limestones and dolomites of same age in neigh- Characteristic for the restricted shelf and lagoons bouring areas, e.g. in the Carnic Alps (Buggisch, are varieties of the algal biomicritic packstone, 1974; Buggisch et al., 1976; Holser & Schön- 36 Bojan OGORELEC laub, 1991; Magaritz & Holser, 1991; Noé, 1987), alternate with oolitic layers that are especially Dolomites (Bosellini & Hardie, 1973), on Mt. distinctive in the field. Dolomites and limestones Velebit (Kochansky-Devidé, 1979; Sremac, 1991, have a sandy appearance owing to admixture of 2005) and in Hungary (Haas, 2001; Haas et al., terrigenous quartz and mica. The non-carbonate 2004, 2006). component locally attains as much as 50 %. Clas- tites are represented by reddish claystones, marlstones and siltstones. As to texture, the limestone TRIASSIC is mostly biomicrite or pelmicrite. It was depo sited in a very shallow restricted part of shelf that Triassic rocks are in Slovenia the most abun- possessed at times characteristics of lagoons and dant of all, covering almost a quarter of its ter- littoral. It is often entirely or partly dolomitized, ritory, and their total thickness attains up to and bioturbation structural features are also 3800 meters (Buser, 1979), with carbonate rocks typical. Thinner lenses and nests of gypsum and decidedly predominating over clastic and pyro- anhydrite indicate local and periodic evaporitic clastic rock types (Fig. 2). They are distinguished conditions of sedimentation. by an extraordinary diversity of lithologies with Oolites formed in intertidal channels and del- characteristics of Alpine development within the tas with higher energy index. Characteristic is Tethys which is similar or identical to that known their reddish color resulting from hematitic pig- in the Northern Alps). ment. Nuclei of ooids were often subjected to late In Lower Triassic the carbonate sedimenta- diagenetic dolomitization manifested by up to tion on shallow shelf was accompanied by sup- 300 μm large dolomitic rhombohedrons. Between ply of terrigenous, largely fine-grained terrestrial ooids occur often plates of echinoderms and tiny material, while in Lower Anisian the carbonates gastropod shells of Natica gregaria and Holopella completely prevail. End of Anisian (Buser, 1989), gracilior species, and also fine terrigenous grains in the Idrija area already in Middle Anisian (^ar, of quartz and mica. 1985, 2010), the Slovenian platform started to dif- In the upper part of the Lower Triassic suc- ferentiate as a result of intense tectonics, into the cession terrigenous content decreases. A darker Dinaic carbonate platform in the south, the Julian biomicritic or pelmicritic marly limestone (mud- carbonate platform in the south, and the interme- stone to packstone) prevails over the lighter diate Slovenian basin (Fig. 6). The latter persisted colored dolomite. Among fossils foraminifers, and in the central Slovenian region all to the middle in certain beds also abundant ostracods, echino- of Jurassic period when it extended also to the derm plates and thin valves of species Claraia Julian carbonate platform territory, while toward clarai are represented. Some conodonts are pre- the Dinaric carbonate platform it existed till the sent too (Kolar-Jurkov{ek & Jurkov{ek, 1995, end of Cretaceous. 1996, 2007). The most important for stratigraphy More detailed descriptions of paleogeographic is foraminifer Meandrospira pusilla. development inTriassic on the integral Slovenian North of the Periadriatic lineament, especially territory, of paleotectonics and biostratigraphic in surroundings of ^rna na Koro{kem, the Lower subdivisions are found above all in the works by Triassic beds appear in an clastic development, Buser, 1979, 1980b, 1988, 1996; Dozet & Buser, in respect that the region of the Northern Kara- 2009; Premru, 1980, 1982, 2005; Buser et al., 2007, vanke Mts. is a part of the Eastern Alpine geo- 2008, and Placer, 2009. tectonic unit. They are developed as sandstones, A recent example of how this paleogeograp shaly siltstones and conglomerates of the Bunt- hic region in Slovenia might look like in Triassic sandstein type (Mio~, 1983), and they contain no time is given by the Bahamas archipelago (Fig. 7) fossil remains (Štrucl, 1971). where the unique very shallow carbonate plain Lower Triassic beds on the Slovenian terri- is split by the up to 900 meters deep trench, the tory generally display the same, or a very similar Tongue of the Ocean. By the dimension of several microfacies to beds of same age in neighbour- hundred kilometers' this trench is comparable ing areas, e.g. the Werfen beds in Northern Alps with the size of the ancient Slovenian basin. (Mostler & Rössner, 1984), in Carnic Alps (Hol- In Fig. 8 a schematic presentation of lithologic ser & Schönlaub, 1991), Dolomites (Assereto et development of the Triassic rocks in Slovenia is al., 1972), Hungary (Nagy, 1968; Haas, 2001), in given with selected stratigraphic columns. Austrian part of Southern Karavanke Mts. (An- derle, 1970), at Mt. Svilaja in Dalmatian Zagora (Š~avni~ar et al., 1983, Jelaska et al., 2003) and LOWER TRIASSIC (Induan and Olenekian) elsewhere, which indicates a vast and uniform sedimentary environment in the Lower Triassic. 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 MIDDLE TRIASSIC Southern Karavanke Mts. (Buser, 1980a). In the entire Slovenian region south of the Periadriatic Development of Anisian beds in Slovenia is lineament the beds appear in a rather uniform de- rather uniform, mostly as bedded dolomite that velopment. In the lower part of sequence which is exhibits frequent indications of intertidal sedi- up to 250 meters thick clastic and carbonate beds mentation with stromatolites and shrinkage pores Mikrofacies mezozojskih karbonatnih kamnin Slovenije 37

(Grad & Ogorelec, 1980; Dolenec et al., 1981). 2003). Important macrofossils are ammonites Limestone is less common than dolomite. Among and bivalves (Jurkov{ek, 1983, 1984; Ramov{ & fossils foraminifers (Meandrospira dinarica, Jurkov{ek, 1983; Ramov{, 1989). Pilammina densa, Glomospirella irregularis, Interesting in the Upper Ladinian of Kam- G. grandis, G. semiplana, Trochammina sp.) pre- nik-Savinja Alps is the Koro{ica Formation that vail, locally also algae (Physoporella pauciforata) overlies granular dolomite and green tuff. The occur. In northern part of Julian Alps between limestone is a slightly bituminous black biomi Mojstrana and Kranjska Gora massive reef lime- crite containing chert nodules. Among fossils bi- stone is preserved, consisting primarily of algae valves (Jurkov{ek, 1984), ammonites and fish as and thrombolitic structures (Ramov{, 1987). The well as reptile skeletons occur (Celarc, 2004a; same development is present also in the castle Celarc & Žalohar, 2010). rock wall above the Bled lake (Flügel et al., 1993). In the Northern Karavanke Mts., in Mežica Thickness of Anisian beds attains up to 600 area an over 1000 meters thick complex of mas- meters. sive, in part bedded limestone and dolomite oc- North of the Periadriatic lineament, at Topla cur in Ladinian and Cordevolian, known as the below Mt. Peca bedded dolomite is exposed which Wetterstein limestone (Štrucl, 1970, 1971). The is mineralized with lead and zinc ores (Štrucl, most characteristic such massif is the Mt. Peca 1974). It is overlain by dark micritic limestone group. The limestone is mineralized with zinc with chert nodules. and lead ores (Štrucl, 1971, 1984; Brigo et al., In the middle of Anisian the Slovenian plat- 1977; Drovenik et al., 1980). The lower part of form begun to disintegrate. As a result the sedi- Wetterstein Formation is more massive, and in- mentation from Middle Triassic on took place on cludes reef limestones with corals and chaetetides separate geotectonic units in different environ- (Turn{ek, 1997; Bole, 2002), whereas its upper ments. For the deeper marine development of part, already of Cordevolian age, was deposited Anisian as known in Karavanke Mts. near Trži~, largely in intratidal zone of an open shelf. The in Idrija area and in eastern Sava folds ammo- rocks contain frequent stromatolitic and loferi nites (Balatonites balatonicus, Buser, 1979a) and tic beds. Southwards the Wetterstein limestone conodonts (Kolar-Jurkov{ek, 1983, 1991) are passes into dark mudstones and marlstones with characteristic. rare limestone interbeds. These beds, known as Ladinian beds are distinguished by a highly the Partnach Formation, were sedimented in a diverse lithology of various rapidly alternating restricted, somewhat deeper part of shelf. In this lithologic types. They are exposed in a number packet locally also lenses and nodules of evapori of localities in central Slovenia, in broader Idrija tic minerals, mostly gypsum occur (Štrucl, 1971; and Cerkno areas, in foothills of Julian Alps and Mio~, 1973). Karavanke Mts., and in a larger extent north of the Periadriatic lineament in the Peca mountains. As a result of intense tectonics during the UPPER TRIASSIC Idrija tectonic phase (Buser, 1980b) the territory of central Slovenia became drastically dismem- Carnian beds are the most abundant in west- bered. In deeper trenches volcanic effusions of ern Slovenia. Within them stratigraphically the spilitic-keratophyric association (basalts, quartz Cordevolian, Julian and Tuvalian rocks can be keratophyres, porphyries …) occurred, accom- distinguished. They occur in the shallow marine panied by deposition of their tuffs and tuffites and in deeper marine development. The entire (Buser, 1979; Dozet & Buser, 2009). Some blocks Carnian time lasted 14 million years. became subaerially exposed as indicated by thick Lately, the term Cordevolian substage is beeing beds of slope breccias and conglomerates. In abandoned (Celarc, 2004b; Lucas et al., 2010) be- Southern Karavanke Mts. and part of Julian Alps cause the fossil assemblage of these beds belongs they appear as the Ukve (Ugovizza) breccia (Bu already to the lower part of the Julian substage. ser, 1986b; Jurkov{ek, 1987), and in surroundings However, considering the distinctive, more reefal of Idrija as the Stopnik conglomerate (Mlakar, facies of massive limestone and dolomite known 1969; âr & âdež, 1977; âr & Skaberne, 2003; from lowermost Carnian in Slovenia, as well as âr, 2010). On Dinaric and Julian platforms in the traditional subdivision in the Basic Geologic some places dark limestones with chert and in- Map, Cordevolian substage is kept as a separate terbedded tuff layers deposited, and in the cen- stratigraphic unit in this monograph. tral part of Slovenian basin the Psevdozilja beds Rocks of Cordevolian age occur only in car- that are characterized by an alternation of dark bonate development, mostly as light, massive shaly claystones, sandstones and tuffs with sub- saccharoidal dolomite with primary texture of ordinate limestones. Texture of limestone is gene rock only exceptionally preserved. The fossils, rally biomicritic mudstone or wackestone, and predominantly dasycladacean algae and corals, among fossils in addition to thin mollusc shells allow the supposition that the Cordevolian dolo- especially the conodonts (Kolar-Jurkov{ek, 1983, mite represents ancient reefs that were later sub- 1991; Kolar-Jurkov{ek & Placer, 1987; Placer jected to intense dolomitization. Limestones of & Kolar-Jurkov{ek, 1990; Kolar-Jurkov{ek & this age compose the larger part of Mts. Mežakla Rižnar, 2006) and radiolarians occur (Gori~an, and Pokljuka in the Julian Alps (Ramov{, 1988; 1997; Gori~an & Buser, 1990; Skaberne et al., Ramov{ & Turn{ek, 1984; Turn{ek & Buser, 1989) 38 Bojan OGORELEC and extensive areas in Kamnik-Savinja Alps The upper parts of Julian and Tuvalian se- (Krvavec, Velika planina, Menina – Premru, 1974, quence are often represented by grey dolomite 2005; Ramov{ & Šribar, 1993; Celarc 2004a; with rare marlstone intercalations, and locally Žalohar & Celarc, 2010), whereas in smaller also with several meters thick layers of tuffaceous outcrops they appear also in the region between claystone. This dolomitic packet gradually passes Cerkno and Ljubljana and in eastern Sava folds. to lighter-colored bedded dolomite without inter- As a result of paleokarstification (Buser, 1980b) calated marly sheets, the Main dolomite. Age of the limestone is often reddish colored, and it con- this dolomite is determined by up to several cm tains pockets of red clay and bauxite. Such lime- large megalodontid bivalves, foraminifers, algae stone has been appreciated as ornamental stone. (Poikiloporella duplicata) and conodonts (Kolar- It is being extracted in quarries at Hotavlje and Jurkov{ek, 1991). Lesno Brdo near Vrhnika (Ramov{, 1995). In do- A distinct development of Julian-Tuvalian se- lomite and limestone of the mentioned areas, the quence are the Amphiclina beds, which in Cerkno most frequent fossils are skeletal algae (Diplopora area and in Ba{ka grapa attain thicknesses of up annulata, Diplopora annulatissima, Gyroporella to 250 meters (Buser, 1986b). Characteristic for ladinica), that are locally rock-forming (Ramov{, them is interbedding of dark grey to black marly 1988, 1992; Dozet, 1979; 2004; âr, 2010). biomicritic limestone, shaly marlstone, quartz A special bedded development of dolomite is sandstone and conglomerate, tuffs and tuffites. In known on the Vojsko plateau at Ga~nek, where this complex several up to 40 meters thick reefs in a 40 meters thick succession structures typical occur in the wider Cerkno area (Senowbari-Dar- for littoral intertidal environment can be found yan & Schäfer, 1979; âr et al., 1981; Turn{ek et (Mlakar, 1969; âr, 2010). al., 1984). They are mainly built of sponges and to In the region of Northern Karavanke Mts. the a lesser degree of corals (Turn{ek, 1997). Struc- sedimentation of bedded limestone and dolomite tural characteristics of limestones and graded as the top part of the Wetterstein Formation con- bedding in beds allow to interpret the sedimen- tinued in Cordevolian. tation of Amphiclina beds as taken place in the Thicknesses of Cordevolian dolomite and transitional zone of carbonate shelf toward the limestone may be very variable, from several tens Slovenian basin (Turn{ek et al., 1984). meters up to 600 meters in different geotectonic In Julian Alps the shallow- as well as the units of Slovenia. deeper-marine development of Julian and Tuva Rocks of Julian and Tuvalian substages are lian beds can be observed. The shallow marine variable, mainly carbonatically developed. With- development crops out e.g. at Tamar and Log in limestones and dolomites also layers of marl- pod Mangartom (Ogorelec et al, 1984; Jurkov{ek, stones and packages of clastites and tuffs occur. 1987). The biomicritic limestone (wackestone Their thickness varies between 100 and 400 me- to packstone) contains numerous foraminiferal ters. In the southwards direction on the Dinaric tests, small megalodontids and other bivalves, carbonate platform clastites and tuffs become echinoderm plates. It is often dolomitized, large- more and more abundand, so that in the Idrija ly marly, containing up to 15 % noncarbonate and Ko~evje areas they already prevail above the admixture, mostly clay and organic matter. For carbonates (Cigale, 1978; Dozet, 1990a). the deeper sea development dense biomicritic In contrast to Cordevolian dolomite, the Ju- limestone with chert nodules is characteristic. lian and Tuvalian beds were deposited on restric Among fauna thin-valved bivalves, calcitized ra- ted shallow shelf, often in lagoons. Dark color diolarians and washed-in plates of echinoderms of limestone and pyritic pigment indicate ano prevail (Ogorelec et al., 1984; Jurkov{ek, 1987). xic conditions in the sedimentary environment. In these beds on Kozja dnina below Mt. Triglav Limestone is often marly and locally with boudi- the fossil fish Birgeria sp. was found (Jurkov{ek & nage structural features. Organic matter content Kolar-Jurkov{ek, 1986), a worm Valvasoria car- varies around an average of 1 %, at most to 4 %, niolica (Kolar-Jurkov{ek & Jurkov{ek, 1997) and and its origin is largely terrestrial (Ogorelec et other fossils were found (Dobruskina et al., 2001; al., 1996a). According to texture the limestone is Bitner et al., 2010), while in the western part of micritic and biopelmicritic mudstone to pack- Southern Karavanke Mts. algae Clypeina besici stone. Predominant fossils are thin-valved bi- (Kolar-Jurkov{ek & Jurkov{ek, 2003) and radio- valves (Jelen, 1990; Jurkov{ek, 1994), skeletal and larians (Kolar-Jurkov{ek et al., 2005). nonskeletal algae (Poikiloporella duplicata, Cly- Julian and Tuvalian beds in Northern Kara- peina besici), ostracods and smaller foraminifers vanke Mts. are represented at Mežica with an up (Nodosaria ordinata, Glomospira sp., Diplotremi- to 350 meters thick succession of limestone and na astrofimbriata, Lamelliconus multispirus, Am- dolomite developed in 20 cyclothems of lofer type, modiscus parapriscus, Frondicularia pupiformis) for which three clastic horizons of shale, siltstone (Oblak, 2001) and bivalves of Triadomegalodon and marlstone are characteristic (Štrucl, 1970, idrianus species (âr 2010). A somewhat more 1971; Pungartnik et al., 1982). Certain beds are agitated environment is indicated by individual extremely rich with fossils, especially crinoids ooids and oncoids. Limestone was often affected (Jurkov{ek, 1978; Jurkov{ek & Kolar-Jurkov{ek, by early- as well as late-diagenetic dolomitiza- 1997; Kaim et al., 2006; Kolar-Jurkov{ek & tion and karstification with pockets and layers of Jurkov{ek, 2009, 2010; Jurkov{ek et al., 2002). A bauxites (Dozet, 1979, 2004; Buser, 1980b). rather agitated environment within the shallow Mikrofacies mezozojskih karbonatnih kamnin Slovenije 39 shelf is indicated by individual oolitic layers and lodontids, foraminifers and algae are represented. oncoids. Locally also beds and lenses with oncoids and Rocks of Norian and Rhaetian ages are repre- vadose pisoids appear (Ogorelec, 1988; Dozet, sented in Slovenia by three developments. In both 1991). Main dolomite deposited initially as lime- Julian and Dinaric carbonate platform the Main stone on very shallow restricted shelf with wide dolomite and its lateral variety, the Dachstein coastal plains, in the shallower part of shelf as limestone occur, and in Slovenian basin the Ba~a Dachstein limestone. Dolomitization was early dolomite and Železniki limestone (Fig.13). Main diagenetic according to the evaporative pump- dolomite and Dachstein limestone cover large ing model (Illing et al., 1965). Later the rock was areals, and are the most widespread rock forma- affected also by the late diagenetic dolomitiza- tions in Slovenia. They build most of the Julian tion. Dolomite also shows often indications of Alps, a large part of Notranjska, northern part of paleokarstification. Smaller and larger corrosion Trnovski gozd and part of Dolenjska. vugs are filled with zonal sparitic cement, com- The thickness of Main dolomite is between 800 monly accompanied by red internal micrite. and 1300 meters, the same as also of the Dachstein In the same time, when Dachstein limestone limestone. Limestone predominates on the Julian and Main dolomite were depositing on the plat- carbonate platform, whereas on the Dinaric platforms, the Ba~a dolomite and Železniki limestone form dolomite prevails. Thickness of the Ba~a do- were formed in the basin and on its margins (Bu lomite is 3 to 4 times smaller, and is estimated to ser, 1979; Ramov{, 1970; Gale, 2010). The carbo at most 400 meters (Buser, 1986b). nate sediment in both formations is micritic, with Dachstein limestone is thickly bedded, and it very rare fossils, i.e. small foraminifers (Roži~, occurs in the typical lofer develoment as known 2005, 2006, 2008; Roži~ & Kolar-Jurkov{ek, 2007; in the Northern Alps (Fischer, 1964; Zankl, 1971; Buser & Ogorelec, 2008; Roži~ et al., 2009; Gale Piller & Lobitzer, 1979; Piller, 1981), Dolomites et al., 2010) and conodonts (Kolar-Jurkov{ek, (Bosellini, 1967; Bosellini & Rossi, 1974) or in 1982, 1991, 2011) but characteristic for the two Hungary (Haas, 1994). Individual cyclothems formations are interbeds and nodules of chert. (Fig. 12) consist of up to 2 meters thick beds of biomicritic and biosparitic limestone which are interrupted by thin stromatolitic and loferitic JURASSIC layers, and locally also interbedded by breccias with clayey matrix. As in the Middle and Upper Triassic the ter Among fossils the most abundant are foramini ritory of Slovenia also in Jurassic belonged to fers (Triasina hantkeni, Aulotortus gr. sinuosus, three geotectonic units that at the same time A. permodiscoides, A. friedly, Miliolipora cuvil- represented distinct sedimentary environments. lieri, Galeanella sp.), algae (Macroporella retica) Southern Slovenia was a part of the Dinaric and echinoderms. In certain beds large mega- carbonate platform with typical shallow water lodontid bivalves are even rock-forming. The sedimentation and imposing thickness of car- Dachstein limestone was deposited on a shallow bonate rocks which attains in Jurassic more than open and near-shore shelf with periodic intertidal 1500 meters (Buser, 1989; Buser & Dozet, 2009). and supratidal conditions (Ogorelec, 1988; Dozet To the north the carbonate platform bordered & Ogorelec, 1990; Ogorelec & Rothe, 1992). The on the Slovenian basin, and north of it the Ju- beds deposited in littoral environment are often lian carbonate platform still existed. The latter dolomitized. disintegrated in Dogger, and was replaced by the On Julian platform larger reef massifs occur basin. within the Dachstein limestone Formation (e.g. Begunj{~ica, Pokljuka, Bohinj), and smaller reefs Dinaric carbonate platform containing a rich coral fauna (Turn{ek & Ramov{, 1987; Turn{ek & Buser, 1991; Turn{ek, 1997). The transition of Upper Triassic Main dolo- On both Dinaric and Julian carbonate platforms mite and Dachstein limestone to Jurassic beds is periodically short-term emersions of their in- not sharp. Only locally an up to several tens of dividual parts occurred. In such occasions pa meters thick package of intraformational brec- leokarst developed. It is best preserved in Kanin cia occur on the contact, which formed during Mts. and on Mt. Krn (Babi}, 1980/81; Ogorelec short-term emersion phases accompanied by & Buser, 1996). Equal fauna and microfacies as paleokarstification (Buser, 1979b; Ogorelec & found in reef limestone of Slovenian part of the Rothe, 1992; Jurkov{ek et al., 1996). Stromato- Alps occur also in Norian-Rhaetian reefs in the lites which are typical for Main dolomite gradu- Northern Alps (Zankl, 1971; Flügel, 1981; Piller, ally disappear, but frequent structural features 1981; Stanton & Flügel, 1989; Flügel & Koch, of the littoral environment – shrinkage pores and 1995; Turn{ek et al., 1999). desiccation cracks, supratidal conglomerate and Main dolomite has a monotonous, entirely laminites – still persist in the Lower Lias beds dolomitic development. Characteristic is cyclic (Ogorelec, 1988, 2009; Orehek & Ogorelec, 1979, interchanging of thicker dolosparitic and bio 1980; Dozet, 1992a, 1998). micritic beds with thinner stromatolitic layers, In Middle and Upper Lias as well as in Dog- loferites, locally also supratidal conglomerate ger various environments within the carbona and emersion breccias. Among fossils large mega- te shelf can be recognized (Buser, 1979b; Ore- 40 Bojan OGORELEC hek & Ogorelec, 1979, 1981; Strohmenger & Mt. Trnovski gozd a part of the carbonate com- Dozet, 1990, Dozet, 1992a,b). On Trnovski gozd, plex is completely dolomitized. Hru{ica, Logatec plateau and on Gorjanci Mts. sedimentation took place on the open shelf with Slovenian basin a higher energy. Oolitic limestones prevail (Buser 1973, 1978; Strohmenger et al., 1987; Ogorelec Jurassic beds in pelagic development are & Dozet, 2000) which may attain a thickness of found in the broad region of Tolmin and Bovec, several hundred meters. Within them locally la in foothills of Julian Alps and in western part yers with large oncoids appear. Locally lithiotid of Southern Karavanke Mts., and in a reduced bivalves are frequent, so that in places they form extent also in eastern part of Sava folds. coquinas (Buser, 1978; Buser & Debeljak, 1996; Lias beds, attaining a thickness of up to 300 Debeljak & Buser, 1998; Ramov{, 2000). meters, are represented by platy micritic li Among important fossils that can be observed mestone with chert nodules, intercalated with in thin-sections of Lower Jurassic – Liassic beds thin shaly marlstone layers. Among fossils fora- algae Paleodasycladus mediterraneus and Ses- minifers Ophthalmidium leischneri and Involuti- trosphaera liasina, and foraminifers Orbitopsella na liassica, radiolarians and sponges occur. Along praecursor, Involutina liassica, Agerella mar- basin margins thicker packets of calcareous tana, Trocholina turris, Pseudocyclammina lias- breccias sedimented sliding down the shelf edge sica, Haurania deserta were determined (Šribar, (Roži~, 2006, 2008; Roži~ & Popit, 2006; Buser & 1979a, and data from explanatory books to Ba- Ogorelec, 2008). Between breccia fragments also sic Geologic Map 1 : 100,000). Abundant are also ooides are found. Breccia and beds of finer cal- stratigraphically less characteristic species of carenites often display graded bedding and lami- alga Thaumatoporella parvovesiculifera, echi- nation. On Mt. Begunj{~ica platy limestones with noderms, microgastropods, bivalves, ostracods, chert are impregnated with manganese oxides, and locally also tiny brachiopods. In Dogger beds and they contain numerous ammonites. the foraminifer Mesoendothyra croatica and alga Dogger and Lower Malm beds are not easily Selliporella donzelli were determined. On Mt. determined by fossils. Their thickness is several Hru{ica and Trnovski gozd rare coral buildups tens of meters only. They are represented with and layers of crinoidal limestone occur. shales, radiolarites and beds of micritic and bio In Notranjska dark grey biomicritic and pel micritic limestone with chert nodules (Buser, micritic limestone occurs in Lower and Middle 1979b; Ogorelec & Dozet, 1997). Among the fos- Jurassic, that indicates sedimentation in rather sils foraminifer Globigerina helveto-jurassica secluded and restricted parts of shelf with la- and radiolarians appear (Gori~an, 1997). goons and periodic anoxic conditions (Orehek Upper Malm – Tithonian is represented in the & Ogorelec, 1981). Within the limestone often up to 50 meters thick succession with white and lenses of sparry dolomite occur. In Ko~evje area light grey micritic limestone of the biancone type locally also thinner coal seams appear (Dozet, containing chert nodules and sheets. In limestone 1998). Thickness of Lower and Middle Lias beds calpionellas and radiolarians are frequent. The varies from 200 to 400 meters, and of Upper same limestone type continued to sediment also Lias and Dogger beds up to 450 meters (Buser, in Lower Cretaceous, in Berriasian and Lower 1979b). Valanginian, so that the entire package of calpi- In Lower Malm a several tens kilometers long onellid limestones can be up to 250 meters thick and several kilometers wide coral-stromato (Cousin, 1981; Buser, 1986, 1987; Jurkov{ek, 1987; poridic reef extended across the Trnovski gozd, Jurkov{ek et al., 1990). which at that time represented the northern mar- gin of Dinaric carbonate latform. The reef is up Julian carbonate platform to 500 meters thick (Turn{ek, 1966, 1969, 1972, 1997; Turn{ek et al., 1981). Between the reefs that The Lower Jurassic beds are developed in a extended with interruptions to Suha Krajina and shallow water facies of the open shelf. In them across Gorjanci to Lika in Croatia (Veli} et al., biosparitic, oolitic and micritic limestones alter- 2002) sedimentation of interreef breccias and nate, and locally also stromatolitic and loferi bedded limestones with hydrozoan Cladocoropsic tic beds are present. On the contact with Upper mirabilis took place. Triassic carbonates emersion breccias and nep For the Upper Malm (Kimmeridgian and tunian dikes occur in places, both impregna Tithonian) are again characteristic oolitic and ted with reddish clayey matrix (Babi}, 1980/81; biomicritic limestones with algae Clypeina juras- Jurkov{ek et al., 1990; ^rne et al., 2007). sica and Salpingoporella annulata (Buser, 1979b; In Upper Lias the Julian platform became dis- Orehek & Ogorelec, 1981; Strohmenger & Dozet, sected into several blocks that subsided to vari- 1990), and with aberrant tintinnidas (Ker~mar, ous depths. On them pelagic sedimentation and 1961). Among foraminifers the trocholinas (Tro- condensation of sediments started (Buser, 1986a; cholina alpina in T. elongata), Protopeneroplis Jurkov{ek et al., 1990; Šmuc, 2005). On Mts. Man- striata, Pfenderina salernitana, Kurnubia pa gart and Rombon, in Trenta valley and in the Val- lestinensis, K. jurassica in Nautiloculina oolithica ley of Triglav lakes reddish biomicritic limestones were recognized (Šribar Lj. – Analyses for BGM). of the »ammonitico rosso« type outcrop that con- Certain beds indicate littoral sedimentation. On tain iron and manganese nodules (Jurkov{ek et Mikrofacies mezozojskih karbonatnih kamnin Slovenije 41 al., 1990; Šmuc, 2005; Ogorelec et al., 2006). The and owing to traces of organic matter usually variegated limestones exhibit a microfacies that of medium to darker grey color. Some limestone is very similar to the one known from the clas- beds were affected by early or/and late diagenetic sic locality of nodular deeper water limestones dolomitization. The latter is manifested by do- in Northern Alps (e.g. at Adnet near Salzburg – lomite rhombohedrons, often of zonal structure, Böhm et al., 1999). and by smaller lenses of sparry dolomite. The manganese-bearing horizon is overlain by Šribar (1979b) subdivided the entire Lower several meters thick reddish and brownish micri Cretaceous succession on Logatec plateau into tic limestone with radiolarians and chert nodules five cenozones on the basis of microfossil assem- of Dogger and Malm age, followed by Berriasian blages. The same subdivision is valid also for the »biancone« type limestone with chert nodules. Trnovski gozd (Koch, 1988; Koch et al., 1989) and Ko~evje areas (Dozet, 1990c; Dozet & Šribar, 1991). Eastern Alps Characteristical of Berriasian and Valanginian In Northern Karavanke Mts. Lower Jurassic stage and the most important are the microcopro- beds occur in the area of Ur{lja gora and sur- lite Favreina salevensis and algae Salpingoporella roundings as reddish platy and nodular reddish annulata. Favreinas are locally so numerous that limestones with chert lenses, deposited in a deeper they become rock-forming. Among the foramini- sea (Ramov{ & Rebek, 1970; Mio~ & Šribar, 1975). fers species Pseudocyclammina lituus appears. In the upper part of Valanginian and Hauteri vian beds alga Clypeina solkani and foraminifers CRETACEOUS Pseudotextulariella salevensis and Orbitolinop- sis capuensis are present. In larger numbers Although Cretaceous period is the longest occur also ostracods and tiny molluscs. In those one in Mesozoic era, lasting for whole 80 mil- times were present next to biomicritic limestones lions years, its development in Slovenian region also microfacial types with frequent desiccation is rather monotonous. On the Dinaric platform cracks that indicate paleogeographic conditions as a thick sequence of limestones and dolomites, similar to those in Valanginian, i.e. restricted and in the Slovenian basin, that at that time shelf with lagoons and intertidal plains (Orehek extended also to the region of the Julian carbo & Ogorelec, 1979, 1981; Šribar, 1979b; Dozet & nate platform, as flysch beds with intermediate Šribar, 1991). packets of deeper water limestones. Thickness of Barremian age of limestone is supported by Cretaceous beds on the Dinaric carbonate plat- dasycladacean algae Salpingoporella muehlber- form attains up to 2000 meters, and in the basin geri, and the Aptian age by species Salpingopo- up to 800 meters (Pleni~ar, 1979, 2009; Buser, rella dinarica, which is extraordinarily numerous 1989) ; OGK Explanatory books). At the end of in some beds at transition to Albian. In Aptian Cretaceous a long period of subaerial exposure S. dinarica is accompanied by foraminifer Pal- started in southern Primorska and in Istria. In orbitolina lenticularis, miliolids and numerous the same time the Dinaric carbonate platform specimens of microorganism of problematic ori- disintegtrated to several smaller units with inter- gin Bacinella irregularis Radoi~i}, for which it mediate flysch basins that starting in the Upper is assumed to belong to cyanobacteria (Flügel, Cretaceous all to the end of Paleogene gradually 2004). Due to intense tectonics thedifferentiation shifted from the north, resp. from the Bovec area of Dinaric platform and changes of paleoenviron- southwards to central Istria (Buser, 1986b). ment occurred in this time. This resulted into a Schematic presentation of development of greater diversity of facies and of thicknesses of Cretaceous beds is shown on figures 2 and 3, and individual cenozones within particular series separately on figure 14. (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 Dinaric carbonate platform by emersion breccia on the boundary between the The Lower Cretaceous beds are the most exten Brje and Povir Formations (Fig. 19), i.e. on the sively represented in shallow water development boundary between Aptian and Albian (Koch & in Dolenjska, Notranjska, on Mt. Hru{ica and on Ogorelec, 1987; Jurkov{ek et al. 1996; Jurkov{ek western part of Trnovski gozd. Their development 2010; ). Limestone of Valanginian to Albian age is is rather monotonous, having characteristics of often dolomitized, partly or totally, the dolomiti- sedimentation on restricted shelf with lagoons zation being of late diagenetic character. and periodical intertidal conditions. With respect To the upper part of Lower Cretaceous beds, to microfacies among limestones prevail types of Albian age, Šribar (1979b and Dozet & Šribar with micritic matrix (mudstone to packstone) and 1991) attributed limestone and dolomite beds fossils typical for quieter environments – fora- containing orbitolinas (Orbitolina ex gr. texa- minifers, ostracods, algae and molluscs. na) and foraminifers (»Valdanchella« dercourti). The lithologic transition of Upper Jurassic to Quite frequent in this beds are also miliolids, and Berriasian beds is gradual. The limestone texture requienids among the molluscs. is biopelmicritic, often with desiccation cracks A higher energy index within the Lower Cre- and lamination. The rock is locally slightly marly, taceous succession is indicated by rare beds con- 42 Bojan OGORELEC taining ooids and pseudoooids. Both were trans (Jurkov{ek et al., 1996; Jurkov{ek, 2008, 2010, ported into the quieter environment with micritic Jurkov{ek & Kolar-Jurkov{ek, 2007). Within the carbonate mud, and mixed between pellets and Repen formation comprising Lower Turonian in tiny fossils. Locally also smaller reefs and bios- certain levels extremely numerous calcispheres tromes of corals, hydrozoans and algae existed. occur that may become even rock-forming (cal- Such coral reef is known from Berriaian and Val- cispheric packstone), indicating a sea-level rise- anginian at Zavrh on Banj{~ice plateau (Turn{ek between the Cenomanian and Turonian (Jenkyns & Buser, 1974), and from Aptian and Albian coral 1985, 1991; Haq et al., 1987, Jurkov{ek et al., reefs at Kanalski vrh and environs on Banj{~ice 1996; Jurkov{ek, 2010), i.e. the subsidence of the plateau (Turn{ek & Buser, 1974; Grötsch, 1991; platform. Grötsch et al., 1994), and on Ko~evska gora (Tu A sedimentological and microfacial peculiarity rn{ek et al., 1992) were described. In Aptian a within the lower part of Sežana formation is rep- smaller algal reef consisting predominantly of resented by a several meters thick horizon with Lithocodium aggregatum (syn. Bacinella irregu- large oncoids (Oncoidal limestone, Jurkov{ek et laris) existed on Mt. Sabotin (Koch et al., 2002). al., 1996; Jurkov{ek, 2010). This oncoidal horizon Within the Hauterivian succession occurs in is widespread and is recognizable as a marker ho- western part of Trnovski gozd and on Mt. Sabotin rizon throughout the Dinaric carbonate platform a 15 to 40 meters thick packet of black biomic- (Gu{i} & Jelaska, 1990; Ti{ljar et al., 2002). ritic and biopelmicritic platy and bituminous In the region of Dinaric carbonate platform limestone with chert nodules (»Trnovo platy lime- two well-marked emersion phases occurred in stone«, Pleni~ar & Buser, 1967) which contains the Upper Cretaceous that resulted in strati- up to 1.1 % Corg. Analyses of a number of samples graphic gaps. The first such phase in the interval indicate that this limestone could be regarded as from Upper Cenomanian to Coniacian happened a potential source rocks for hydrocarbons with on the northern edge of platform and it can be low capability for their generation (Ogorelec et best recognized on Mt. Sabotin, wheras toward al., 1996a). Mt. Nanos its extent is already smaller, cover- Upper Cretaceous beds were deposited on a ing only a part of Coniacian (Jež, 2011). In Kras more open and shallow shelf of a higher energy area this gap cannot be recorded. The second index. For them are characteristic light color emersion phase covered a wider time-span. In of limestones, thick beds and rich rudist fauna places on Kras subaerial exposure lasted for an (Pleni~ar, 2005; Pleni~ar & Jurkov{ek, 1996, insignificant time-range between Campanian and 1998). All types of limestones are represented, Maastrichtian, while more to the south (Matarsko but packstone and grainstone are the most fre- podolje, Istria) it existed already from Senonian quent. The Upper Cretaceous beds are exposed on, and lasted up to Eocene (Drobne, 1979; Buser, to a larger extent on the Trieste-Komen plateau 1980; Jurkov{ek et al., 1996; Otoni~ar, 2006, 2007; and on Mt. Nanos, and to a lesser extent on Ja- Jež, 2011). Results of emersion phases and karsti- vorniki Mts., in Dolenjska and Ko~evje area. fication are pockets of bauxitic clay. Owing to great thicknesses of individual beds, Within the Upper Cretaceous succession on interesting appearance and good technical pro the Trieste-Komen plateau black platy and bitu- perties they are appreciated as architectural minous limestones with chert nodules are charac- stone, and are quarried especially in the Kras teristic, known in literature as »the Komen fish- region in numerous quarries. Dolomite beds are shales« for the numerous fossil remains of fishes considerably less frequent than in the Lower Cre- (Gorjanovi}-Kramberger, 1895; Jurkov{ek et al., taceous succession. 1996; Jurkov{ek, 2010; Cavin et al., 2000; Palci In spite of monotonous lithologic development et al., 2008). Primarily (Buser, 1968) these lime- the Upper Cretaceous beds can be biostratigrap stones were attributed to three horizons within hically well subdivided on basis of fossils, espe- the Albian-Cenomanian, Turonian and Senonian cially foraminifers and rudists (Šribar & Pleni~ar, succession, however newer research revealed 1990; Pleni~ar, 1960, 1979, 2005, 2009; Jež, 2011). more horizons. In the interval from Cenomanian Such division is shown on Fig. 20 for the region to Santonian they belong to the Komen limestone, of southwestern Slovenia. For Middle and Upper and in the Santonian-Campanian part of the Li- Cenomanian among foraminifers Broeckina (Pas- pica formation horizons of Tomaj limestone occur trikella) balcanica is characteristic, for Upper (Jurkov{ek et al., 1996; Jurkov{ek, 2008, 2010). Turonian the nonskeletal alga Aeolisaccus kotori, The texture of Komen limestone is biomicritic for Coniacian and Lower Santonian foraminifer and biopelmicritic, often with millimeter-scale Pseudocyclammina sphaeroidea, for Upper San- lamination. It was deposited in shallow restricted tonian and Campanian Keramospherina terge lagoons under anaerobic conditions and on inter- stina, and for Maastrichtian Orbitoides media tidal plains. The latter are indicated by torn la and Rhapydionina liburnica (Šribar & Pleni~ar, minae (»flat pebble conglomerate«), stromatolites 1990). and shrinkage pores. The microfossil assemblage In the Trieste-Komen plateau region forma- is poor and atypical (foraminifers, ostracods, al- tions were defined in addition to cenozones : the gae – mainly Thaumatoporella parvovesiculifera). Povir formation of Cenomanian age, Sežana for- Periodic communication of lagoons with the open mation of Upper Turonian, Coniacian and San- sea is indicated by pelagic fossils. Next to fishes tonian, and the Lipica formation of Campanian also other macrofossils occur in limestone, such Mikrofacies mezozojskih karbonatnih kamnin Slovenije 43 as plants, saccocomas, ammonites and others tents (Hansen et al., 1995), and presence of glassy (Jurkov{ek & Kolar-Jurkov{ek, 1995, 2007; Do- spherulae (Gregori~ et al., 1998). bruskina et al., 1999; Summesberger et al., 1996, 1999). The Tomaj limestone contains beds of bio Deeper-marine development of Cretaceous calcarenite as well, often showing graded bedding. Calcarenite is believed to have been deposi Deeper-marine development of sedimentary ted as allodapic limestone in local deepenings rocks in the region of Slovenian basin continued occurring within anoxic basins. owing to tecto from Jurassic into Cretaceous that, in addition, nics (Ogorelec et al. 1987). In spite of black color advanced northwards. For this deeper environ- and smell of bitumen the Komen limestone con- ment beds with intermediate limestone breccias tains only a scarce proportion of organic C, in are characteristic, in short the clastic develop- major part up to 0.8 %, and only exceptionally to ment of Cretaceous (Pleni~ar, 1979, 2009). Flysch 1.7 %. Unfavorable for oil potential is the compo- occurs in two thicker packets – as the lower flysch sition of organic matter which is predominantly formation, 100 to 400 meters thick, in Aptian and of terrestrial origin (Ogorelec et al., 1996a,b). Albian (Cousin, 1970), and as the upper, up to 800 The Cretaceous time is terminated by lime- meters thick flysch formation in the Upper Creta- stones of the Liburnian Formation which conti ceous (Buser, 1986). The source material for car- nues further to Lower Paleocene. Biosparitic bonate breccias were shallow-marine limestones limestone is alternating with biomicritic varieties, that broke off the edge of the Dinaric platform, and locally with stromatolitic beds. Characeans and slided down the slope, while the flysch was indicate sedimentation in brackish palustrine deposited from the northwest (Ogorelec, 1970; environment. In the lower part of Liburnian Ku{~er et al., 1974). The total thickness of deeper- formation which is marked by Vreme beds, and marine Cretaceous succession varies between 500 is still of Maastrichtian age, the most charac- and more than 1000 meters. The most complete teristical foraminifer Rhapydionina liburnica development of these strata of the Slovenian ba- (Stache) occurs, which is accompanied by milio sin is found in Tolmin area (Buser, 1986a,b) and lids, rhizocodia, ostracods and molluscs, espe- in eastern Sava folds between Kr{ko and Gorjan- cially gyropleuras (Drobne, 1981; Drobne et al., ci Mts., whereas in the Bovec area and in central 1989, 1995; Pleni~ar et al., 1992; Hötzl & Pavlo- Slovenia they occur rather fragmentarily. vec, 1979). In this facies also thinner coal seams From the standpoint of carbonate sedimen- appear in places, which were mined in the past tology and microfacies only three facies types (Vremski Britof, Lipica, Se~ovlje; Hamrla, 1959). or rock packets are interesting within the Creta- The Cretaceous-Tertiary (K/T) boundary in ceous deeper water development: Slovenia is recognizable in Kras region where it – white and light grey platy limestones of was studied in several sections, at Dolenja vas Berriasian age, that continue from the Up- (Drobne et al., 1988, 1989, 1995, 1996, 2009), on per Jurassic, Sopada near Štorje (Ogorelec et al., 2007), at – marly limestones of »scaglia« type of Albian Kozina (Delvalle & Buser, 1990), and êbulovica to Turonian and »Senonian« ages, and (Ogorelec et al., 2001). On Italian side of the area – the Vol~e limestone of »Senonian« age. it was studied at Padri~e (Padriciano, Brazzati et al., 1996) and Bazovica (Basovizza, Riccamboni, The oldest Cretaceous beds of deeper-marine 2005). Its geologic peculiarity is a shallow water development belong to the white micritic lime- facies development which is extraordinary and stone of the biancone type (mudstone and wacke- unique for the entire Mediterranean domain. stone) with chert nodules. It represents the con- The very boundary lies within a 0.2 do 2 me- tinuation of sedimentation from the upper part ters thick emersion breccia deposited in an of Jurassic. It is the uppermost part of a 100 to intertidal environment of a restricted lagoon 250 meters thick limestone packet of which the with characteristic shrinkage pores, rhizocodium Berriasian and Lower Valanginian age is de- structures (Paronipora sp.), stromatolitic lami- termined by calpionellas (Calpionella elliptica, nae and bauxite pockets (Jurkov{ek et al., 1996; C. alpina, Tintinopsella hungarica) and radiolari Ogorelec et al., 2007; Drobne et al., 2009). Lime- ans (Pleni~ar, 1979, 2009; Šribar, 1981; Buser, stone just below the boundary is light biomicrite 1986). and pelmicrite (wackestone and packstone), lo- In the region of the Slovenian basin no sedi cally slightly marly, and dark biomicrite with gy- ments from Valanginian to Barremian are known ropleuras and foraminifers (Drobne et al., 1995; at present. The succession starts transgressively Pugliese et al., 1995). Biomicritic limestone pre- with flysch rocks on biancone beds not earlier than vails just above the boundary in Lower Danian, in Aptian, whereas the sedimentation of flysch and shows all characteristics of palustrine facies and intermediate limestone breccias in environs (Otoni~ar & Ko{ir, 1998; Ogorelec et al., 2001; of Bohinj started already in Valanginian (Buser, Ko{ir 2004). In addition to the change of biota the 1986; Budkovi~, 1978); their deposition lasted to boundary is marked also by a change of isotopic the end of Lower Cretaceous. Age of this flysch composition of limestone – an extraordinary, up has been dated by nanoplankton (Buser & Pav{i~, to 8 ‰ enrichment with light δ13C isotope exactly 1978; Pav{i~ & Gori~an, 1987; Pav{i~, 1994). at the boundary (Dolenec et al., 1995; Ogorelec In the lower part of Upper Cretaceous, i.e. in et al., 1995, 2007), an increased iridium con- Cenomanian and Turonian, reddish platy and 44 Bojan OGORELEC marly limestones were deposited in the wider replaced by, red marly limestone of the scaglia Tolmin area. They are interbedded with marl- type (Ogorelec, 1970; Ku{~er et al., 1974; Buser, stones, chert sheets and with calcarenites, and 1986b; Šmuc, 2005) known as scaglia rossa, which the formation is known as »scaglia variegata« contains in addition to species of globotruncanas, (Buser, 1986b). In the wider surroundings of occurring in Vol~e limestone, also other ones Mt. Mangart such sediments appear already in (Radoi~i} & Buser, 2004). Albian (Šmuc, 2005). Age of these beds is deter- Above the Vol~e limestone and red scaglia mined with nanoplankton (Pav{i~, 1979) and glo- again an up to 600 meters thick packet of flysch botruncanas (Globotruncana helvetica, G. schne beds occurs. In fragments of coarse-grained flysch egansi, G. sigali; Buser, 1986b). breccia of Senonian age that overlies the Vol~e The variegated scaglia is followed by 100 to limestone numerous corals were determined on at most 300 meters of Vol~e limestone Forma Banj{~ice plateau (Turn{ek & Buser, 1976). The tion. Characteristical for the Vol~e limestone flysch basin gradually shifted from Campanian is alternation of thin layers of biomicrite, calci on more and more southward, to Gori{ka Brda, to rudite and calcarenite with frequent interme Trieste area and Istria (Buser, 1986b). diate chert sheets and nodules. The calciruditic beds often show graded bedding and lamination (Ogorelec et al., 1976). These beds were deposited Eastern Alps by turbidity flows at basin margins, whereas the biomicritic sheets of mudstone type result from In surroundings of Zre~e and Stranice near quiet pelagic phases. Thus, Vol~e limestone can Slovenske Konjice a reef limestone with nume be recognized as carbonate flysch or allodapic rous rudists lies between clastites, consisting limestone. Autochthonous fossils are pelagic, of claystones, siltstones, marlstones and a coal mainly globotruncanas and radiolarians, while seam (Pleni~ar, 1971, 1993, 2005). In marlstones among the washed-in particles fragments of ru solitary corals are also frequent (Turn{ek, 1994). dist valves, of echinoderms and of other bivalves Development of these beds has been compared occur. The most common globotruncanas are by authors (Hamrla, 1988; Turn{ek, 1994; Ple Globotruncana arca, G. calcarata, G. conica, G. ni~ar, 1971, 2009) to Gosau development of Cre- elevata and G. lineiana lineiana (determined by taceous in the Northern Alps. Limestones of the L. Šribar, in Ogorelec et al., 1976) that occur Gosau facies are not considered in the present from Upper Turonian to Campanian. North of monography since they were not a subject of our Kobarid the Vol~e limestone passes into, or is researches. Mikrofacies mezozojskih karbonatnih kamnin Slovenije 45

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Carint the role of the Krn area in the Upper Triassic and hia II (1975), Klagenfurt:17-26. Jurassic history of the Julian Alps. Vesnik Zavoda Buggisch, W., Flügel, E., Leitz, E. & Tietz, G.F. 1976: za geol. i geof. istraž. A Geologija, 38/39: 59-88. Die fazielle und paläogeographische Entwicklung Babi}, Lj. & Zupani~, J. 1978: Kosmatovi “Železnikarski im Perm der Karnischen Alpen und in den Randge- vapnenci i dolomiti” i Zalilo{ki krovni {kriljevci u bieten. Geol. Rundschau, 65: 649-690. predgorju Julijskih Alpa: podaci o stratigrafiji, fa Buser, S. 1968a: Osnovna geolo{ka karta SFRJ ciesu i paleogeografskom zna~enju. = Kossmat’s 1 : 100.000, list Gorica. Zv. geol. zav., Beograd. “Kalke und Dolomite von Eisnern” and “Dachschie Buser, S. 1968b: Razvoj jurskih skladov v slovenskih fer von Salilog” in the Julian Prealps: data about Zunanjih Dinaridih = Development of Jurassic stratigraphy). Geol. vjesnik, 30/1: 21-42. strata in Outer Dinarides of Slovenia. Prvi kolokvij Bathurst, R.G.C. 1971: Carbonate Sediments and o geologiji Dinaridov 1: 59-67. their Diagenesis. Dev. Sediment. 12, Elsevier Publ., Buser, S. 1973: Tolma~ lista Gorica – Osnovna geolo{ka Amsterdam: 620 p. karta SFRJ 1 : 100.000. Zv. geol. zav., Beograd: 50 p. Bitner M.A., Jurkov{ek, B. & Kolar-Jurkov{ek, T. 2010: Buser, S. 1974: Neue Feststellungen im Perm der west New record of the inarticulate brachiopod genus lichen Karawanken. Carinthia II, 164/ 84: 27-37. Discinisca from the Upper Triassic (Carnian) of Buser, S. 1978: Razvoj jurskih plasti Trnovskega gozda, the Julian Alps, NW Slovenia. Neues Jahrb. Geol. Hru{ice in Loga{ke planate = The Jurassic strata of Paläontol. Abh., 257/3: 367-372. Trnovski gozd, Hru{ica and Loga{ka planota. Rud. Böhm, F., Ebli, O., Krystin, L., Lobitzer, H., Rakus, M. met. zb., 4: 385-406. & Siblik, M. 1999: Fauna, Stratigraphy and Deposi- Buser, S. 1979a: Triassic beds in Slovenia. 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Buser, S. 1980a: Tolma~ lista Celovec, Osnovna geolo Bosellini, A. & Hardie, L.A. 1973: Depositional thema {ka karta SFRJ 1 : 100.000. Zv. geol. zav., Beograd: of a marginal marine evaporite. Sedimentology, 20: 62p. 5-28. Buser S. 1980b: Stratigrafske vrzeli v paleozojskih Bosellini, A. & Rossi, D. 1974: Triassic Carbonate Buil in mezozojskih plasteh v Sloveniji – Simpozium dups of the Dolomites, Northern Italy. Soc. Econ. iz regionalne geologije i paleontologije. Rud. geol. Paleont. Min. Spec. Publ., 28: 209-233. fakultet Beograd: 335-344. Bradner, R. & Resch, W. 1981: Reef Development in the Buser, S. 1986a: Osnovna geolo{ka karta SFRJ Middle Trassic (Ladinian and Cordevolian) of the 1 : 100.000, list Tolmin in Videm. Zv. geol. zav., Beo- Northern Limestone Alps near Innsbruck, Austria. grad. 46 Bojan OGORELEC

Buser, S. 1986b: Tolma~ lista Tolmin in Videm (Udine). Disertacija, Univ. Ljubljana, NTF, Odd. geol., Lju- Osnovna geolo{ka karta SFRJ 1 : 100.000. Zv. geol. bljana: 137 p. zav., Beograd:103 p. Celarc, B. 2004b: Problematika »cordevolskih« apnen- Buser, S. 1989: Development of the Dinaric and the cev in dolomitov v slovenskih Južnih Alpah = Prob- Julian Carbonate Platforms and of the intermediate lems of the “Cordevolian” Limestone and Dolo- Slovenian Basin (NW Yugoslavia). Mem. Soc. Geol. mite in the Slovenian part of the Southern Alps. It., 40 (1987): 313-320. Geologija, 47/2:139-149, Buser, S. 1996: Geology of Western Slovenia and its doi:10.5474/geologija.2004.011. paleogeographical evolution. In: Drobne, K., Go Celarc, B. & Kolar-Jurkov{ek, T. 2008: The Carnian- ri~an, S. & Kotnik; B. (eds.): Int. workshop Postojna Norian basin-platform system of the Martuljek ’96: The role of impact processes in the geological mauntain group (Julian Alps, Slovenia): progra- and biological evolution of planet Earth, Ljubljana: dation of the Dachstein carbonate platform. Geol. 111-123. Carpathica, 59/3: 211-224. Buser, S. & Debeljak, I. 1996: Lower Jurassic beds Celarc, B. & Žalohar, J. 2010: Ladinijske plasti v with bivalves in south Slovenia. Geologija, 37/38 Kamni{ko-Savinjskih Alpah in Južnih Karavankah. (1994/95): 23-62. In: Hitij T. et al. (ur.): Kraljestvo Tetide, Okameneli Buser, S. & Dozet, S. 2009: Jura = Jurassic. In: Pleni~ar svet triasnih vreten~arjev Kamni{ko-Savinjskih M., Ogorelec, B. & Novak, M. (eds.): Geologija Slo- Alp. Scopolia Suppl. 5:148-156. venije = The Geology of Slovenia, Geolo{ki zavod Cigale, M. 1978: Karnijske plasti v okolici Idrije = Car- Slovenije, Ljubljana: 215-254. nian beds in the Idria region. Geologija, 21/1: 61-75. Buser, S. & Komac, M. 2002: Geolo{ka karta Slovenije Cousin, M. 1970: Esquisse géologique des confins italo- 1 : 250.000 = Geologic Map of Slovenia 1 : 250.000. yougoslaves: leur place dans les Dinarides et les Geologija, 45/2: 335-340, Alpes méridionales. Bull. Soc. Géol. Fr. 7/XII-6: doi:10.5474/geologija.2002.029. 1034-1047. Buser, S. & Ogorelec, B. 1987: Carnian Amphiclina Cousin, M. 1973: Le sillon slovéne: les formations tria Beds – Hudajužna. Guidebook, Int. Symp. Evol. siques, jurassiques et néocomiennes au Nord-Est Karstic Carbonate Platforms, Trieste: 13-18. de Tolmin (Slovénie occidentale, Alpes méridio Buser, S. & Ogorelec, B. 2008: Globjevodne triasne in nales) et leurs affinités dinariques. B.S.G.F., 7/15, jurske plasti na Kobli = Deep-water Triassic and 3-4: 327-339. Jurassic beds from Mt. Kobla (W. Slovenia). Geologi- Cuvillier, J. 1952: Le notion de «microfacies» et ses ja, 51/2: 181-189, doi:10.5474/geologija.2008.019 applications. VIII Congr. Nation. Methan Petrol., Buser, S. & Pav{i~, J. 1978: Spodnjekredni nanoplank- Sect. I.: 1-7 ton med Sevnico in Brestanico. Rud.met. zb., 2/3: Cuvillier, J. 1962: Etude et utilisation rationelle de mi- 199-205. crofacies. Rev. Micropal. 4/1: 3-6. Buser, S., Grad K. & Pleni~ar, M. 1967: Osnovna âdež, F. 1977: Sadra in anhidrit na Idrijskem = Gyp- geolo{ka karta SFRJ 1 : 100.000, list Postojna. Zv. sum and Anhydrite Occurrences in Idria Region. geol. zav., Beograd. Geologija, 20: 289-301. Buser, S., Grad, K. & Pleni~ar, M. 1970: Tolma~ lista âr, J. 1989: Okolje nastanka anizijskega dolomita nad Postojna, Osnovna geolo{ka karta SFRJ 1 : 100.000. srednjetriasno erozijsko diskordanco v Idrijskem Zv. geol. zav. Beograd: 62 p. rudi{~u = Depositional environment of the Anisian Buser, S., Pav{i~, J. & Radoi~i}, R. 1979: Spodnjekred- dolomite above the Middle Triassic erosional dis ne plasti v Bohinju. Rud. met. zb., 26/4, 385-393. konformity in the Idrija ore deposit. Rud. met. zb., Buser, S., Pav{i~, J. & Ani~i}, B. 1982a: Globokomorske 36/2: 395-407. kredne plasti v vzhodni Sloveniji = Deep sea Creta- âr, J. 2010: Geolo{ka zgradba idrijsko-cerkljanske- ceous beds of Eastern Slovenia. X jub. kongr. geol. ga hribovja – Tolma~ h Geolo{ki karti idrijsko- Jug., Budva, 1: 11-23. cerkljanskega hribovja med Stopnikom in Rovta- Buser, S., Ramov{, A. & Turn{ek, D. 1982b: Triassic mi 1 : 25.000. Geolo{ki zavod Slovenije, Ljubljana: reefs in Slovenia. Facies, 6: 15-24. 127 p. Buser S., Grad, K., Ogorelec, B., Ramov{, A. & Šribar, âr, J. & âdež, F. 1977: Klasti~ni vložki v srednjetriad L. 1988: Statigraphical, paleontological and sedi- nem dolomitu na Idrijskem = Middle Triassic Dolo- mentological characteristics of Upper Permian beds mite Intercalated with Clastic Sedimentary Rocks in Slovenia, NW Yugoslavia. Mem. Soc. Geol. It., 34 in Idrija Region. Geologija, 20: 85-106. (1986): 195-210. âr, J. & Skaberne, D. 1995: Ladinijske plasti Stopnika Buser, S., Kolar-Jurkov{ek, T. & Jurkov{ek, B. 2007: = Ladinian beds of Stopnik. Geolo{ki zbornik, 10: Triasni konodonti Slovenskega bazena = Triassic 22-25. conodonts of the Slovenian Basin. Geologija, 50/1: âr, J., Gregori~, V., Ogorelec, B. & Orehek, S. 1980: 9-28, doi:10.5474/geologija.2007.001 Sedimentolo{ki razvoj skitskih plasti v idrijskem Buser, S., Kolar-Jurkov{ek, T. & Jurkov{ek, B. 2008: rudi{~u = Sedimentological development of Scyt Slovenian Basin during Triassic in the Light of hian beds in the Idrija mercury deposit. Rud. met. Conodont Data. Boll. Soc. Geol. It., 127/2: 257-263. zb., 27/1: 3-20. Carozzi, A. 1960: Microscopic Sedimentary Petrogra- âr, J., Skaberne, D., Ogorelec, B., Turn{ek, D. & phy. Wiley Publ. Co., New York: 485 p. Placer, L. 1981: Sedimentological characteristics of Carozzi, A.V. 1989: Carbonate rocks depositional mo Upper Triassic (Cordevolian) circular quite water dels. A mocrofacies approach. Englewood Cliffs coral bioherms in Western Slovenia, Northwestern (Prentice Hall): 604 p. Yugoslavia. In: Toomey, D.F. (ed.): European Fossil Cavin, L., Jurkov{ek, B. & Kolar-Jurkov{ek, T. 2000: Reef Models. SEPM Spec. Publ., 30: 233-240. Stratigraphic succession of the Upper Cretaceous ^rne, A.E., Šmuc, A. & Skaberne, D. 2007: Jurassic nep- fish assemblages of Kras (Slovenia). Geologija,43/2: tunian dikes at Mt. Mangart (Julian Alps, NW Slo- 165-195, doi:10.5474/geologija.2000.013 venia). Facies, 53:249-265, Celarc, B. 2004a: Geolo{ka zgradba severovzhodnega doi:10.1007/s10347-007-0102-8 dela Kamni{ko-Savinjskih Alp = Geologic struc- Delvalle, D. & Buser, S. 1990: Microfacies analysis of ture of Northeastern part of Kamnik-Savinja Alps. limestone from the Upper Cretaceous to the Low- Mikrofacies mezozojskih karbonatnih kamnin Slovenije 47

er Eocene of SW Slovenia (Yugoslavia). Geologija, across the Permian-Triassic boundary in the Masore 31/32 (1988/89): 351-394. section (Western Slovenia). Facies 50, 287-299, Dem{ar, M. & Dozet, S. 2002: Nekaj razvojev zgor doi:10.1007/s10347-004-0016-7. njepermskih plasti zahodno od Škofje Loke = Some Dozet, S. 1977: Triadne plasti na listu Delnice = The developments of Upper Permian in the area west Triassic beds on the Delnice Map Sheet. Geologija, of Škofja Loka – Western Slovenia. Geologija 45/1: 20: 236-246. 189-200, doi:10.5474/geologija.2002.015 Dozet, S. 1979: Karnijske plasti južno in zahodno od Dem{ar, M. & Dozet, S. 2003: Anizijske in ladinijske Ljubljanskega barja = Carnian beds south and west plasti v profilu nad Sredi{ko grapo pod Križno of the Ljubljana Moor. Geologija, 22/1: 55-70. Goro, osrednja Slovenija = Anisian and Ladinian Dozet, S. 1980: Jurske plasti na ko~evskem in južno beds in the cross-section above Srednik Valley at vzhodnem Notranjskem = Jurassic beds in Ko~evska Križna Gora, Central Slovenia. Geologija, 46/1: 41- and Southern Notranjska area. Rud. met. zb., 27/4: 48, doi:10.5474/geologija.2003.002 443-457. Dobruskina, I.A., Jurkov{ek, B. & Kolar-Jurkov{ek, T. Dozet, S. 1990a: Triasni skladi Ko~evske in Gorskega 1999: Upper Cretaceous flora of Slovenia. Annales, Kotarja = Triassic Beds of Ko~evje and Gorski Ko- Ser. Hist. Nat., 9/2-17: 243-256. tar Area. Rud. met. zb., 37/2: 141-160. Dobruskina, I.A., Jurkov{ek, B. & Kolar-Jurkov{ek, Dozet, S. 1990b: Loferske cikloteme v glavnem dolo- T. 2001: Upper Triassic flora from “Raibl beds” of mitu Ko~evske = The Lofer Cyclothems in the Main Julian Alps (Italy) and Karavanke Mts. (Slovenia). Dolomite (Hauptdolomit) of the Ko~evje Area. Rud. Geologija, 44/2: 263-290, met. zb., 37/4: 507-528. doi:10.5474/geologija.2001.019 Dozet, S. 1990c: Biostratigrafska raz~lenitev jurskih Dolenec, M. 2004: Permsko-triasna meja v Karavankah in spodnjekrednih plasti Ko~evske in Gorskega Ko- in zahodni Sloveniji: sedimentolo{ki, izotopski in tarja = Biostratigraphic subdivision of the Jurassic geokemi~ni vidiki globalnih sprememb v zahodni and Lower Cretaceous beds in Ko~evje and Gorski Tetidi. Disertacija, NTF Univ. Ljubljana: 110 p. Kotar area. Rud. met. zb., 37/1: 3-18. Dolenec, M. & Ogorelec, B. 2001: Organic carbon iso Dozet, S. 1991: Norian oncoids in the Main Dolomite of tope variability across the P/Tr boundary in the the Ko~evje area. Rud. met. zb., 38/1: 79-95. Idrijca Valley section (Slovenia): A high resolution Dozet, S. 1992a: Litostratigrafske enote in zna~ilne study. Geologija, 44/2: 331-340, mikrofacije ko~evske jure. Lithostratigraphic Units doi:10.5474/geologija.2001.025 and significant Microfacies of the Ko~evje Jurassic. Dolenec, T. & Pav{i~, J. 1995: Elemental and stable iso Rud. met. zb., 39/3-4: 287-305. tope variations in the Cretaceous-Tertiary bound- Dozet, S. 1992b: Litostratigrafija, diageneza, sedimen- ary sediments from the So~a Valley, NW Slovenia. tacijsko okolje in geokemija jurskih plasti na listu Terra Nova, 7: 630-635. Delnice. Lithostratigraphy, diagenesis, environ- Dolenec, T. & Ramov{, A. 1998: Isotopic changes at the ment and geochemistry of the Jurassic beds on the Permian-Triassic boundary in the Idrijca Valley, Delnice sheet. Rud. met. zb., 39/1-2: 193-209. W Slovenia). RMZ - Mater. Geoenviron. 45/3-4: 405- Dozet, S. 1993: Lofer cyclothems from the Lower Lias 411. sic Krka Limestones. Riv.It. Paleont. Strat., 99/1: Dolenec, T., Buser, S. & Dolenec, M. 1998: The Permian- 81-100. Triassic boundary in the Karavanke Mountains Dozet, S. 1995: The Malm algal nodules (oncolites) (Slovenia): Stable isotope variations in the boun- from the Suha Krajina (Slovenia). Rud. met. zb., dary carbonate rocks in the Ko{utnik Creek and 42/3-4: 165-169. Brsnina section. Geologija, 41: 17-27. Dozet, S. 1996: Foraminiferal and algal biostratigra- Dolenec, M., Dozet, S. & Lojen, S. 2006: Permsko- phy of the Jurassic beds in Southeastern Slovenia. triasna meja ter zgornjepermski in spodnjeskitski Rud. met. zb., 43/1-2: 3-10. skladi na jugovzhodnem obrobju Ljubljanskega Dozet, S. 1997: Ambrus Beds – Important Key for In- barja, osrednja Slovenija = Permo-Triassic bounda- terpretation of Neocomian Paleogeography, Sea- ry and Upper Permian as well as Lower Scythian Level Changes, depositional Setting and Tectonics beds in the southeastern borderland of the Ljubljana in Suha Krajina Area (Slovenia). Geologija, 39 marsh, Central Slovenia. RMZ – Materiali in geo (1996): 119-131. okolje, 53/2: 229-246. Dozet, S. 1998: Lower Jurassic dolomite – limestone Dolenec, T., Ogorelec, B. & Pezdi~, J. 1981: Zgornje- succession with coal in the Ko~evski Rog and cor- permske in skitske plasti pri Trži~u = Upper Per relation with neighbouring areas (southeastern Slo- mian and Scythian beds in the Trži~ area. Geologi- venia). Geologija, 41 (1999): 71-101. ja, 24/2: 217-238. Dozet, S. 1999: Ple{ka baritonosna formacija, osred Dolenec, T., Ogorelec, B., Lojen, S. & Buser, S. 1999a: nja Slovenija. Primerjava baritonosnih plasti in ba Meja perm-trias v Masorah pri Idriji = Permian- ritnih pojavov na obmo~ju Zunanjih Dinaridov = Triassic boundary in the Idrijca Valley: Masore Barite-bearing Ple{e Formation, Central Slovenia. section. RMZ – Materiali in geookolje, 46/3: 449- Comparison of barite-bearing beds and barite oc- 452. curences in the Outer Dinarides area. Geologija, 42 Dolenec, T., Lojen, S., Buser, S. & Dolenec, M. 1999b: (2000): 41-68. Stable isotope event markers near the Permo-Trias- Dozet, S. 2000: Vi{nja gora formation, central Slove- sic boundary in the Karavanke Mountains (Slove- nia. Rud. met. zb. 47/2: 137-154. nia). Geol. Croatica, 52/1: 77-81. Dozet, S. 2004: O karnijskem železnatem boksitu Ko Dolenec, T., Lojen, S. & Dolenec, M. 1999c: The Per pitovega gri~a ter o plasteh v njegovi talnini in mian-Triassic boundary in the Idrijca Valley (West- krovnini. On Carnian oolitic iron bauxite of Kopi- ern Slovenia): isotopic fractionation between car- tov gri~ and on beds in its foot- and hanging wall. bonate and organic carbon at the P/Tr transition. RMZ - Mater. Geoenviron. 51/ 4: 2191-2208. Geologija, 42: 165-170. Dozet, S. & Buser, S. 2009: Trias = Triassic. In: Pleni~ar Dolenec, T., Ogorelec, B., Dolenec, M. & Lojen, S. M., Ogorelec, B. & Novak, M. 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Hrvatski geol. konges, Vodi~ ekskurzije, Zagreb: logic column of the Lower Triassic in the Zmijavac 67-110. Mikrofacies mezozojskih karbonatnih kamnin Slovenije 55

Ti{ljar, J., Vlahovi}, I., Veli}, I. & Soka~, B. 2002: Car- Turn{ek, D., Buser, S. & Ogorelec, B. 1982: Carnian bonate Platform megafacies of the Jurassic and Coral-Sponge Reefs in the Amphiclina Beds bet Cretaceous Deposits of the Karst Dinarides. Geol. ween Hudajužna and Zakriž (Western Slovenia). Groatica, 55/2: 139-170. Razprave SAZU, IV, 24/2: 51-98. Tucker, M.E. & Wright,V.P. 1990: Carbonate sedimen- Turn{ek, D., Buser, S. & Ogorelec, B. 1984: The Role of tology. Blackwell, Oxford: 482 p. Corals in Ladinian – Carnian Reef Communities of Turn{ek, D. 1966: Zgornjejurska hidrozojska favna iz Slovenia, Yugoslavia. Paleontographica Americana, južne Slovenije = Upper Jurassic Hydrozoan Fauna 54: 201-209. from Southern Slovenia. Razprave SAZU, IV, 9/8: Turn{ek, D., Buser, S. & Ogorelec, B. 1987: Upper Car- 355-428. nian Reef Limestone in Clastic Beds at Perbla near Turn{ek, D. 1969: Prispevek k paleoekologiji jurskih Tolmin (NW Yugoslavia). Razprave SAZU, IV, 27/3: hidrozojev v Sloveniji = A Contribution of the 37-64. Paleoecology of Jurassic Hydrozoa from Slovenia. Turn{ek, D., Pleni~ar, M. & Šribar, Lj. 1992: Lower Razprave SAZU, IV, 12/5: 209-237. Cretaceous Fauna from Slovenski vrh near Ko~evje Turn{ek, D. 1972: Zgornjejurske korale iz južne Slo- (South Slovenia). Razprave SAZU, IV, 33/8: 205-257. venije = Upper Jurassic Corals of Southern Slove- Turn{ek, D., Dolenec, T., Siblik, M., Ogorelec, B., nia. Razprave SAZU, IV, 15/6: 145-261. Ebli, O. & Lobitzer, H. 1999: Contributions to the Turn{ek, D. 1994: Upper Cretaceous Reef building Fauna (Corals, Brachiopods) and Stable Isotopes Colonial Corals of Gosau Facies from Stranice of the Later Triassic Seinplatte Reef/Basin – Com- near Slovenske Konjice (Slovenia). Razprave SAZU, plex, Northern Calcareous Alps, Austria. Abh. Geol. IV, 35/1: 3-41. B.-A., 56/2: 121-140. Turn{ek, D. 1997: Mesozoic Corals of Slovenia = Mezo- Veli}, I. 2007: Stratigraphy and Palaeobiography of zojske korale Sovenije. Zbirka ZRC SAZU, 16, Lju- Mesozoic Benthic Foraminifera of the Karst Dina- bljana: 512 p. rides (SE Europe). Geologia Croatica, 60/1: 1-113. Turn{ek, D. & Buser, S. 1966: Razvoj spodnjekrednih Veli}, I., Mati~ec, D., Vlahovi}, I. & Ti{ljar, J. 1995: skladov ter meja med juro in kredo v zahodnem Stratigrafski slijed jurskih i donjokrednih karbona- delu Trnovskega gozda = The Development of the ta (bat-gornji alb) u zupadnoj Istri = Stratigraphic Lower Cretaceous Beds and the Boundary Between Succession of Jurassic and Lower Cretaceous Car- Jurassic and Cretaceous Formations in the Part of bonates (Bathonian - Upper Albian) in Western Trnovski gozd. Geologija, 9: 527-542. Istria. In: Vlahovi}, I. & Veli}, I. (eds.): 1. Hrvatski Turn{ek, D. & Buser, S. 1974: Spodnjekredne ko- geol. kongr., Vodi~ ekskurzija: 31-66. rale, hidrozoji in hetetide z Banj{ke planote in Veli}, I., Ti{ljar , J., Vlahovi}, I., Veli}, J., Koch, G. & Trnovskega gozda = The Lower Cretaceous corals, Mati~ec, D. 2002: Paleogeographic Variability and hydrozoans and chaetetids of Banj{ka planota and Depositional Environments of the Upper Juras- Trnovski gozd. Razprave SAZU, IV, 17/2: 81-124. sic Carbonate Rocks of Velika Kapela Mt. (Gorski Turn{ek, D. & Buser, S. 1976: Knidarijska favna iz Kotar Area, Adriatic Carbonate Platform, Croatia), senonijske bre~e na Banj{ki planoti = Cnidarian Geol. Croatica, 55/2: 121-138. Fauna from the Senonian Breccia of Banj{ka plano- Vlahovi}, I., Ti{ljar, J., Veli}, I. & Mati~ec, D. 2005: ta (NW Yugoslavia. Razprave SAZU, IV, 19: 37-88. Evolution of the Adriatic Carbonate Platform: Turn{ek, D. & Buser, S. 1989: The Carnian reef com- Paleogeography, main events and depositional dy- plex on the Pokljuka (NW Yugoslavia). Razprave namics. Paleogeography, Palelclimatology, Paleo- SAZU, IV, 30: 75-127. ecology, 220/3-4: 333-360. Turn{ek, D. & Buser, S. 1991: Norian - Rhaetian Coral Wilson, J.L. 1975: Carbonate Facies in Geologic His- Reef Buildups in Bohinj and Rde~i rob in Southern tory. Springer Verl., Berlin: 471 p. Julian Alps (Slovenia). Razprave SAZU, IV, 32/7: Zankl, H. 1971: Upper Triassic carbonate facies in the 215-257. Northern Limestone Alps. In: Müller, G. (ed.): Se Turn{ek, D. & Ramov{, A. 1987: Upper Triassic (Norian- dimentology of Parts of Central Europe, Guidebook. Rhaetian) reef buildups in the northern Julian Alps 8. Int. Sedim. Congress, Heidelberg: 147-185. (NW Yugoslavia). Razprave SAZU, IV, 28: 27-67. Žalohar, J. & Celarc, B. 2010: Geolo{ka zgrad- Turn{ek, D., Buser, S. & Ogorelec, B. 1981: An Upper ba Kamni{ko-Savinjskih Alp. V: Hitij T. et al. Jurassic reef complex from Slovenia, Yugoslavia. (eds.): Kraljestvo Tetide, Okameneli svet triasnih In: Toomey, D.F. (ed.): Eurpoean Fossil Reef Models. vreten~arjev Kamni{ko-Savinjskih Alp. Scopolia SEPM Spec. Publ., 30: 361-369. Suppl. 5, 43-53.

Table – Plates 58 Bojan OGORELEC

Tabla 1 – Plate 1

Zgornji perm – Upper Permian

1 Rekristaliziran mikritni apnenec s terigenimi zrni kremena in sljude. Bazalna plast zgornjepermskega zaporedja. ^adovlje pri Trži~u, 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. ^adovlje at Trži~, XN, alizarin red staininig

2 Biomikritni wackestone s {tevilnimi preseki skeletnih alg vrste Gymnocodium bellerophontis in foraminiferami. Alge in foraminifere so bile v ~asu diageneze izlužene, moldi~ne 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 plo{~ico ehinoderma. Javorjev dol pri Sovodnju. Zna~ilni 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. Karavan{ki cestni predor, 802. m, X nikoli Gypsum vein in micritic dolomite. Karavanke road tunnel, 802. m, XN

6 Kristali anhidrita v sparitnem dolomitu. Karavan{ki cestni predor, 670. m, X nikoli Anhydrite crystals in sparry dolomite. Karavanke road tunnel, 670. m, XN Mikrofacies mezozojskih karbonatnih kamnin Slovenije 59

Tabla 1 – Plate 1 60 Bojan OGORELEC

Tabla 2 – Plate 2

Zgornji perm – Upper Permian

1 Izpran gimnokodijski packstone s plo{~icami 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 ~asu diageneze izluženi, moldi~ne 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 Pre~ni presek korale Waagenophyllum indicum v mikritni osnovi. Preko koralitov poteka stilolitni {iv. 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 ~asu diageneze izlužen (moldi~na poroznost), nato pa zapolnjen z anhidritom. Karavan{ki 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 Mikrofacies mezozojskih karbonatnih kamnin Slovenije 61

Tabla 2 – Plate 2 62 Bojan OGORELEC

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 {e opazno prvotno strukturo kamnine. Izlužene moldi~ne pore po ooidih sta v pozni diagenezi zapolnila sparitni kalcit in kremen. Potok Ko{utnik pri Trži~u. Prepa- rat 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. Ko{utnik creek at Trži~. Ali- zarin red staining

3, 4 Oolitni grainstone. Ve~ino 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 rudi{~e 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 Mikrofacies mezozojskih karbonatnih kamnin Slovenije 63

Tabla 3 – Plate 3 64 Bojan OGORELEC

Tabla 4 – Plate 4

Zgornji perm – Upper Permian

1 Satasti mikrosparitni dolomit. Pore, nastale z izluževanjem evaporitov, zapolnjuje kalcitni cement (rde~e). 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 plo{~icami ehinodermov. Rejc na Vojskarski planoti Gymnocodian packstone with some foraminifers and echinoderm plates. Rejc on Vojsko plateau by Idrija

3 Permocalculus fragilis in kopu~e cianobakterij v mikritni osnovi – algni floatstone. Mažgon pri Jagr{~ah Algal floatstone with Permocalculus fragilis and microbial clusters. Mažgon at Jagr{~e

4 Sparitni dolomit z znaki dedolomitizacije (kalcitizacije). Najvi{ji 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 Karavan{ke formacije. ^adovlje pri Trži~u Micritic dolomite (mudstone) with radiolarians. Basal beds of Karavanke Formation. ^adovlje at Trži~

6 Oolitni grainstone s sparitnim kalcitnim cementom. Tesero horizont na P/T meji. Masore pri Spo- dnji Idriji Oolitic grainstone with sparry calcite cement. Tesero horizon at the P/T boundary. Masore at Spo- dnja Idrija Mikrofacies mezozojskih karbonatnih kamnin Slovenije 65

Tabla 4 – Plate 4 66 Bojan OGORELEC

Tabla 5 – Plate 5

Spodnji trias – Lower Triassic

1, 2 Gastropodni wackestone. [tevilni 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 dolomitiziran. Lom pri Trži~u Oolitic packstone. Microgastropod can be seen in nucleus of one of ooids. Limestone is partly dolomitized. Lom at Trži~

4 Biosparitni grainstone s {tevilnimi gastropodi. Zna~ilni facies spodnjetriasnega zaporedja. ^ebine nad Trbovljami Biosparitic grainstone with numerous gastropods. Characteristic facies of Lower Triassic succession. ^ebine 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, di splaying the extent of dolomitization. Podlipa at Vrhnika

6 Dolomitiziran gastropodni wackestone. Med polže je ujet tudi ve~ji ooid, ki je rde~e obarvan s he- matitom. La{ko Dolomitized gastropod wackestone. Among gastropods some ooids are present. Their reddish color is due to hematite pigment. La{ko Mikrofacies mezozojskih karbonatnih kamnin Slovenije 67

Tabla 5 – Plate 5 68 Bojan OGORELEC

Tabla 6 – Plate 6

Spodnji trias – Lower Triassic

1, 4 Oosparitni grainstone (detajl). Ooidi so zaradi železovih hidroksidov obarvani rde~kasto. Na sl. 4 so vidna zajedanja med posameznimi ooidi zaradi raztapljanja apnenca v ~asu diageneze. Kamno- lom 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. La{ko Oosparitic grainstone. Sediment was affected by vadose diagenesis. Ooid nuclei were leached and moldic pores were later cemented by sparry calcite. La{ko

5 Oosparitni grainstone – detajl. Jedra ve~ine 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 ve~jih dolomitnih zrnih. Ledina nad Sevnico Oosparitic dolomitic packstone. Primary rock structure is recognized by ooid contours and larger dolomite crystals. Ledina over Sevnica Mikrofacies mezozojskih karbonatnih kamnin Slovenije 69

Tabla 6 – Plate 6 70 Bojan OGORELEC

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 terigenimi 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 pome{ani med pelete. Medzrnska poroznost, nastala pri pozni dolomitizaciji. Rimske Toplice Washed oopelmicritic dolomite – packstone. Numerous ooids are mixed among pellets. Intergranu- lar porosity caused by late dolomitization. Rimske Toplice

4 Biosparitni packstone, ki ga sestavljajo plo{~ice ehinodermov. Vrhnji del spodnjetriasnega zaporedja. Zakamnik nad karavan{kim 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 plo{~ice ehinodermov. Lom pri Trži~u Biosparitic dolomitic grainstone, composed solely of echinoderm plates. Lom at Trži~

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 Mikrofacies mezozojskih karbonatnih kamnin Slovenije 71

Tabla 7 – Plate 7 72 Bojan OGORELEC

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 {kolj~ne 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 {kolj~nih 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 izsu{itvene 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 izsu{itvene pore v stromatolitnem dolomitu z dvema generacijama cementov – obrobni cement pripada dolomitu z evhedralnimi zrni, osrednji del por pa zapolnjuje sparitni kalcit (rde~e). 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 Mikrofacies mezozojskih karbonatnih kamnin Slovenije 73

Tabla 8 – Plate 8 74 Bojan OGORELEC

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 Izsu{itvena pora v mikritnem dolomitu – detajl. Dve generaciji cementa – obrobni kalcit generacije A (rde~e) 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 (rde~e). 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 ^rna pri Kamniku Biosparitic grainstone with algal fragments (recognized by contours and micritic envelopes) and some foraminifers. ^rna mine at Kamnik

6 Sparitni dolomit, impregniran s sfaleritnimi kristali. Rudnik Topla pri Mežici Sparry dolomite, impregnated by sphalerite crystals. Topla mine near Mežica Mikrofacies mezozojskih karbonatnih kamnin Slovenije 75

Tabla 9 – Plate 9 76 Bojan OGORELEC

Tabla 10 – Plate 10

Srednji trias (ladinij) – Middle Triassic (Ladinian)

1, 2 Rekristaliziran intrasparitni packstone. Mikritni intraklasti so zaradi tektonike splo{~eni in daje- jo kamnini videz trakaste teksture. Na sl. 2 so prisotni tudi fragmenti ehinodermov (pu{~ica). 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 {koljkami in radiolariji. Kamnolom Kamna Go- rica Micritic wackestone with thin-valved bivalves and radiolarians. Kamna Gorica quarry

4 Intramikritni apnenec, v katerem so pome{ani drobci vulkanskih kamnin. Psevdoziljske plasti. Kotredež pri Zagorju Intramicritic limestone with fragments of volcanic rocks. Psevdozilja beds. Kotredež at Zagorje

5 Drobnozrnata konglomeratna bre~a, ki jo sestavljajo dolomitni drobci in kalcitno vezivo (rde~e). Preparat je obarvan z alizarinskim barvilom. Miklaj~ na Vojskarski planoti Fine-grained conglomeratic breccia, composed of dolomite grains and calcite matrix (red). Aliza- rin red staining. Miklaj~ 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 Mikrofacies mezozojskih karbonatnih kamnin Slovenije 77

Tabla 10 – Plate 10 78 Bojan OGORELEC

Tabla 11 – Plate 11

Srednji trias (zgornji ladinij) – Middle Triassic (Upper Ladinian)

1 Bioklasti~ni 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 - Ve- lika planinna, sl. 4. - Okre{elj v Savinjskih Alpah Sections of algae Diplopora sp. in grainstone (Fig. 2) and in washed micrite (Fig. 4). Fig. 2 - Velika planina, Fig. 4 - Okre{elj 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 Bioklasti~ni grainstone s preseki dazikladacejnih alg in cianobakterij, ki obra{~ajo 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 Mikrofacies mezozojskih karbonatnih kamnin Slovenije 79

Tabla 11 – Plate 11 80 Bojan OGORELEC

Tabla 12 – Plate 12

Zgornji trias (karnij) – Upper Triassic (Carnian)

1, 2 Biomikritni packstone s preseki {kolj~nih lupin. Sl. 2 – detajl. Kamnolom Drenov gri~ pri Vrhniki Biomicritic packstone with bivalve shells. Fig. 2 – detail. Drenov gri~ quarry at Vrhnika

3, 4 Mikritni wackestone s posameznimi ostrakodi in {kolj~nimi lupinami. Sl. 3 – Limbarska gora nad Morav~ami, sl. 4 – kamnolom Drenov gri~ pri Vrhniki Micritic wackestone with ostracods and bivalve shells. Fig. 3 – Limbarska gora above Morav~e, Fig. 4 - Drenov gri~ quarry at Vrhnika

5 Alga Poikiloporella duplicata v stromatolitnem apnencu. Š~ura nad Spodnjo Trebu{o Poikiloporella duplicata algae in stromatolitic limestone. [~ura above Spodnja Trebu{a

6 Sferoidalni onkoidni packstone. Ga~nik na Vojskarski planoti Spheroidal oncoidal packstone. Ga~nik on Vojsko plateau Mikrofacies mezozojskih karbonatnih kamnin Slovenije 81

Tabla 12 – Plate 12 82 Bojan OGORELEC

Tabla 13 – Plate 13

Zgornji trias (karnij) – Upper Triassic (Carnian)

1 Stromatolitni dolomit z izsu{itvenimi porami. V ve~ji 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 izsu{itvenimi porami, v katerih opazujemo dve generaciji cementa – obrobni cement A in sparitni kalcit B ter geopetalno strukturo internega mikrita. ^rna pri Ka- mniku Micritic limestone with shrinkage pores. Two generations of cement are present – rim cement A and sparry calcite B. Geopetal texture of internal micrite. ^rna at Kamnik

3 Plo{~ice ehinodermov (rde~e) 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. Š~ura nad Spodnjo Trebu{o Pelmicritic packstone. Micritic matrix is mostly washed. Š~ura above Spodnja Trebu{a

5 Sparitni dolomit. Pore, nastale pri dolomitizaciji apnenca, zapolnjuje sparitni kalcit (rde~e). Vzo- rec 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 Mikrofacies mezozojskih karbonatnih kamnin Slovenije 83

Tabla 13 – Plate 13 84 Bojan OGORELEC

Tabla 14 – Plate 14

Zgornji trias (cordevol) – Upper Triassic (Cordevolian)

1, 2 Selektivna dolomitizacija pizoida v biosparitnem grainstonu. Na sl. 2 pizoid pre~ka stilolitni {iv. 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 rde~e 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 dolomitization. Krma in Julian Alps

4 Moldi~no poro po neznanem organizmu v biosparitnem grainstonu zapolnjujeta obrobni dolomitni cement generacije A (beli evhedralni kristali), osrednji del pore pa sparitni kalcit (rde~e). 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 (rde~e) in prepreden z avtigenim 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. Le~a v grebenskem apnencu kamnoloma Lesno Brdo pri Vrhniki Dolosparite with euhedral conar crystals. Lens in reefal limestone of quarry Lesno Brdo at Vrh nika Mikrofacies mezozojskih karbonatnih kamnin Slovenije 85

Tabla 14 – Plate 14 86 Bojan OGORELEC

Tabla 15 – Plate 15

Zgornji trias (karnij) – Upper Triassic (Carnian)

1, 2 Ogrodje grebenskega apnenca sestavljajo ~lenkaste spongije vrste Alpinothalamia slovenica. Hu- dajužna Reef framework formed by encrusting sphyntozoan sponges Alpinothalamia slovenica. Hudajužna

3 Vzdolžni presek ~lenkaste 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 plo{~ica ehinoderma. Hu- dajužna Pyrite crystals in reefal spongiostromate limestone. Echinoid plate in upper right corner. Huda južna

5 Detajl vzdolžnega preseka ~lenkaste morske gobe Colospongia dubia v grebenskem apnencu. Hu- dajužna Detail of longitudinal section of sphyntozoan sponge Colospongia dubia in reefal framestone. Hu- dajužna

6 Pre~ni preseki korale Margarosmilia richthofeni v grebenskem apnencu tipa framestone. Corde- vol-jul. Pokljuka (zbirka D. Turn{ek) Transversal section of Margarosmilia richthofeni coral in reefal framestone. Cordevolian-Julian. Pokljuka (D. Turn{ek collection) Mikrofacies mezozojskih karbonatnih kamnin Slovenije 87

Tabla 15 – Plate 15 88 Bojan OGORELEC

Tabla 16 – Plate 16

Zgornji trias – karnij (jul in tuval) – Upper Triassic – Carnian (Julian and Tuvalian)

1,2 Onkoidno-ooidni grainstone s {tevilnimi bioklasti. Posamezni ooidi in fragmenti moluskov so inkrustirani s cianobakterijami. Apnenec je tudi delno piritiziran. Helenski potok pri Mežici, 2. klasti~ni 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 – plo{~ice ehinodermov. Helenski potok pri Mežici, 2. klasti~ni 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 plo{~ice 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 izsu{itvene pore, zapolnjene s sparitnim kalcitom. Dolenja Trebu{a - ^epovan Nonskeletal algae with filaments in stromatolitic layer. Numerous small fenestrae are cemented by sparry calcite. Dolenja Trebu{a - ^epovan Mikrofacies mezozojskih karbonatnih kamnin Slovenije 89

Tabla 16 – Plate 16 90 Bojan OGORELEC

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 pelagi~nih organizmov. Belca v zahodnih Karavan- kah Biomicritic packstone with radiolarians and pelagic filaments. Belca valley in western Karavan- ke Mts.

4 Biomikritni packstone s fragmenti moluskov in foraminiferami. Belca v zahodnih Karavankah Biomicritic packstone with mollusc fragments and foraminifers. Belca valley in western Karavan- ke 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. Mikrofacies mezozojskih karbonatnih kamnin Slovenije 91

Tabla 17 – Plate 17 92 Bojan OGORELEC

Tabla 18 – Plate 18

Zgornji trias (norij in retij) – Upper Triassic (Norian and Rhaetian) Medplimsko okolje – Intertidal environment

1, 2 Stromatolitni loferit z drobnimi izsu{itvenimi porami. Nekatere pore na sl. 1 so zapolnjene z internim mikritom. Sl. 1 – Grudnica pri ^epovanu, Sl. 2 – Begunj{~ica nad Ljubeljem Stromatolitic fenestral limestone – loferite. Some fenestra on fig. 1 are filled with internal micrite. Fig. 1 – Grudnica at ^epovan, Fig. 2 – Mt. Begunj{~ica above Ljubelj road pass

3, 4 Laminirana stromatolitna tekstura z ohranjeno strukturo cianobakterij. Sl. 3 in 4 - Dolenja Trebu{a - ^epovan Laminated stromatolitic texture with preserved cyanobacteria. Figs. 3 and 4 - Dolenja Trebu{a - ^epovan

5 Izsu{itvene pore v mikritni osnovi – loferit. Pore kažejo geopetalno strukturo z internim mikritom in gravitacijskim cementom (pu{~ice). 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 Mikrofacies mezozojskih karbonatnih kamnin Slovenije 93

Tabla 18 – Plate 18 94 Bojan OGORELEC

Tabla 19 – Plate 19

Zgornji trias (norij in retij) – Upper Triassic (Norian and Rhaetian) Medplimsko okolje – Intertidal environment

1 Stromatolitni dolomit. Izsu{itvene pore so bile v pozni diagenezi zapolnjene s sparitnim kalcitom (rde~e). Vzorec je obarvan z alizarinskim barvilom. Begunj{~ica nad Ljubeljem Stromatolitic dolomite. Shrinkage pores were filled by sparry calcite (red) during late diagenesis. Alizarin red staining. Mt. Begunj{~ica above Ljubelj road pass

2 Izsu{itvena pora v izpranem pelmikritnem packstonu. Poro zapolnjuje interni mikrit, gravitacijski cement (pu{~ica) in sparitni kalcit. Dachsteinski apnenec, Begunj{~ica Shrinkage pore in washed pelmicritic packstone. Pore is filled by internal micrite, gravitational cement (arrow) and sparry calcite. Dachstein limestone, Mt. Begunj{~ica

3 Mikritni mudstone z redkimi intraklasti in izsu{itvenimi porami – loferit. ^epovan Fenestral mudstone with rare intraclasts and shrinkage pores – loferite. ^epovan

4 Stromatolitni dolomit – bafflestone z izsu{itvenimi porami. Glavni dolomit. Borovnica Stromatolitic dolomite – bafflestone with shrinkage pores. Main dolomite. Borovnica

5 Laminiran dolomit z izsu{itvenimi razpokami, ki kažejo na medplimsko okolje in z drobnimi iz su{itvenimi 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 izsu{itvenimi 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 Mikrofacies mezozojskih karbonatnih kamnin Slovenije 95

Tabla 19 – Plate 19 96 Bojan OGORELEC

Tabla 20 – Plate 20

Zgornji trias (norij in retij) – Upper Triassic (Norian and Rhaetian)

1 Grainstone s {tevilnimi 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 Bo- vec

3 Izpran pelmikritni packstone z izsu{itvenimi porami – loferit. Pore zapolnjuje sparitni kalcit. Grudnica pri ^epovanu Washed pelmicritic packstone with shrinkage pores – loferite. Fenestrae are filled by sparry calcite. Grudnica at ^epovan

4 Laminiran dolomit z izsu{itvenimi 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. Javor{ki vrh na Trnovskem gozdu Section of algae (Solenopora) in washed intrabiomicritic limestone. Javor{ki vrh on Trnovski gozd

6 Rekristalizirani koraliti v pelmikritnem apnencu – framestone. Moldi~ne pore po koralitih zapolnjuje sparitni kalcit. Dachsteinski apnenec, ^epovan - Lokovec Coralite contours in recrystallized pelmicritic framestone. Moldic pores are cemented by sparry calcite. Dachstein limestone, ^epovan – Lokovec Mikrofacies mezozojskih karbonatnih kamnin Slovenije 97

Tabla 20 – Plate 20 98 Bojan OGORELEC

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 Ko~evju Vadose pisoids, encrusted by cyanobacteria. Sparry dolomite between the pisoids. Main dolomite. Koprivnik at Ko~evje

2 Vadozni pizoidi v intramikritnem dolomitu z izsu{itvenimi porami. Trenta Vadose pisoids in the intramicritic dolomite with shrinkage pores. Trenta

3 Ve~kratno prera{~anje algnega onkoida, inkrustiranega z ovoji cianobakterij. Glavni dolomit. Spodnja Trebu{a - ^epovan Multiple owergrowth of algal oncoide, encrusted by cyanobacteria. Main dolomite. Spodnja Tre bu{a - ^epovan

4 Onkoid v pelmikritnem packstonu, ki ga je zajela poznodiagenetska dolomitizacija. Begunj{~ica Algal oncoid in fenestral pelmicritic packstone, affected by late dolomitization. Mt. Begunj{~ica

5 Intramikritni dolomit z izsu{itvenimi porami (A) prehaja v horizont z vadoznimi pizoidi (B), te pa prera{~a stromatolitni bafflestone z izsu{itvenimi porami (C). Korozijske votline med pizoidi zapolnjuje ve~ generacij dolomitnega cementa (kokardna struktura). Glavni dolomit. Krn v Julijskih Alpah Intramicritic dolomite with shrinkage pores (A) pass to horizon with vadose pisoids (B), owergrown 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 Mikrofacies mezozojskih karbonatnih kamnin Slovenije 99

Tabla 21 – Plate 21 100 Bojan OGORELEC

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 calcite. Nomenj at Bohinjska Bistrica

3,4 Gastropodni grainstone. Hi{ice polžev so ohranjene po mikritnih ovojih. Dachstainski apnenec. ^epovan – Lokavec Gastropode grainstone. Gastropod shells are preserved after micritic envelopes. Dachstein limestone. ^epovan - Lokavec Mikrofacies mezozojskih karbonatnih kamnin Slovenije 101

Tabla 22 – Plate 22 102 Bojan OGORELEC

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 Borov nici Paleodasycladus mediterraneous algae in biosparitic grainstone. Preserje at Borovnica

3 Intrapelmikritni packstone z izsu{itvenimi porami. V ve~ji pori je viden gravitacijski cement (pu {~ica). Javor{ki vrh na Trnovskem gozdu Intrapelmicritic packstone with shrinkage pores. In a larger pore gravitational cement (arrow) is visible. Javor{ki vrh on Trnovski gozd

4 [kolj~ne lupine v intramikritnem packstonu. Dežnikasta poroznost pod lupino, pore zapolnjuje sparitni kalcit. Javor{ki vrh na Trnovskem gozdu Bivalve shells in intramicritic packstone. Umbrella porosity under some shells; pores are filled with sparry calcite. Javor{ki vrh on Trnovski gozd

5 Moldi~na poroznost po fragmentu debelolupinske {koljke v oosparitnem apnencu. Pora je zapolnjena s sparitnim kalcitom. Javor{ki vrh na Trnovskem gozdu Moldic porosity after thick-walled shell fragment in oosparitic limestone. The pore was later filled by sparry calcite. Javor{ki 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 Mikrofacies mezozojskih karbonatnih kamnin Slovenije 103

Tabla 23 – Plate 23 104 Bojan OGORELEC

Tabla 24 – Plate 24

Spodnja jura (lias) – Lower Jurassic (Lias)

1 Oolitni grainstone s {kolj~nimi lupinami, ki so na konveksni strani inkrustirane z ovoji cianobakterij. Dežnikasta poroznost pod lupinami {koljk. 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. Razli~na struktura ovojev (mikritna in radialna struktura kalcita). Gr~arevec – Kalce Ooids in micritic matrix – packstone. Micritic and radial-fibrous texture of ooid envelopes. Gr~arevec – Kalce

3 Oosparitni grainstone s teksturo »polmeseca«, ki je rezultat meteorske diageneze in izluževanja evaporitnih ali aragonitnih kristalov. Geopetalna struktura. Javor{ki 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. Javor{ki vrh on Trnovski gozd

4 Oosparitni grainstone z razli~no 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 plo{~ice ehinodermov. Javor{ki vrh na Trnov skem gozdu Oosparitic grainstone. Echinoid plates serve as nuclei in some ooids. Javor{ki vrh on Trnovski gozd

6 Sparitni dolomit z ohranjeno strukturo ooidov. Onek pri Ko~evju Sparry dolomite with preserved primary ooid structure. Onek at Ko~evje Mikrofacies mezozojskih karbonatnih kamnin Slovenije 105

Tabla 24 – Plate 24 106 Bojan OGORELEC

Tabla 25 – Plate 25

Spodnja jura (lias) – Lower Jurassic (Lias)

1 Oolitni apnenec – grainstone, ki ga je zajela selektivna poznodiagenetska dolomitizacija. Ta je osredoto~ena na mikritna jedra ooidov. Plo{~ice ehinodermov kot jedra nekaterih ooidov. Vrhpe~ pri Trebnjem Oolitic grainstone affected by selective late diagenetic dolomitization, focused on micritic nuclei of ooids. Echinoid plates in some ooid nuclei. Vrhpe~ at Trebnje

2 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

3 Detajl oosparitnega apnenca. Opazni sta dve generaciji cementa – obrobni cement A (pu{~ica) in sparitni kalcit B. Javor{ki vrh na Trnovskem gozdu Detail of oosparitic limestone. Two generations of cement – rim cement A (arrow) and sparry calcite are evident. Javor{ki vrh on Trnovski gozd

4 Oosparitni grainstone z zna~ilno me{ano 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

5 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)

6 Oosparitni grainstone s stalaktiti~nim cementom (pu{~ica) pod nekaterimi ooidi, ki kaže na diage- nezo v meteorskem okolju. Gr~arevec – Kalce Oosparitic grainstone. Stalactitic cement under some ooids (arrow) is indicating diagenesis in meteoric environment. Gr~arevec – Kalce Mikrofacies mezozojskih karbonatnih kamnin Slovenije 107

Tabla 25 – Plate 25 108 Bojan OGORELEC

Tabla 26 – Plate 26

Spodnja jura (lias) – Lower Jurassic (Lias)

1 Bioosparitni grainstone z ooidi, iglicami ehinodermov in rekristaliziranimi koraliti. Kozjak pri Dobrni~u (zbirka S. Dozeta) Bioosparitic grainstone with ooids, echinoid spines and recrystallized coralites. Kozjak at Dobrni~ (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.) Javor{ki vrh na Trnovskem gozdu Foraminifer in intrabiosparitic grainstone (transitional form from Mayncina sp. in Lituosepta sp.) Javor{ki vrh on Trnovski gozd

4 Lumakela drobnih brahiopodov v biosparitnem grainstonu. Javor{ki vrh na Trnovskem gozdu Lumachelle of fine brachiopod valves in biosparitic grainstone. Javor{ki vrh on Trnovski gozd

5 Rekristaliziran presek spongije – detajl. Kamnolom Vrhpe~ pri Trebnjem Section of recrystallized sponge – detail. Vrhpe~ quarry at Trebnje

6 Sparitni dolomit z odprtimi medzrnskimi porami, ki so nastale pri pozni dolomitizaciji kamnine. Prvotna oolitna tekstura je {e ohranjena. Bistra pri Vrhniki Sparry dolomite with open intergranular pores, formed during the late dolomitization. Primary oolitic structure is still evident. Bistra at Vrhnika Mikrofacies mezozojskih karbonatnih kamnin Slovenije 109

Tabla 26 – Plate 26 110 Bojan OGORELEC

Tabla 27 – Plate 27

Zgornja jura – Upper Jurassic

1 Biomikritni apnenec – packstone s {tevilnimi algami, moluski in ooidi. V ve~jih skeletih alg sta vidna stalaktiti~ni cement (pu{~ica) 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 Kra- jina (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 dolomitizacija. Vrhnika - Logatec Algae Clypeina jurassica in pelmicritic matrix. Limestone was affected by late diagenetic dolomitization. Vrhnika – Logatec Mikrofacies mezozojskih karbonatnih kamnin Slovenije 111

Tabla 27 – Plate 27 112 Bojan OGORELEC

Tabla 28 – Plate 28

Zgornja jura – Upper Jurassic

1 Biointrasparitni grainstone. Ve~ja {kolj~na lupina (pu{~ica) 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 prevle~eni z oolitnimi ovoji. Vrhnika - Logatec Intraoosparitic grainstone. Some intraclasts are coated with oolitic laminae. Vrhnika -Logatec

3 Intrapelmikritni packstone z izsu{itvenimi porami – loferit. Oolitni ovoji okrog ve~jih 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 (Sne- žni gri~) Intrabiosparitic packstone with large tintinnids. Vrhnika – Logatec, old road (Snežni gri~)

5 Intrapelmikritni packstone z izsu{itvenimi porami – loferit. Racna gora pri Ložu Intrapelmicritic fenestral packstone – loferite. Racna gora at Lož Mikrofacies mezozojskih karbonatnih kamnin Slovenije 113

Tabla 28 – Plate 28 114 Bojan OGORELEC

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. Turn{ek) Corallites of dendroid colonial coral Stylosmilia corallina. Malm, Kal nad Kanalom, negative imprint (D. Turn{ek collection)

2 Korala Dermosmilia laxata v mikritni osnovi. Zati{ni greben. Col na Trnovskem gozdu, negativni odtis (zbirka D. Turn{ek) Dermosmilia laxata coral in micritic matrix. Inner-reef facies. Col on Trnovski gozd, negative imprint (D. Turn{ek 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. Turn{ek) Section of Clausastraea pseudoconfluens coral. Kal nad Kanalom, negative imprint (D. Turn{ek collection)

5 Presek stromatoporoida Ellipsactinia. Tur{ki klanec na Trnovskem gozdu, negativni odtis Ellipsactinia stromatoporoid. Tur{ki klanec on Trnovski gozd, negative imprint Mikrofacies mezozojskih karbonatnih kamnin Slovenije 115

Tabla 29 – Plate 29 116 Bojan OGORELEC

Tabla 30 – Plate 30

Jura in spodnja kreda – Jurassic and Lower Cretaceous Globljemorski razvoj – Deeper-marine facies

1 Biomikritni packstone s {tevilnimi plo{~icami 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 mo~no okremenjena. Dogger-Malm. Bav{ica pri Bovcu. X nikoli Radiolaria-bearing spiculitic packstone. Micritic matrix is heavily silicified. Dogger-Malm. Bav{ica at Bovec. XN

3 Krinoidni packstone s plo{~icami ehinodermov. Dogger. Mangart Crinoidal packstone with echinoderm plates. Dogger. Mt. Mangart

4 Aptihi in kalpionele v mikritni osnovi – wackestone. Tithonij-berriasij. ^isti vrh v Trenti Aptychus-bearing wackestone with some calpionellids. Tithonian-Berriasian. ^isti vrh in Trenta

5, 6 Kalpionele v mikritni osnovi – wackestone. Na sl. 6 so prisotni {e radiolariji. Berriasij Calpionellid wackestone. In Fig. 6 some radiolarians are present too. Berriasian 5 - Vas na Skali v Trenti 6 - Bav{ica pri Bovcu Mikrofacies mezozojskih karbonatnih kamnin Slovenije 117

Tabla 30 – Plate 30 118 Bojan OGORELEC

Tabla 31 – Plate 31

Srednja jura (dogger) – Middle Jurassic (Dogger) Globljemorski razvoj, manganski horizont – Deeper-marine environment, manganese horizon

1 Manganove skorje obra{~ajo plo{~ico 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 plo{~icami ehinodermov, drobci {kolj~nih 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. Plo{~ice ehinodermov so obdane z manganovimi ovoji. Dolina Triglavskih jezer Crinoidal packstone. Echinoderm plates with manganese encrustations. Triglav lakes valley Mikrofacies mezozojskih karbonatnih kamnin Slovenije 119

Tabla 31 – Plate 31 120 Bojan OGORELEC

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 {tevilnimi pre~nimi 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 problemati~nim mikrofosilom Bacinella irregularis. Barremij. Svi{~aki pod Snežnikom Microproblematic fossil Bacinella irregularis in biomicritic limestone. Barremian. Svi{~aki 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 Mikrofacies mezozojskih karbonatnih kamnin Slovenije 121

Tabla 32 – Plate 32 122 Bojan OGORELEC

Tabla 33 – Plate 33

Spodnja kreda – Lower Cretaceous

1 Dolomitni romboedri s conarno rastjo v mikritnem apnencu. Poznodiagenetska dolomitizacija. Valanginij. Ko~evski Rog – Podturn Dolomite rhombohedrons with porphyrotopic zonar fabrics in micritic matrix. Late diagenetic dolomitization. Valanginian. Ko~evski Rog – Podturn

2 Stromatolitni apnenec – bindstone z izsu{itvenimi porami. Aptij. Snežnik Stromatolitic boundstone with shrinkage pores. Aptian. Mt. Snežnik

3 Intraoosparitni packstone. Jedra ve~ ooidov predstavljajo foraminifere. Albij. Nadrt na Hru{ici (zbirka J. Ježa) Intraoosparitic packstone. Foraminifers as nuclei in some ooids. Albian. Nadrt on Hru{ica (J. Jež collection)

4 Biomikritni mudstone/wackestone z lupinami ostrakodov. Albij. Nadrt na Hru{ici (zbirka J. Ježa) Biomicritic mudstone/wackestone with ostracod slells. Albian. Nadrt on Hru{ica (J. Jež collection)

5 Koraliti grebenske korale Dermosmilia cretacica. Barremij – sp. aptij. Osojnice na Banj{ki planoti (zbirka D. Turn{ek) The colony of reef-forming coral Dermosmilia cretacica. Barremian – Lower Aptian. Osojnice on Banj{ice plateau (D. Turn{ek collection)

6 Laminiran mikritni apnenec z neizrazito stromatolitno strukturo in s stilolitnimi {ivi. Valanginij. Dvor pri Žužemberku Laminated micritic limestone with indistinctive stromatolitic texture and stylolites. Valanginian. Dvor at Žužemberk Mikrofacies mezozojskih karbonatnih kamnin Slovenije 123

Tabla 33 – Plate 33 124 Bojan OGORELEC

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 izsu{itvene pore. Cenomanij. Nadrt na Hru{ici (zbirka J. Ježa) Washed intrabiopelmicritic packstone with rare shrinkage pores. Cenomanian. Nadrt on Hru{ica (J. Jež collection)

5 Oolitni boksit. Santonij – turonij. Nanos – Podra{ka bajta (zbirka J. Ježa) Oolitic bauxite. Santonian – Turonian. Mt. Nanos – Podra{ka bajta (J. Jež collection)

6 Foraminiferni miliolidni apnenec – packstone. Santonij (Lipi{ka formacija). Rodik pri Kozini Foraminiferal miliolid packstone. Santonian (Lipica Formation). Rodik at Kozina Mikrofacies mezozojskih karbonatnih kamnin Slovenije 125

Tabla 34 – Plate 34 126 Bojan OGORELEC

Tabla 35 – Plate 35

Zgornja kreda – Upper Cretaceous

1 Izpran biopelmikritni packstone s foraminifero Dicyclina schlumbergeri. Santonij – campanij (Lipi{ka formacija). Gabrk pri Sežani Foraminifer Dicyclina schlumbergeri in washed biopelmicritic packstone. Santonian – Campanian (Lipica Formation). Gabrk at Sežana

2 Izpran miliolidni packstone. Santonij – campanij (Lipi{ka formacija). Gabrk pri Sežani Washed miliolid packstone. Santonian – Campanian (Lipica Formation). Gabrk at Sežana

3 Mikritni apnenec – mudstone z izsu{itvenimi porami – loferit. Maastrichtij (Liburnijska formacija). Suhadole pri Štorjah Mudstone with shrinkage pores – loferite. Maastrichtian (Liburnia Formation). Suhadole at Štorje

4 Mo~no izpran mikritni apnenec – packstone. Maastrichtij (Liburnijska formacija). Vremski Britof Washed micritic packstone. Maastrichtian (Liburnia Formation). Vremski Britof

5, 6 Algni wackestone s {tevilnimi preseki vrste Decastronema (ex. Aeolisaccus) kotori (sl. 5) in D. barattoloi (sl. 6) ter posamezne foraminifere (Fleuryana adriatica). Turonij – Santonij (Sežan- ska 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) Mikrofacies mezozojskih karbonatnih kamnin Slovenije 127

Tabla 35 – Plate 35 128 Bojan OGORELEC

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 {koljk. Coarse-grained biocalcarenite, composed of rudist shell fragments. 2 - Turonij /Turonian. Kopriva pri Dutovljah 3 - Cenomanij/Cenomanian. Nadrt na Hru{ici (zbirka/collection of J. Jež)

4 Biopelmikritni packstone s {tevilnimi 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 {tevilnimi kalcisferami in posameznimi pelagi~nimi 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 fli{no bre~o. Kanalski Lom na Banj{icah (zbirka D. Turn{ek) Eugyra lanckoronensis coral of Aptian age, resedimented into Upper Cretaceous flysch breccia. Kanalski Lom on Banj{ice plateau (D. Turn{ek collection) Mikrofacies mezozojskih karbonatnih kamnin Slovenije 129

Tabla 36 – Plate 36 130 Bojan OGORELEC

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 / Škrbina at Komen

3 Biomikritni apnenec – wackestone z miliolidami in drugimi foraminiferami (Pastrikella balcanica), bogat z organsko snovjo. Cenomanij. Toma~evica pri Komnu Biomicritic wackestone with miliolids and other foraminifers (Pastrikella balcanica), rich in organic matter. Cenomanian. Toma~evica 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 parvovesiculifera in foraminiferami. Coniacij Intramicritic packstone with organic matter, algae Thaumatoporella parvovesiculifera and foraminifers. Coniacian 5 - Skopo pri Dutovljah / Skopo at Dutovlje 6 - Konjske stope pri Tomaju Mikrofacies mezozojskih karbonatnih kamnin Slovenije 131

Tabla 37 – Plate 37 132 Bojan OGORELEC

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 {tevilnimi 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 (pre~ni 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 {tevilnimi 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. Microco dium). Pedogenic carbonate with rhizoids. Cretaceous/Tertiary boundary. Sopada at Sežana

6 Intramikritni apnenec z ve~jimi izsu{itvenimi porami, v katerih nastopa stalaktiti~ni cement. Kredno/terciarna meja. Štorje pri Sežani Intramicritic limestone. Stalactitic calcite cement in some shrinkage pores. Cretaceous/Tertiary boundary. Štorje at Sežana Mikrofacies mezozojskih karbonatnih kamnin Slovenije 133

Tabla 38 – Plate 38 134 Bojan OGORELEC

Tabla 39 – Plate 39

Kreda – Cretaceous Globljemorski razvoj – Deeperwater environment

1 Spikulit – mo~no okremenjen mikritni packstone s {tevilnimi 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 {tevilnimi globotrunkanami, drobirjem pelagi~nih foraminifer in kalcisferami. Senon Foraminiferal wackestone with numerous globotruncanas, pelagic foraminifers debris and calcispheres. Senonian 3 - Koritnica pri Bovcu / Koritnica at Bovec 4 - Vol~anski apnenec. Kolovrat nad Tolminom / Vol~e limestone. Kolovrat above Tolmin

5 Biokalkarenit z odlomki rudistnih lupin in ehinodermov, redka drobna zrna terigenega kremena. Bazalni del plasti Vol~anskega apnenca. Senon. Drežnica pri Kobaridu Biocalcarenite, composed of rudist fragments, echinoderm plates and some terrigenous quartz grains. Basal part of Vol~e limestone beds. Senonian. Drežnica at Kobarid

6 Radiolarijski packstone – radiolarit. Albij. Bav{ica pri Bovcu Radiolarian packstone – radiolarite. Albian. Bav{ica at Bovec Mikrofacies mezozojskih karbonatnih kamnin Slovenije 135

Tabla 39 – Plate 39