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MORAVSKOSLEZSKÉ PALEOZOIKUM 2008 XII. Ročník MORAVSKOSLEZSKÉ PALEOZOIKUM 2008 XII. ro čník BRNO 14. ÚNOR 2008 Obrázek na p řední stran ě: Čert ův most v Suchém žlebu, Moravský kras. Lažánecké vápence macošského souvrství, st řední devon, givet. Kolorovaná xylografie E. Herolda z r. 1875 (archiv A. P řichystala). Ústav geologických v ěd P řírodov ědecké fakulty Masarykovy univerzity Česká geologická spole čnost, pobo čka Brno Česká geologická služba, pobo čka Brno MORAVSKOSLEZSKÉ PALEOZOIKUM 2008 Sborník abstrakt ů Edito ři: Lukáš K rmí ček, Michaela Halavínová a Vojt ěch Šešulka BRNO 2008 Obsah David Buriánek: VÝVOJ PERALUMINICKÝCH GRANIT Ů PROSTOROV Ě SVÁZANÝCH S TŘEBÍ ČSKÝM PLUTONEM ............................................................................................................................................4 Zden ěk Dolní ček a Marek Slobodník NOVÝ NÁLEZ KALCITOVÉ MINERALIZACE S UHLOVODÍKY V LOMU CEMENTÁRNY V HRANICÍCH ............................................................................................................................................5 Ladislav Dvo řák a Ji ří Kalvoda MOKRÁ – VÝZNAMNÁ LOKALITA PRO ROZPOZNÁNÍ BÁZE VISÉ ......................................................6 Helena Gilíková, Jind řich Hladil, Jaromír Leichmann a František Pato čka CO JIŽ VÍME O SEDIMENTECH KAMBRIA V JIŽNÍ ČÁSTI BRUNOVISTULIKA ....................................7 Lukáš Krmí ček: GENEZE A VÝZNAM HERCYNSKÝCH ULTRADRASELNÝCH LAMPROFYR Ů ŽELEZNÝCH HOR ..................................................................................................................................8 Tomáš Lehotský: NOVÉ PALEONTOLOGICKÉ VÝZKUMY LOKALITY STÍNAVA – VÍKENDOVÝ DOMEK, PŘEDB ĚŽNÁ ZPRÁVA..........................................................................................................................10 Tomáš Lehotský: REVIZE GONIATITOVÉ FAUNY MORAVICKÉHO SOUVRSTVÍ NÍZKÉHO JESENÍKU (SPODNÍ KARBON, ČESKÝ MASIV) .....................................................................................................11 Št ěpán Rak: AUTEKOLOGIE TRILOBITOVÝCH TAXON Ů Z LOMU MOKRÁ U BRNA (TOURNAI-VISÉ)...................13 Miloš René: AMFIBOLY T ŘEBÍ ČSKÉHO PLUTONU ................................................................................................14 Vojt ěch Šešulka a Lukáš Krmí ček: VYUŽITÍ POZEMNÍ CS – MAGNETOMETRIE P ŘI DETAILNÍM GEOLOGICKÉM PR ŮZKUMU .............15 Marek Slobodník, Ond řej Peša a Antonín P řichystal: (PŘEKVAPIVÝ) CHARAKTER FLUID Z INKLUZÍ V K ŘIŠ ŤÁLECH NA PUKLINÁCH KVARCIT Ů Z JEGŁOWE, SILEZIKUM ........................................................................................................................16 Vladimír Vrobel a Rostislav Melichar: TEKTONICKÁ POZICE DEVONSKÉHO RELIKTU V HORNINÁCH BRN ĚNSKÉHO MASIVU V JIŽNÍ ČÁSTI M ĚSTA BRNA...................................................................................................................17 Auto ři zodpovídají za odbornou nápl ň a jazykovou úrove ň svých p řísp ěvk ů Moravskoslezské paleozoikum 2008 Sborník abstrakt ů 4 VÝVOJ PERALUMINICKÝCH GRANIT Ů PROSTOROV Ě SVÁZANÝCH S TŘEBÍ ČSKÝM PLUTONEM David Buriánek Česká geologická služba, Leitnerova 22, 658 59, Brno, [email protected] Durbachity t řebí čského plutonu bývají provázeny řadou typ ů peraluminických granit ů, které tvo ří drobná t ělesa a žíly. Tyto taveniny jsou jedním z projev ů pom ěrn ě rozsáhlé plutonické aktivity v oblasti moldanubika svázané s variskou orogenezí. Tyto granity m ůžeme roz členit na dv ě hlavní skupiny: turmalinické granity a biotitické granity. Muskovit biotitické až muskovitické granity s rozptýleným turmalínem (DTG) nebo s nodulárním turmalínem (NTG) se vyskytují hlavn ě v st řední a severní části t řebí čského plutonu. Tvo ří žíly a drobná tělesa často prorážející durbachity. Geologická pozice dob ře koresponduje s jejich stá řím 320 až 314 Ma, které bylo ur čeno datováním monazit ů metodou CHIME. Z akcesorických minerál ů je p řítomen apatit, zirkon, monazit, n ěkdy kasiterit. V obou skupinách turmalinických granit ů (NTG a DTG) mají křivky REE podobný tvar, ale liší se koncentracemi. Chování REE je ve všech typech turmalinických granit ů řízeno frakcionací stejných minerál ů, p ředevším monazitu, zirkonu a apatitu. Vysoké pom ěry Rb/Sr v horninách DTG jsou typické pro horniny derivované dehydrata čním tavením muskovitu. Naopak nižší hodnoty Rb/Sr u NTG nazna čují, že se na jejich vzniku podílelo spíše dehydrata ční tavení biotitu. Dalším vysv ětlením pro rozdílné chemické složení obou skupin turmalinických granit ů m ůže být frak ční krystalizace. Druhou skupinou hornin jsou biotitické granity (BG) n ěkdy s granátem, které vystupují hlavn ě na jižním okraji t řebí čského plutonu. Datování monazit ů v granitech a mafických enklávách, které jsou v nich obsaženy poskytlo shodné v ěky kolem 323 Ma (metodou CHIME). Granitová tavenina byla derivovaná z biotitem bohatých metapsamit ů. Skute čnost že jde o typickou korovou taveninu indikuje chemické složení granit ů a častá p řítomnost granátu a silimanit ů. Avšak zárove ň tyto granity obsahují mafické enklávy. Chemické složení mafických enkláv (Ni, Cr, Mg, REE) nazna čuje, že jde o materiál podobný durbachit ům. Enklávy leží svým chemickým složením mezi durbachity a granity. Jsou jemnozrnné a n ěkdy nesou známky asimilace granitovou taveninou. Jejich tvar a charakter nazna čuje že jsou produktem míšení mezi korovou taveninou granitu a taveninou geneticky velmi blízkou durbachit ům. Izotopické a chemické složení granit ů také nazna čuje že byly částe čně ovlivn ěny interakcí s taveninou durbachitového složení. Tyto granity se po stránce chemické i mineralogické mírn ě odlišují od typických peraluminických granit ů prostorov ě svázaných s t řebí čským plutonem. Období vzniku obou skupin granit ů se kryje s obdobím výrazné magmatické aktivity v oblasti moldanubického plutonu (intruze post-orogenních granitoid ů). Intruze turmalinických granit ů souvisí s extenzí a dehydrata čním tavením metamorfních sérií moldanubika. Biotitické granity (BG) vznikaly v podobném tektonickém režimu. Vznikly krystalizací tavenin generovaných dehydrata čním tavením biotitu patrn ě ve st řední k ůř e. Jejich vznik byl iniciován intruzí taveniny durbachitového složení. Mezi ob ěma magmaty došlo v omezené mí ře k interakci a míšení. Dekompresní reakce, p ři níž vznikal v granitech na úkor granátu cordierit a biotit, prob ěhly v d ůsledku snížení tlaku a teploty b ěhem pom ěrn ě rychlého výstupu k povrchu. Po svém vmíst ění do dnešní pozice se v záv ěre čných stádiích magmatické krystalizace uvolnilo malé množství zbytkové taveniny a fluida. V durbachitech p ři kontaktu s granity byly nahrazeny amfiboly a pyroxeny biotitem, a to v d ůsledku interakce s fluidy uvoln ěnými p ři krystalizaci granit ů (BG). Nejmladší tavenina je representována granity, které tvo ří drobné žíly s neostrým okrajem. Tyto granity p ředstavují pozdní taveninu derivovanou z biotitických granit ů. Stejný původ patrn ě má v ětšina pegmatitových žil. Pozdní tavenina byla obohacena bórem a vodou, obsahy fluoru byly patrn ě relativn ě nízké, jak ukazuje chemické složení turmalínu. Práce byla vypracována s finan ční podporou grantového úkolu GA ČR 205/05/P223: Geneze peraluminických granit ů moldanubika. Moravskoslezské paleozoikum 2008 Sborník abstrakt ů 5 NOVÝ NÁLEZ KALCITOVÉ MINERALIZACE S UHLOVODÍKY V LOMU CEMENTÁRNY V HRANICÍCH Zden ěk Dolní ček 1 a Marek Slobodník 2 1 Katedra geologie P řF UP, t ř. Svobody 26, 771 46 Olomouc, ČR, [email protected] 2 Ústav geologických v ěd P řF MU, Kotlá řská 2, 611 37 Brno, ČR, [email protected] Ve vápencovém lomu v Hranicích byly nalezeny hydrotermální kalcity s uhlovodíky ve fluidních inkluzích. Kalcity tvo ří výpl ň nepravidelných puklin nebo tmel brekciovaných devonských vápenc ů. Ojedin ěle byl zaznamenán i kontakt s nezpevn ěnými sedimentárními výpln ěmi krasových kapes. Monominerální hrubozrnné kalcitové výpln ě dosahují mocnosti až 5 cm. Starší kalcit I je medov ě žlut ě zbarvený, mladší kalcit II je bezbarvý a vytvá ří zrnité agregáty či drúzovité povlaky. Kalcit I je chudý na stopové prvky. T ěžké kovy a REE jsou pod mezí stanovitelnosti nebo jen t ěsn ě nad ní (0,X-X ppm). Vyšší obsahy byly zaznamenány pouze u Ba (14 ppm) a Sr (340 ppm). Pom ěr LREE/HREE je pro chondritem normalizovanou k řivku REE vyrovnaný, u prvk ů La-Ce-Pr-Nd je nazna čen W-tetrádový efekt a chybí pozitivní Eu anomálie. Fluidní inkluze v kalcitu I jsou trojího typu. Typ 1 jsou jednofázové inkluze s vodným roztokem, což indikuje nízké teploty vzniku (pod ~50 °C). Dvoufázové inkluze (L+V) jsou v kalcitu I vzácné. Kryometrická m ěř ení prokázala H 2O-NaCl (± MgCl 2 ± CaCl 2) typ fluid a nižší salinitu uzav řených roztok ů (0,9 až 5,3 hm. % NaCl ekv.). Krom ě tání ledu (Tm = -3,2 až -0,5 °C) bylo pozorováno v některých inkluzích typu L+V i tání další pevné fáze (klathrátu?) za teplot -7,5 až -4,2 °C. Inkluze typu 2 jsou málo pr ůhledné, tmavé a vypln ěné uhlovodíky, které mají modrou fluorescenci v UV zá ření. Inkluze typu 3 obsahují vodný roztok, uhlovodíky a p říp. i plynnou fázi. Kalcit II obsahuje v inkluzích jen vodný roztok s velmi nízkou salinitou (<1 hmot. % NaCl ekv.). Hodnoty δ13 C kalcit ů I a II jsou -10,3 a -1,1 ‰ PDB, hodnoty δ18 O -6,0 a -7,3 ‰ PDB. Vypo čtené izotopické složení kyslíku roztoku ukazuje na p ůvod v mo řské vod ě (kalcit I, δ18 O = -2,2 až +1,5 ‰ SMOW) a meteorické vod ě ( δ18 O = -5,0 až -1,3 ‰ SMOW, kalcit II). Vypo čtené hodnoty δ13 C fluid ukazují na v ětší uplatn ění uhlíku z organické hmoty ve starší fázi (kalcit I: δ13 C
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