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Triasni Konodonti Slovenskega Bazena GEOLOGIJA 50/1, 19–28, Ljubljana 2007 doi:10.5474/geologija.2007.002 Triasni konodonti Slovenskega bazena Triassic conodonts of the Slovenian Basin † Stanko BUSER1, Tea KOLAR-JURKOVŠEK2 & Bogdan JURKOVŠEK2 1Univerza v Ljubljani, NTF – Oddelek za geologijo, Privoz 11, 1000 Ljubljana; 2Geolo{ki zavod Slovenije, Dimi~eva ulica 14, 1000 Ljubljana, tea.kolar�geo-zs.si, bogdan.jurkovsek�geo-zs.si Klju~ne besede: konodonti, trias, Slovenski bazen, Slovenija Key words: conodonts, Triassic, Slovenian Basin, Slovenia Izvle~ek Slovenski bazen je nastal v ladiniju po razpadu enotne Slovenske karbonatne platfor- me in je trajal neprekinjeno do zgornje krede. V triasnih plasteh Slovenskega bazena so bile ugotovljene {tevilne konodontne zdru`be. Stratigrafsko pomembne vrste pripadajo rodovom Budurovignathus, Epigondolella, Gladigondolella, Metapolygnathus, Misikella, Neogondolella, Nicoraella, Norigondolella in Paragondolella. Abstract Slovenian Basin was formed during the Ladinian following disintegration of the Slo- venian Carbonate Platform. It persisted continuously until the Late Cretaceous. Several conodont asscociations were recognized within the Triassic rocks of the Slovenian Basin. Stratigraphically significant species belong to the genera Budurovignathus, Epigondolel- la, Gladigondolella, Metapolygnathus, Misikella, Neogondolella, Nicoraella, Norigondo- lella and Paragondolella. Uvod bazen v dolini So~e zahodno od Tolmina iz- klinil v obliki ozkega jarka. Tu sta od spod- Slovenski bazen je prvi zasledil v zahod- nje jure naprej neposredno mejili Dinarska nem delu Slovenije oziroma na meji med karbonatna platforma, ki se nadaljuje v so- Italijo in Slovenijo Cousin (1973). Kasneje sednjo Italijo kot Friuli platforma, in Julij- je Buser (1989) dognal, da se bazen proti ska karbonatna platforma, ki se nadaljuje v vzhodu {iri skoraj preko celotne osrednje Italiji kot Trento platforma brez vmesnega Slovenije. Sprva je prevladovalo mnenje, bazena. V vzhodnem delu Slovenije, kjer da se je bazen nadaljeval {e dlje proti zaho- dose`e Slovenski bazen najve~jo {irino in du v sosednjo Italijo v Belluno bazen, proti globino, pa se je nadaljeval preko Hrva{ke vzhodu pa naj bi imel zvezo z Bosanskim severno od Zagreba~ke gore na sosednjo bazenom (Buser, 1989; Haas et al., 1995). Mad`arsko. Dana{nji na povr{ini odkriti Domnevno prekinitev Slovenskega bazena sedimenti Slovenskega bazena se pojav- na zahodu smo tolma~ili s tem, da je zveza z ljajo v smeri vzhod–zahod na dol`ini okoli Belluno bazenom na povr{ini pokrita z na- 170 km in {irini do 40 km (slika 1). rinjenimi deli Julijskih Alp (Buser, 1986). S konodontnimi raziskavami triasnih Kasnej{e objave (Buser & Debeljak, sedimentov Slovenskega bazena je bilo ugo- 1996; Buser, 1996, 2003) navajajo, da se je tovljeno 45 biostratigrafsko pomembnih 20 † Stanko Buser, Tea Kolar-Jurkov{ek & Bogdan Jurkov{ek Slika 1. Dana{nji polo`aj geotektonskih enot v zahodni in osrednji Sloveniji in raz{irjenost sedimentov nekdanje Julijske in Dinarske karbonatne platforme ter Slovenskega bazena. Figure 1. Actual position of geotectonic units in western and central Slovenia with extension of the sediments of the ancient Julian and Dinaric Carbonate Platforms and the intermediate Slovenian Basin, respectively. vrst, ki pripadajo rodovom Budurovignat- in svetlo sivi gomoljasti apnenci tipa Han hus, Epigondolella, Gladigondolella, Meta- bulog, ki naznanjajo za~etek kasnej{ega po- polygnathus, Misikella, Neogondolella, Ni- polnega razpada karbonatne platforme. V coraella, Norigondolella in Paragondolella. bazenskih sedimentih osrednje Slovenije je bila pri Polhovem Gradcu najdena bogata anizijska amonitna favna (Petek, 1998). Pregled konodontnih raziskav triasnih Anizijske plasti z amoniti, konodonti in plasti Slovenskega bazena radiolariji so znane tudi iz jugovzhodnega dela Slovenskega bazena iz okolice Mir- V zgornjem permu je nastala na prosto- ne, Mokronoga in Novega mesta (Kühn & ru dana{nje Slovenije obse`na Slovenska Ramov{, 1965; Krivic & Premru 1976; karbonatna platforma, ki je bila stabilna Kolar-Jurkov{ek, 1983; Ramov{, 1983, do zgornjega anizija (Buser, 1989). V zgor- 1998c). Na {ir{em, idrijskem prostoru je bila njem aniziju je pri~elo ob dolgih regional- s konodotnti dokazana ilirska podstopnja nih prelomih razlamljanje (slika 2). Na njej (Kolar-Jurkov{ek, 1983, 1991). Nekoliko so se {e naprej odlagale karbonatne kamni- mlaj{i so apnenci na [marni gori pri Ljub- ne, v globokih vmesnih jarkih pa rde~kasti ljani, ki vsebujejo ilirsko do spodnjeladi- Triasni konodonti Slovenskega bazena 21 nijsko konodontno in radiolarijsko zdru`bo poredkih mestih so ostali {e naprej manj- (Ramov{ & Gori~an, 1995). {i ostanki nekdanje karbonatne platforme. Idrijska tektonska faza je v ladiniju pov- Najgloblje pogreznjen predel je bil na ob- zro~ila tektonski razpad Slovenske karbo- mo~ju osrednje Slovenije, ki predstavlja natne platforme (Buser, 1980). Nekateri za~etek kasnej{ega Slovenskega bazena. V predeli so bili globoko pogreznjeni pod globljem morju so nastajale psevdoziljske morje, nekateri pa so postali kopno. Le na plasti, ki jih sestavlja menjavanje skrilavih Slika 2. Paleogeografski razvoj Slovenskega bazena Figure 2. Paleogeographic evolution of Slovenian Basin 22 † Stanko Buser, Tea Kolar-Jurkov{ek & Bogdan Jurkov{ek glinavcev, drob in tufov, s poredkimi plastmi glinavcev, kremenovih pe{~enjakov in drob. temno sivega apnenca. Psevdoziljske plasti Ime so dobile po brahiopodu rodu Amphic- v vzhodnem delu Posavskih gub vsebujejo lina (Kossmat, 1910). Te plasti so podobne konodonte (Kolar-Jurkov{ek & Placer, psevdoziljskim ladinijskim plastem, vendar 1987; Placer & Kolar-Jurkov{ek, 1990; v njih ni ne tufov in ne primarnih riolitov, Kolar-Jurkov{ek & Ri`nar, 2006). Ko- andezitov in bazaltov. V spodnjem delu am- nodonti so pogostni tudi v plastovitih in fiklinskih plasti so nastali ob robu bazena plo{~astih apnencih osrednjega dela Slove- temno sivi masivni grebenski apnenci, ki jih nije, ki jih marsikje spremljajo zelene tuf- v ni`jih delih sestavljajo {tevilne spongije ske plasti »pietra verde« (Ramov{, 1997). (Senowbari-Daryan, 1981), navzgor pa V teh plasteh so pogostne pozidonije in da- prevladujejo korale (^ar et al., 1981, Turn- onele (Jurkov{ek, 1983, 1984). Zna~ilne {ek et al., 1982; 1984; Turn{ek, 1997). V ladinijske zdru`be so znane iz {ir{ega idrij- zgornjem delu amfiklinskih plasti se me- skega prostora (Kolar-Jurkov{ek, 1991), njavajo klastiti s skladnatimi apnenci. V iz okolice Ljubljane (Ramov{, 1977, 1985a, apnencih so bile v {tevilnih lokalitetah med 1994b, 1997; Krivic & Stojanovi~, 1978; Tolminom, Cerknim in [kofjo Loko ugotov- Kolar-Jurkov{ek, 1991) ter iz vzhodnga ljene zna~ilne karnijske zdru`be konodon- dela Jelovice pri Kropi, kjer se pojavljajo tov, od katerih je ve~ina tuvalskih, nekatere skupaj z daonelami in bogato radiolarijsko pa segajo {e v norij (Flügel & Ramov{, zdru`bo (Skaberne et al., 2003). 1970; Krivic, 1977; Krivic & Buser, V sedimentih globjevodnih jarkov, ki so 1979; Kolar-Jurkov{ek, 1982a; Ramov{, segali na prostor nastajajo~e Julijske kar- 1994a, 1998a, 1998b). bonatne platforme, so bile v Gorenji Trenti V osrednji in vzhodni Sloveniji dobimo ter na Pokljuki v ladinijskih plasteh ugo- v karniju Slovenskega bazena temno sive tovljene zdru`be daonel (Ramov{ & Jur- skladnate mikritne apnence z ve~ ali manj kov{ek, 1983), radiolarijev in konodontov tankimi polami laporja, ki ponekod vsebu- (Gori~an & Kolar-Jurkov{ek, 1984; jejo konodonte (Kolar-Jurkov{ek, 1994). Kolar-Jurkov{ek, 1989; Gori~an & Bu- Na poredkih mestih so bili v teh apnencih ser, 1990), iz ju`nega obrobja bazena pa so najdeni amoniti (Kühn & Ramov{, 1965), bili na Blokah, ju`no od Ljubljane najde- zahodno od Celja, na Kozjanskem in na Do- ni fassanski konodotni elementi (Ramov{, lenjskem pa ladinijsko-karnijski konodon- 1996). ti (Krivic, 1978; Ramov{, 1978; Kolar- Na dvignjenih kopnih predelih so takrat Jurkov{ek, 1982b, 1990, 1991). nastali pisani konglomerati. V Idriji je v la- Proti severu so se v karniju iz Slovenske- diniju na obmo~jih jarkov z vmesnimi hor- ga bazena na Julijsko karbonatno platfor- sti nastalo svetovno znano hidrotermalno mo zajedali globljemorski intraplatformni sinsedimentarno `ivosrebrovo rudi{~e. Ver- jarki, ki so {e posebno pogostni v Julijskih jetno pa so takrat nastala {e nekatera druga Alpah in Ju`nih Karavnkah ter v Kamni- rudi{~a. {ko-Savinjskih Alpah. V teh jarkih so se od- Koncem ladinija ali v za~etku karnija je lagali beli do temno sivi mikritni apnenci, nastopilo obdobje kompakcije. Osrednje ob- ki poleg raznovrstnih mikro- in makrofosi- mo~je Slovenije je ostalo {e naprej globoko lov vsebujejo tudi konodonte (Kolar, 1979; pogreznjeno in je pre{lo v Slovenski bazen. Jurkov{ek et al., 1984; Ramov{, 1985b; Vulkanizem je popolnoma zamrl. Severno Jamnik & Ramov{, 1993; Jurkov{ek & od globokomorskega obmo~ja je nastala sta- Kolar-Jurkov{ek, 1986; Kolar-Jurkov- bilna Julijska karbonatna platforma, ki za- {ek, 1982b, 1991; Kolar-Jurkov{ek & jema dana{nje ju`ne Karavanke, Julijske in Jurkov{ek, 1997, 2003; Dobruskina et Kamni{ko-Savinjske Alpe. Ju`no od Sloven- al., 2001; Jurkov{ek et al., 2003; Kolar- skega bazena pa je nastala Dinarska (=Ja- Jurkov{ek et. al., 2005). dransko-Dinarska) karbonatna platforma, Norij in retij sta pomenila za Slovenski ki je danes sestavni del Zunanjih Dinaridov. bazen stabilno obdobje. Nivo morja se je V zahodnem delu Slovenskega bazena, to je precej dvignil, na celotnem prostoru bazena v okolici Tolmina, so nastali v karniju tem- so nastali enaki
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