sign in sign up
<<
Home , Karawanks

Iìirist:r ftrli.rnr di l',rlri,nrolo:i.r c \rrùi:r.rli,r \olunr. Ila J pls. pp.6ir)-679 Decenrbcr li0{

ANISIAN TERRESTRIAL SEDIMENTS IN THE BÙKK MOUNTAINS (NE HUNGARY) AND THEIR ROLE IN THE TRIASSIC RIFTING OF THE VARDAR-MELIATA BRANCH OF THE NEO-TETHYS OCEAN

I. EI-ICITASZ VI.,LLEDITS

R..tirùl ()rtu!,et )1.:::i:..(tt:t'td lnh t.;. )iîJ

Ào ;or1l: Bùkk \irs.. hLc scdinrrnrs. il!\ilil. ..Jinr(rrr. crntsrdinrcnr.rrir chc è c.rr.rttcrisrìe.r tlelh prrrc lilcvrrr in un conre- br,rìclcd rìvcl l,.rli grrbrn. riitinr, S,,LLrhern Alt\. Dirrfi(1(\. sr<, Lli riltìng. I seclinrcnricontinenr.rli delh porzione nrcLiclionrlc deile nron!rgne f.rppfr\entino l.r p;rrte pìir prcilond:r

B;rscrl on rhe s t rr i!f.ìphic.Ì l positìon,rni1 rricrol.rci* rn.rlvs.r ot rhc resrilinrenred gr.rin., r" o rerr,:.rri.rì er int. crn hc Introduction eil. l he rge oi thc r ourì{(r is lìrt l).ln),ìixn c.rrlr llh rì,rni. l his c.rn [c colrcl,rred rith the Rì,:hrhoierr Corrglonerrr, in rhe Di,L,mitcs. Thc Anis jlrr tcrresrri:rl sedjnrcnts rvitìrin thick platfornt rgc r,f Lhc old. r rcrrcsrri,rl ctnr coultl nor bc ert.rblishccl L r.rcrh brr ir crrbon;ltc sLrcccssions are $.cll-known in rhe mu:t h,rr,: h.rppcned cither il rhr Irelstrri.ur or in rhc .\cgc.rn-iìirhr ni.rnr conrc.lutnrh ir nnr con el.rrc cirhcr s iLL rhe \i,lL.rg,, or r irìr rhc I,iz Jc llnd rhel rrc :rlso rvcll-docunrcnred (lrlrabegol; & Le- Pcrer ConsL,nrer.rrc ìn rhc t)ol<,n,ir... TLc rerre'tri,rl scrlinrenr' in rh, \'rnri 198.2i I)e Zanchc et al. 1993; Serrowbar ì-D;uyan cr tsill,k ùlount.rins.rre p.rni t,i.r.olc,rn,r scdinrnr,ìr! sLr..c\\ion. \'|r.lr al. l99i; Cianolla &Jacquin 1998; Girnolla er î1. 1998). is chrr'.rcrcr isri,: ,'r rhc rrpclonring p.ìrr ,,4.ì rilr;rr .rrtr. Ten errri:l :c

t)cperrmerrr oi Ccoìogrl hi;tviis I-r,r'ind Unirr:rsìtv ol Scicnccs - H-11 l/ llud.tpcst. Pízrìin\ Parcr \órín\' l/C. Hung.r|.\. l-rrrail: ilc lledirs(, fìi cnr.ril.hLr 664 F Velled.its

i.l0,--

i;o\ l :\j 'k..i i/,

MISKOLC

0 2km

..l -/r#P,q6ò'.'l / ..,.. \J ' ')-i*rí-z' : .s éa , s*F \ i t-, Vàrheov' lr' ).t,i,aast)_,n'nnl) ) A - "-(Tz":9// 1 7'-'i -_.--' ,*@ :--;1ir-) ,i':&

Fig. 1 - Locarion ntap of the srudied areas. 1/a. Bùkk Mrs., D: Darnó-zone, AR: Aggrelek-Rudabínya Mts. 1/b. Geographical posirion of the Sebesvíz Section (Svv), and borehole Miskolc-10 (Mk-10). 1/c. Geographical posìtion of borehole lels6rírkiny 7 (It-7), and the dol omite quarry of Vírhegy (Dq).

tions suirable for sedimentological investigations can be rions of three Triassic sections revealed Anisian terrestrial found only on its margins. Sedimentological investiga- sediment occurrences, out of which two are situated in ,Jriri.rrr tr |rtrnr.rl ri.rltnttrt: i, tlt lliìkk .llouutaius 661

rhe'norrhern prrr, wlrile onc in rhe southern perr of rhc mount.rins (Fìr. 1b,c). Triessic seclimenlarion of thc Birkk \lount.rins \\':Ìs conn ollcd nl:linì\ b\. e\tcnsionll recton- ìcs i\eìlcdirs l99tì.r). The elolurion of rhe volceno-sedi- l- I tl nlcìltùr'\ succc sion oi the mounrrins follou's the evolu- i_lL rion of thc uptlonrint prrt of .r rifting are:1 (Dixon er :ì1. .È 191ì9 ) lronr the Anisi.rn. ' Sillcc irr rhe nlonrcnr thcre is no fornr.rllv acccpted i àr defjnition of thc Anìsirn/Lrclinirrn staecs ìnd rheìr bound- rg 3 rr\'. thc ilticle ntlinlv follorvs the schentc proposed bv J 3e \li.'tto N \l.rntr ìn (1995). J iÈ= g I ,r- r

i Sections

Ilr.r clct.rilccl tlc:cription ol rhc outcrops r.c.ealins the z Anisi.rn Lcrrcstriel scdimcnts of thc Biikk IloLrnr.rins sce \tll- cdirs r1999,20C0). ln rhc prcscnr p,rpcr onlr.!hc mosr intpor- trlrL i.ìcrs tre givcn belo\:

Bo|'cholc Felsíjtirkínr'-7

(ìcogrrphic.rl position: south oi rhc vilhsc ol Felsrîírkín1,. in rìrr N\\ ridee oi rhe V.ir Hill ltìig. lc). Thc srr.rtigr.rphic set- rinq c,i thc rerresrrj.rl sedinrcnts in bcrrcholr Fclsr'irirkinr-7 can L)C \eCD lll r'jg, l, '1he borcholc sroppcd in rhc rcrrcstfiil dcposìts. (it Con- Fie. -l - Srr.rtirr.rphìr.,rrìf{ b,,111,,1. Ì i I i ; .i I l{ ,i r I \ I it I .1nl ìr, ' seqLrlrtìu thc L.rs.rl p.rrL oi rhe rcrrerrrirl deporits,rnd rhe un- k,(ii(.ìll illr. I cqcnrl: | (1,'l,,nrirc rHj.)tjf l)t,l,jnrir< t:rìr.,, tLcrlr int irrn.rtion .1rr unknosn. trlost prob;rbh; .r[ter a short l. ìrcLrrrrinr nr.rrl. ì. SzcrrLi.rr.inhtc\ lt.r.ììfJ(,ìre I r,..t. uncrpli'rL.cl inrtnrl H.iuor l)olonr ir r: occu r-s. Thc h,r,riri. r.ì1..ì,,.,i!, nr.,,l. i. r.rJir,lrr.iri. r.. rIrrrr lìnrc,r,,rc dolomitc cen (bisin t.r.ie\: lr'l\,,ri,h.in\ I\(. Lì.r. / pl. i,,r',ì ù,1),)f.ìL! bc 'nrdiccl ir rhe ncishbourhood in ;r quarrl on the Vír Hjll, south ol lrclsiitírk.inr' iBcn.r l.{ I rrr I (lìir. lc). It consisrs of pcrticlal tcetures ie.s..rlq.ll nrrts.:rlg,rl clonres lFig..'ì.r)..rnd htrse ll 1cm) on- ctiiel: i. .rnd subrid:rl t1

l. Innlrnrunn .tlntrtlo;.i. Koihn-ZrnintLri. \ = ilr. r. lirl1ll,., rp.. \ = 7l\ 662 F. Ve//edis

Borehole Felsótàrkàny -- 7. LAKE lMarine

RlS l rs l B =\ = -\- = \\ o )) o (( r50 \\ -+ l-) z l) É .-/ '/ z -s // (( _! \\ \\ \\ \' e 15q \ \ cc \ = \ I \ ì

z .F -c) O .a) L - Lagoon R - Reef S - Slope z Ts - Toe-of-slope 2 B - Basin Hémor Dolomite Felsóterkàny 0uarry

-l r- l .51"1-J ro l=__l r l----l rz FTll r f rq ro ffi ' ffi re ffi rs F-o'l 2a?lil u')>o{ zz l. 23 o 24 r) 25 a

Fig- a - Sequcnce and hcics ot borehole Fels,îífkínr-7. I-egcnd: 1. siliceous, ruftrceous, rverthered cll'stone,2. vc.rrhcrcd rulf,:- r'olc;Lnic ruff,4. radìolarìre.5. lanìnitjc caìcareous nrrl,6. tuffrccous bioturbated narl, 7. frcshwatcr lìmcstont, lj. sandstone rìch ìn fcìdsprr, 9. màr1, c:rlcarcous m:rrl, 10. srronglt weadrcred, rcworkcd \'olcanic fr;rgnrenr, 11. red clarl 12. c:rlclreous nrarl nirh fcldsprrs lJ. sandv marl rich in green nìnerals, 1,+. dolonìte (Hímor DolomLte Fm.), 15. trlus, 16. cherry iinestone (Iels,îírkinv Lst. Fm.), 17. lthochs-

tic inrercrlation (r-.elsr;tirkíny t.imestone), 18. linestone of brsin frcies s ithout cherr, 19. Mrrl ricL ìn r esedinented roìcrnic ch,,ts 2C. dolomirned lìnesrone, 21. l:rck of informrrion, 12. Sedìmentrrìon unirs, ll. ridìohri:Ì, .24. osrr.Ìcode. .25. .hù.ì. Anìsìan teneyrial setlineuts ù tfu I)likk,\launtaitts 663

Dat\Ll.drc€rc ,\g€

\ hr'llri r r, I r \ rrt hl\\ id L.i!o fdiln \,,,tta\tnntlrlrrrt \lueliclrìri; ùùhl.Ír /on. = a a t?S.5 t dngoùrturxn lll.5 s1 lhr.\,tt,tl1ù td!t ilùdu L!úteù.t v i- cn^,a-,,tt" 1*^,r-uu, a ( )tt1 I n1!ù\ rrk\lt1 t\) rr)\^ 7 t'-"'tdú. ^tt t t,hÍn/,,r'11,1 Ittn":.rth ùr''.t .l fth o\ùì! .a t ttt tl.rrùt ùttlnhrd '' Trrtljl,,.l1. t)ùirltll,rri\ T, \ ha ùùú i'\ 1. L, kt I ! ú \ i I 'ilti\\,trr\ tdh nù.r,t H:imor l)oldnil. roruminifs{ P"ltm

larlrk,itnùr,)h ù1r\rt I tinlùt Lkl\'11.r \it.r Trb. I - Thc nro'r inponant fossils ol rhe icxrrri,.rll ol the flurirtile 1 ,nrrt.|ú1r!ù . ùi,rd sedinrr:nrs (borchole: Miskolc- I 0) a \h\tù|.\\ta il,"ùntu - st,r\ttn,r \f

l t1\ hu"""|ù dh,It||||\

tenlporincous t ith rhe volcanic activitr'. TrL,. | - ll-. r'o r.ììt,o1ìnr ".. 1. :,. ',i . r.,-,1 .".r - Thc lal

Sandy Algal N4icrle

Gastropodal Yicrte ostracodal [Iicrite

Lrcusrrirrc sedìmenLs. h thc middlc redìncnLrrr cnii,onmcnrs rnd rheir chrrrcteriirir rirìimcnrs thrr crn be stll conclrrtJ rirh rhc rock r.pcs rnd f.rcies oi bofenore Fc|si;tjrkjn\-7'i'ciìclreousnl.rLl.ric| drill core is 6 cm. b. Clh rnd \\ ìlknxon l9s0). Ch:Lr;L b.rnks colonisc rhc sreeper upper prn o1 tht sìope. (213.3 ,rl. N::0r. c. Crlc,rreous rr,u I l irh nicrokrrst phenonlen.r.ThcioIneIc.rrirr(P.rssjqc0[il|ool0|;L]Ùl|o\jnq0liJ sedincntsìnr:rledcloscthcncrIshorcr.rise.rborcrhescl1c.e]occ.lsionl]lr:(]]]'sm].Nl+I ro highlr bnclìsh rrrc tilìec1 from thr insoluble resiilue. Dct. l\'1. l\lorosrorì tll.l.0 nr) N= tt\. A ìsi.ot terrcsttial st:littents itt th Riikk llountains 665

Miskolc-10c-1 Lithostratigraphic units of the Northern Bùkk z. (t'

z, cú o J t!

z

>l

z

sc.

Ablakoskóv('lgy Fm. _-_---_-

(D o-

r Fl-:-l ::::::::::l .- ^ f_-t . f.]--lt 2 l: I l____l z l_ _ _l r r--T.-] , tl-r-f,lr-ì a f--- -:-l flìlfr] o l-.- l . - Srrrrigrephic sc,tring the lareru thc Sebrsríz "t | ^"1"ì.1 F;9.6 ol 'tudied of Srcrion rnd boreholc lfiskolc-|3. Leqend: Some itens irc T:l al.. .. | 1n l.-: -1 the s.rnre as on I'ig.2. Dìffercnccs rrc rs iolloss: L nr.rrl I l.'. r'-'.".,',1 '- F:-:-i-:= (vi\sz,rs F ).). l. sand'rc,nc. cìrvcv nurì. crlcrrcous mrn (Abhkoski;lajlgv liÌ.1. J. oolitic limestone (Ccrenn:rrir l.sr. Ijìg. 7 - Scquencc,rf borchole Mirkolc- 10.I-egcnd: 1. voìc.rnitc (Szcn- lrn). S!r Steinilnr Linresrone, S(l: SebesrÍz ConglorÌcrrtc. I: tisninhegl Porphlrir,:),2. sindsione, L aleurolire rvirh rc- bor(hole Miskolc-10. ll: sruJicd l.rvers oi rhe Sebes íu Sccri,u. *rxked rolcrnic cl.ìstr..l. er.rnule (:-3 nìm),5. nìicrocon- glonrerarc (:-5 nìnr).6. conglomerrte. breccir (0.5-8 cnr),7. linrcstone, $. chver crlc.rrcous marl.'r. crlcareous marl wìth linresrone cbsts. 10. dolomne. breccia: ll, rcd s.rndstonci C, ochre srndy clay- This sequcnce s as deposited bv l braided strclnr. The conglomerare,/brcccir Lr\ - ers rcpresenr thc channel fill, thc red sandstone interlavc'rs and sindv clal'Iivcrs $,c,re dcpositcd es floodpl.rin mud. the sirnd bar bcrrvccn the charncls, *,hilc the yellorr ish-brorvn A: CongJonrer;rtc/breccie (Pl.l,Fig.h): A bì t tLrrr:'ttr.ll \Ltiuc'tt' tu tl', btikk .llunutaiu; 665

Miskolc-10 Lithostratigraphic units of the Northern Bùkk z.

z.

M J

ilt.

50

il. 100

..,1

Ablakoskóvól gy Fm. ------_-

-- F-=l fr 'Tt l ^r--':.:l I l---l 1l__l^ o- l-TJ fJ'l , [=I]1 ' T:- :--:-l 3l;-!l 'r |.:._:.:: It. I 5l 6[ l-ig.6 Srnrignphic setrirg of thc srudied hvrrs oi Lhr Sebes.Íz l - i Secrn)n rncl borehole Miskolc-10. l-csend: Somt irens are tr;:-:--u rhc s.rmc rs on ljìq. L Ditterences rrc as tolloqs: l. nr.rrl 7l:;=:l I F..,'-.! 91 . Ilof:=-l (vc!s,(;s Iìnr.).2. srndsronc. chyer nrlì, c.rlcrreorLs nrrl (Ablakosk,;r iiìgr lm.).3. ooliric lirncsrone (Cere î!ir Lst. ljig. 7' Sequcnceoi brehole ìVliskolc i0. Lerend: l. lolcanitc (Szen- Fm). Sr: Sreinalnr Linestone,5C: Sebcsvíz Congìonrerrte, l: tisoínheg1, Porphvrire), :. srndstone. L aleurolìte rvih re- borchole NfiskoÌ(- 10, II: stLr,lie

ì,lF ofthe resedimented pebbles Fossils

2. Foraminifèral nrudstone Pelsonren

i,1ca LIr0Vit Lt Llclòntl|!|Ll

l,lcd nLl turp i t o d i ttu r i( \1eunln:pnL|tu utnnrcIi Tolt 3. Foranìniîeral gfainstone l\lcdndt a\pìtu diru|ì(d sand shorl Nlcandrospifa detònrata

Toh pan1tlt in.r :4-cgut ltl Ta|\ paIt,ttt|1 gtcSut ì.1

.1.Oolitic grainstone

5. Peloidal packslone Ht)t(ncllu \ inrn\ i.\

6. Mikroìrial strollatolitc

7. Mudslonc \\ith bivalvc shclls

Limestone pebbles:

8. Radiolarian. sponge spìculc wackestone

9.CrinoidaÌ packs(rre

l0 Cìaystone grains

The thicl

rhan in the forner santple, lt nral indicarc the r ccurrcncc of rhc (Unir II) r'cvc,rlecì th,rt dr,rlorritc ind linr.stone pebblcs origi fluvìal dcposirion during a break of volcanic irctilitr'. nrted nor only fronÌ à for mer carbonle platforur but rlso Irom it besin, Consc'qucnth', n,c can concludc th.rt bcfore thc uplìft It is is violet in coiour. The mejoritv oi rhc qr.ins rrr lhl: b.scDent tas dii[erentietcd. Thc pllriocllse at tì9.95-39.5 plagiochse. Sincc thcir conrour is inract thcl.rrrll'hlvc origi- m (crlsrel tui[) indicatcs coclrl volcenic ectilirr: On thc Lr,rsis nared jn thc nerr vìcinity A singlc cm-sized hr',rlit. flag"r"rrt of the inlcstil4rrion of rhc pl.rgiocl,rsc, r birsic rock-!\,pe orilain nts also cncountercd. can be llso crcluded. 48.5 nT: volcanirc rvith carbonate pcbblcs. The fincr-grrrined rocks of Unit III suggest.r leveìling Occurring in:r light grcen rrratrix, \'iolc! spars xppc,rr oI thc relicf. A gr:rdu.rl dccreesc in thc rescdintcnted sedintcn- rvith an irregular contour', The spars have a thin d:rrk green trrl-rììltcfials in the borehole scction (SIise III) indicates rhc rinr- Thc framcs,ork ol the rock consìsts of phgiocl:rs.' larhcs beginning of intense lolc.tnic ectiritr (Unit l\i). and betwcen thcr'n carbonate fraqnrents c,rn bc scen. Thc rim of the carbonate grains is altere'd. Thc rock is a product of a llll Sebesvízvólgy Section (Fig. 8) flow. Bctwecn the volcÀnic componerts the cirrbonrrc greìns represcnt the se'dimcnts thlt rvere ripped up and incorporltcd Geogllphic positiorr: h,rli-ner lretr.cen the lill.rsrs oi b,r' rhc Lrve flot. B;fukúr .rnd l-illafiìrcd, on rhc southefn side of the Ger:rclna Unit IV (48.5-0 nr): green lolcanic tuff. Vrtler (l:ig. lb). 'l'he srrirrigrlphic serring oi thc sccrion crìr Lrc seerr in lntcrprctirtion; I'ig.6. Bcnveen the dcposition oIrhc lagoonal 5ediments of Unir !l!LL plxrlorn dolomirc (Hinrol Dolonritc). No fos- I (Steinrlrr Linrestonc) ancl thc tcrlestr iel sedirrenrs of Unit Ì I, sils rvelc found in this scction. rhc areiì \\'^s liftcd up. Due ro thc recronic acrility significlnr Unit II: Sebcsvízr-òlgl Congkrnrcrate (ll. 2, l:ig. a). cliffcrences in thc rclicf occurrcd in thc llrc Pclsonian rrnd this A.fter rn crosion surfrrcc thc Scbesr'íz (lorìglotìlrrîtc Iol- resulted in arr intensc e'rosion l'hich provided rhe nl:ìrerirl ol lols ;rnd it hls a thickness oî l.l nr (sincc'thc strar,rl dip is un the conglomcute/brcccia Iavers oI the sccond unit. ccrtaìn, its thickness could be 51.3 n ìf r highcr rnglr' is tirkcù A rnicrofacies investigation of thc redcpositcd pebblcs into eccount). Pebblt's of l-15 cnr in dirrnlcter floer in e srer', cilcercous nriìtri\. In the lo\'er prù-t of the conglomerete, in tn'o (20 lnd 60 c,,)1 thiclt) horizons, thc' mirtrix SEBESVíZ _ VALLEY is rcd cì11'lncl thc qr:ìiDs rrc rngu- hr encl unsolred. In the nretrix ol thc conglomer:rtc, Al chloritc :rnd ptrophvllite rvere indicrted bv X- rirl, rn,rLysis. Thesc tsî nrincrals - tosethel \'ith l lergc illlount of h;enr.rrjte - sugilcsl hcr\') lxteritic

3

9

- l..rclinirn l.rrers .rnd =rl |ig. s -lnirirn 3w i.rcie' cun. oi rhc Scbcsvíz f Section. l-cqrnd: l. s hire rìri\sirc Iirre\1onf (Fehúrl{,, -[l È L5r. |nì.). l. liqht grcv lintc- . sr<'nc. in cerrrin horiz,'ns limest,,nc ci.rsts iD fed chy m.rrrir, L el.rrk rlrcr-chcltl 3= |l,a linrcstrnc sith sh,rle .rnrì r,r- .+. s diol.rlirt inrelc.rl.rtions, t : Fluvialile drrk grc. l.rnrin:rr' liuestorr', 5. ( hì!e dolomi!e, a). roìcin- R : Reel itc (Szentisn I'or phv- Sl :Slope inhegri fireJ, 7. c{)nglorr(f.r!e brccci.ì ù B r Basin (SebLsríz C0ngìontcntcl, 3. dolomitc pcbbles in red cl.rl Il iScbcsvíz Con*lonrcr,rtc), 9. tlF) zffi,E oFili] rflJ 6E elr:'-.l sf-- l n,cdium grcr dol()nìit(' (lli '[r] nìor l)olonìiÌc Fnr.). 668 F. Ve//edits

\reathering (Kovícs Pílffl P.rnd Vicziín I., personai commu Borchole Felsótirkínv-Z: since the borehole nicatiol). Bcr*'ecn the clav mincrals the ììlìtc has a double na- stopped in the leke sedinrents, its footn'all is unknonn. ture: a p:rrr of ìt is a 2lVI-altered, cl:rsric or alreedv netrnorphic Hon'ever, according to tlìe assumed srratigraphiceì posi product; its orher p:ìrr is b:rd11-cr1-stalliscd:rnd has r rviclc brse tion ol the l,rkc dcposits thcir agc is n.rost probablv late rellectioú. The latter \r-rs smectite, thus the tufl3ceous chrrrcter Pclsonian lllvrian. of rhe original nìatcrixl cxnnot be erclucled, eirhcr. iror the nricrofacies rrpes and fossìls of thc resedimcnred Borehole Miskolc-10: the underlying formarion pebbìes sce Table 3. The rge is Acgean-Bithynìen. (Steinaln.r Limestone) contains upper Pelsonì:n-lower ln thc laycr group.,r 70 x l0O cm cLish-sh:rped conslonì- Illyr-ian fossils, so the terrestrial evelìt rÌlust har.e taken erate represents channel sediments. In rhe niddle pxrt of rhe place ìn the latest Pelsonian-earl1' Illvrian. Sebesvíz Conglonrerirle, a mariimum.l.lJ ,ìr thick ruffitic rolcanic The materìel, agc, and facics of the resedimcnted peb intercalation c:rn be found; its lo*-er and upper boundrries rrc bles are diflerent. Arllong these were iound SteinaÌm Lime- jn rectonic thc section. In the upper prrt of the conglomerere, stone, dolonìite (Hímor Dolonite) and shaÌe most proba- cleystonc pcbblcs also occur among thc rcscdimented pebbles. blv originated from the Abiakoskóvólgy Formatìon (uppcr Accordingll, the erosion affcctcd the footrv.rll and the under parî of the Lower Triassic), rÌrd oolitic grrinstone which lving rocks as wcll. nrost probablv fronr The shapc of thc clasts is vcn'oftcn angular and rhel'do originated the Gerennavír Linestone not sho$ anv parricular ordcr. The grains are similar ro those (ìower plrt ot the [-o$,er Triassic). The [rains originated in the lower p,rrr of the SebesvízvillfÌ)' Conqlomerètc and thcv not only lronì rhe directly underlying [ormxrion, bur from are complenented by clav pebblcs. The lattcr most probablr. deeper ones, too. Based on microfacies of the resedimented orìsina!c from the Ablakoskór'ólgy lìornretion thet undcrlies grails, we caù àssuùre that before the updonring the pìat- the Hímor Dolornite (Fig.6). form had been differentiated, so we have to take into con- Flcics: in the lo*'er prft the red, clavev metrìx suggesrs sideratjon the coeval existencc of platforms and basins. lateritic rveathering; according to the Iìtholosy rhe sedimenr can Sebesvízr'òìg1.: the foorw:iìl consisrs of Hímor Dol- be interpretcd as a fluvierìle. tlood-pÌaìn sedjnent. The dish- omitc but rve could not tìncl any fossils jn the srudied out- shaped conglomerate complex is e channcl fi11ing. On the b.rsjs of foranrinìfera, the age of rhe dolonrite crop. The age of the resedinented grains is Lorver Ani- pcbbles is Eariv Anisi,rn, thcir frcics is hgoonal. sian; their nicrofacies indicates a lagoonal orìgin. Onll-a Unit III is the Szentisrvínhegi,Porphvrite. Unir IV (P1. ferv cl,rvstone grains rvere found and these probably origi- 2, Fig. h, i) ìs a thin-bcddcd lirnestone of basin frcies. Its asc is nated fronr the Ablakoski;vólgv Formation. Grains which Ledinian/uppcr Fassanìen on the basis of conodonrs. This is Iol- could have originated from the Steinalm Limestone and iorl'ed bv white dolomite (Unit V) end rhin bcddcd gley lìnrc the Gerennar':'ir Limestone have not been found. sronc (Unit VI), and thcn chcrtv lincstonc q.ith radiolalite in Comparing the niaterial of the pebbles from the tercalat;ons occur.s (Unit VII). Thìs is followed bv light- gre_u Sebesvízr'ólgy Conslomerate as rvell as from borehole Mis- limestone with red clayel' limestone ci:rsts (Unrt VIII). Unir IX is kolc 10, r-c can assumc thJt rhc pcbblcs rcprescn! ts-o tel a platforùr linrcstonc rvith stronrxtact;s that occùrs cn nlassc. restriaÌ evenrs: one ìn the latesr Pelsonian earìv Illyrian, and Interpretation probablv another in the Los,er Anisian or in the Pelsonìan. The Sebesvízvòìg_v.' Section indicates the folÌon'ing Volcanic activity is coeval rvith the Anisjan terres- subsjdence historr,: efter the deposirion of rhe Ìagoonal trial sediments. In the lacustrine rrarl sediments, reworked HínTor Dolonite (Unit I), the area *es raìsed. Sr.rbsequentlr'; volcanìc rock fragments as well as resedimented minerals or probably coevalv \\'irh the volcanjc ectivirr' (Unìt III), rhc area .rrt Le fou r,l. Il rh...rmpl. fr,'rrr Ft--:20-.t, rr. t irn subsìdcd rapidl,v (Units IV VIII). The initial repìd subsidenc.' bc secn th:rt the nratcriaì s/as st;ll plast;c when it entered had slo*ed down by the Late Lrdinian. In the Lrre Ladinien, rhe basjn. The material fronr which the clasrs originated thc scdinrcntatìon, duc to thc progrrdxt;on ol thc platfornrs, was (glassr'). remnants are mineral- continued orì the platforms. originalll. felsitic Its ised with clal'and contein plagiocÌase phenocrysts. On the brsis of the extinctjon of the pÌrgioclese, the grains are almost certainl) derived from acidjc extrus;ve rocks Current knowledge about the terrestrial sediments of the .i , r;r ct rn. 8.C.. pcr.(.nJl cL,r-r-ur ic.rli('n./. Thc r u ..rni, Biikk Mountains ,A rocks arc dcrived from a pyroclastic series that càme jnto Age: the nain problem wirh rhe terresrrial sedi being due to explc,sive volcanism. B,rsed on their petro- nrcnrs of the Bùkk Mount:ìins is that their age cannot be grrphic character, they are puniceous tuffs, the fine grain determined as precisely as that of thosc in thc Dolomitcs. size of n'hich indicates a distal facies. On thc basis of the This is partÌy due to the subsequcnt tccronics, partly to thin sections, tlicir genetic classiiicetion cannot be crrried the bad exposure conditiorls, xnd partly to thc doÌomite out. They nlry be menrbers of a dispersed pyroclestic series (which in some cases forms the footwall) that very fre- connected to a Plini:rn type, or the distaÌ perts ol an ìgn quently contains no fossjls. inrbrite scrics (Harangì, Sz. personal communication). The dating of te..est.ial deposits was based on the Traces of voìcanìc activity can be found bctween xse of the undcrlying formation and on the rge dàta ol the Upper Anisjan l-adinian sediments of the Búkk the resedinrented pebbles. Mounrains. A lsia terlestÍi,rl sed,iments in the Biikk Mountaíns 669

Fìg. 9 - Posuion of the Alpian rnd Di- Vardar-lt4eliala branch naridic of the Neo-Tethys ocean unns during the Trias- sic rifrine of the Nco Terhys. Northerf Calcareus Alps Biikk [4ts. ?So!lhern Alps 'Ihe lorcr parr of the lìigure West Carpathians ?DinarÌdes depicrs rhr modìfied sinple lJpper Crusîal Breakaway she.rr nodcì (Dixon rt. Topographic CLriminat on et llrlnnesl Crusl 1989). See rexr for exptrna-

Role of the Anisian terrestrial sediments of the Bùkk rift stage (Hímor Dolomitc, and Steinalm Liraestone), Mountains in the rifting of the Vardar-Metiata branch of the terrìtory was upÌifted (terrestrial sedimenrs). the Nèo-Tethys-ocean In the Southern Bùkk Mountains the evolurion of a half-graben berween Anisian-Rhaerhian can be followed Terrestrial sedimenrs in rhe Bùkk Mountains are (Velledits 2000, figs. Z-8). In the late Anisian a rerresrri_ parl of a volcano-sedinlentary sc.ies which is characrer- al haÌf-graben came jnto being with a lake in the deep- istic for the updonling parr of a rifring area (Velledirs est part. This evolved ìnto a carbonate shelf half-graben 1998/ a; 1998/b:2000). According to Dixon et al. (1989) due to the subsidence o{ the rifting. (Above the Anisian and Allen and Allen (1990), rhis part of a rifring area is lake sediments we can find cherty limestone in rhe No- characterised bv topographic culmination and by bimo rian-Rhaethian) . dal voicanisn.r (Fig. 9). Above the upwelling of the asthe- After and par rly coevally with the uplift, an acidic nosphere the crusr is updoming and rhe area is upfifted. voicanic event took place. The petrographical character The respective occurrences of the volcanisnr and uplift- of thc volcanic rocks shows rhat rhe Middle Triassic vol- ing probably coincided (Coleman er al. 1983 in Dixon et canìc rocks represent magmatic activity re)ated to ex, al. 1989). Shortly after the uplifting, reworking of clas ren.ionai

dc'positcd on diifcrcnr palts of the V.u d.rr-l,l eli.rra br.rnclr Thc Tri.rssic dcrcÌopnrcnr of the units of Norrh- of thc NccTcthls occirn (Kovics 1981) . The Trirssic se - E:rst Hung:rrr jusriir the ;ìs\'rÌrnìerric rifting model oi qucncc of thc. 13iikli trlorrnrrins t.as dcpcrsitcd on rhc up- \\'erniclic (1931. 1985) rnd Dixon et rl. (l9lì9). donring sidc, rr hilc thc scclucncc of thc Asgteìek Rucì.1- binr'.r Mount:rins l ls deposired on the oppositc (brerrlir- Terrestrial sediments in the Southern Alps , Dinarides rr.rr ) sidc of rhc oce,rn (\'elledits l99S/.r, l99S/'b). Snrrll renìn.rnrs of the occln lre rcptcsentccl trl the ophiolires Anisian terrcstrill scdinrcnrs le elso knoln from in Ilódla V.rller'.rnd D:rrnó Hill (sce Fig. l.r:rnd Fìg.9). the SoLrrhcrn Alps. irorr the are.r ll ing north ol the Sourh- The evolutìon of these threc prrts oi thc riitìng ocerrn ern Alps. end fronr thc Dinarjdes. c.ln l)c cor.elitcd lcrl sell. l ìrc Anisi.rn Stcinaln Linrc- 'l hcl scem ro be charecteristic ofthc southern shelf sronc is plesent in rhc Biikk NIount:rins incl in the As- of the opcninq V.rld.rr-Me lìirr:r ocein, to the northern gtcìcìi-Rudeb.inr.r l\{ount.rins. Altcr rhc scclimenrltion contincntil shcll of the Gondrvirnl. Hol'evcr, thcy are oi thc Steinalnr Linrcsrone rìrc- erer oi lJtikk !lountrins n'tissing lronr the tleltcst part o1 the Northern Clllc.reous n.rs uplilrccì. Sinrulrrncousìr uirh thc Lrplilì the inncr Alps lnci from the Nesrern C.trprthians - rhlr is, front p.rrrs of the As{tcle k-Rucl.Ìbirrr a }lountrrins neirer rhc rhe norrhern shelf ol thc opc'ninq Vardar-Mcliatl br,rnch liit .rris (Bódr'.r rnd Szijl,'js.rrcló unìts) subsiclccl. Dr,rlinr of the' Neo-Tcthvs ocean (Fig. l0). ConscclLrcntlr', the thc Middle-Uppel Trirssic, p.rr,rÌlel rvìth thc strikc ol thc prescncc ol the Anisi,rn terrestri,rl sccliments in the Biikk rift .rsis. l llrger irnd ì,rr gcr ,rree qr adu.rllv clr-os necl in thc l\lountains confilnrs its paÌircoqcographic conncctions Agstelek-Rucl.rbinr a Nlourrr.rins. nirh thc [)in;rr'ìc]es rnd rhc SourherlÌ Alps (Fig. 10). Irr rhe N'liclclle Lrdini.rn. .1./ niÌlion le.rrs .rftcr rhe A conplrison ol the Anisiirrr tcrrcstrillsediments is r.r;rìifr of thc Ilillili N{ountains betwccn the trro shclvcs mrde ntore diflicult bv the fect thirt the)'knowlcdge xboLrt (c;rch halinq,r clificrent evolurion hìstolr'),.r ncr oceirn thcnr is unelen. ln solnc cases onll thc substrge of thcir openccl encì its rernn,rnts rrc rcprcscnrcd ill rhe ophio- aqc is linorvn, rnd sotnetimcs their zone/subzorre is knon'n lithcs of the lJóclvr V.rllcl rnd Drrnó zonc (Réti I9S5. as tr elì. It heppens ,rlso thet the ,rge oi the s.rne fornration 1988; Dosztírlv E: Józsr 1992). is dctclnrìned diliercntlv bv diiferenr aurhors.

I 100 200km '--l Ns ) -'\.--t- \,F.rRpAfgìANr ' i ./ ) 51 z' wtEN \ $l / \ -.-ì "^-1 _ )- -,rr==r--t=-l t/ \ \-\'--r / g_ii.kkt_ __.. -r-'1-r 1 - t lls. J .f-l .t'" rt ÒBroAPllz (1 \ /--. I ctd, f^dt' .^z,,'.1 /( - J , 1, >

Lliihh \1r.. c.rrre inro rhcil prcscrrr l .rJini.rn r Uso' izz.r on(-.lrìxrnìlennrrI,rr'rrri.rnlrrcrr.Th.: 5k'lhe|nC1]!i]].Cc!l!I.l]977).lì.l|lh|{('li}-..NlerlnriD.(|9s]).l].ì|.lbtgolicl.l|'(|9S;).Iì)i\lj.ùiJ'doulÌl(l9s])'JidoulF:N Nicofr A. il9Só), K[riner K. \ I utz l). (l'r']51. \1.ìflùr.ìr'1. ll00l), ]losrlcr H. $. Kfrincf K. (1994), tìl,ria cr rl. (1C00),lt.rdoiòió R. {19'lr0), liuLrelii {100-ì1 ,ìf(l \clledir\ 1le'rS rl. A) ) ì s i Ll1t t trrei tri d I t rrl i n Ln t i n tb e I] ii kl:,1 I o u t t tù n :

Southern Alps Pia (19-17) h.rtl rlreirdv cstrblishcd th.rr dLu'ìng thr Lombardy Trilssic, the Southcrn Aìps sere ,riiecrecl lrr svnsedi Opinions on thc origin oi rhc terr-estri,rl sedinrcnrs nrcntrrl tectorììsnr .rrrd volc.rnisrl. Thc nrost signìficant ol Lomb:rrdv varr'. Girnolh cr .ì1. ( 1998. Fig. {) describe crosion c:ln be cl.rrctl to thc rinrc of thc forrrrlrion of terrcstliirl sedilnents front rhre e lcr cls (Bithr ni:rnl'Osm.rni the lìichthofcn (ìonglonrcrlrc, u hen rhìs unconfoÌnìir\. subzonc, Peisonian/Cuccr'nse subz-onc, lnd Iili,r'i.rn1 dcepJt cut Anisi.rn, Lol'er Triassic encl Perrriirn units. C)n Trinodosus subzone) thlt rrc prraìlcl with the coclrl thc b:rsis ol thc .rn.rllsis of tl.re pebblcs of rhc lìichrhofcn aerrestì'irl sedinlcnts of rhe Dolomitcs. Ser lelcÌ chinscs Conglomcrrue, Be chsr;iclt li Br-.rndner ( l9l0) estrblishcd is bclicved to be the prinrarl f:rctor oi their oriuin. th:ìl r nlorc thln:r.100 nl thickness oi secliDrents s',rs Despite to this, accorcling to G.retrni er;rl. (199S), erocled lt this tinrc. thc scdimcntetion of Lonrblrdr t,rs nr,rinh' iniìucncetl -\fter thc thirrl uplifr lrhe' :r:e oI rr hicìr .rccor dirr{ tt) bv cpisodes ol transprcssion ind tÌiìnstension, s ith l icle- Gianolla cr rl. l99S is rhe l)irrlccr-rtites zonc,,Tr'inoclosus sprciìd voÌc:lnisnl and local uplilìs in thc ìvlidcllc Tri.rssic. subzone). the r.rre oi subsiderce ìncrcascs, The scquence linkcd indir-cctly to thc opcninq oi Nc'otcthvs in thc Errsr. boundlv scenrs ro cor'tcs;roncì to .r dros,nìnq unconforlìritl Middlc Triassic scrics is char',rctcr-iscd bv thick cirrbonirtc clused br' .r strcrng incrc.rse in subsidencc .rrrd in sc.r-ìevel lisc succcssion (1.200 1.500 nr) to the Fhsr elid 500-1000 (Gìrnolla cr:rl. 1998). In rhc l.rtc Illlrirn,lroric Lrlsins ceme l'r'Ì to the Wcst, $'here it contrrins nrljor glps. Grrer.rni er irrto being. ancl in tìrese birunrjnous clrbon.rre rhvrnrires al. (199S) descrìbe ore supcrscqucnce fron rhe lVIidc{le sh.rrph orerlic rhe prelious crrbonire tlnrp scclinrenrs- Tri.ts,.ic thrr is inrt' rno nr.rior,,,nrpositc Rùîicr Ziihìlic (199r) .lnd (J000) 'ubdividecl '.- & Ziihlke hele quences (Al and A2 Ll). presentcd sonrt'rcsulrs lrolr sinrple nunrcricll b.rsin nrod- Fronr the Anisian, the ic,lìor. ìne terrestlj.rl recli- ellinq \\,ith respccr ro subsjdenccr'upìift r-.rres.rncl pr.irnrn nlcnts \vete reportcd: conttoì br sei-lcvcì cìrrnqes or subsiclcncc,rLrpliit. Ac- | . Or r h. L"p o. r ìrr A I .urìu(1r( r. J rì'inùt \rq lt(nic cordìng to rhcr'lr, scqLrcrìcc [roundaries in 1.rluc prrts oI

(41/ll) appc.rrs in Westcrn Lourbrrcly (Brenrbanir Vrìlo ) thc Southcrn Alps (c.rstcr.n Dolonritcs. LonrLr.rrclr'), in in the Upper Anisian. lts lol,cr boundarv is nrrrkecl br'.r the Europcan epìconrincnr,rl scas (S\!:Gcrnr.rnr ). in thc discontornitv q'ith,,terr.r rossrr".ìnd localh- intr,riorrrr.r- Arctic Sea (B.rrents Se.r, C.rn'rdi,rn Arcric),.rncl in Chìn.r lionxl brccci:ì ìn the basal ,,Pcriridal Dolorlìtes" (Upper corrcl.rtc l ìth e.rcìr orìrcr. Nunrericrl rrroclclling for the Antolo Limestonc). Dolomitcs indicrtcs rh.rr thc or igins of thc [)iz cl.r Peres ln the L,rkc Cooro rtrc.t, f.rn clcltes progr:rdcd onto Congìonìerite,rncl Volt.rgo Clonglonrcr.rtc irr l.rrge .rrc.rs ('rrr.rtr,' r (.{rl thc e.rrborr.rre Lr.rr ' lJrll.rrr l r .r..ì c n.c(lu(.n, of the eesteln I)oìonrites tcre induced bl se,r-lcveì chlnq thc incrcrscd siliciclirstic supplv Lìthic arkoscs pessint up- ,.-s, rvhereas the lìicìrtholen Conglonlcrilrc ol rhc r,csreln rvar:d to fcldspathic litharcnitcs rrrc explained bl uplilt of rhe l)olonritcs lrrrd the Voìtrrgo Conglomerltc in rhc Sourhern birsenrent.rs g'ell as eithcr vo]c.urisnr ol basin inversion. Dolorrites n-clc prirttlill conrrolled b' tcctorrics. 2, ln Vrcstcrn Lomb,rrcll. thc ìorver boundlrv ol tìre sequencc A2-l-l is n.rarkcd br':r -i-5 kn prorredltion oi thc Bcll;rno Fornration onto thc undelh ing coasral lr. ln Kr.riner fr" l.utz ( 1995) desclitrc t l o clillclenr liìnds Ccntral Lonrbardr, ir is nrrrrkcd bl rhc subaerirl cxposr.rre of brcccias rrith

The Uegowitz brcccia is overlaid bv a thin sequence Gelovitz ss.2). Thc firsr three are identical wjrh the lev- of carbonate siltstones irnd sandstones (Kùhweg Mem- els described in rhe Dolorrites, whilc rhe youngcst onc ber). Tbe Kùhwes Mcnrbcr is followed bv pelagic lìnrc- corrcsponds to lcvcl 2 of the Ugovizza Breccia. stones and intcrcalated pyroclastìcs (Pictra verde) of rhe From the Northern only the two Buchenstein Iìornt:rtion, younger levcls (Ugovizza Breccia 1, and Ucovizzr Brec- Farabegoli & Levrnti (1982) recognised three rnrin cia 2) are knorvn. lcvels of terrigenous erosion in Vcstern Carnìa. The re- Farabegolict al. (1985) describe three tcctono-sedi, sedimented grains lre included: l, in rhe los,ermost l)onr mentary cycles oI second orden uppcr part oi the Lorver Fbrnation: Pelsonianl 2, in the M. Bivera Fornlation: lo\\- Triassic-Pelsonian, Pclsonian-lower Illr,rian and upper Il- er Illyrian; and 3, Ugovizza l3reccia: upper IIl,vri:rn. lvrìan-Loq'cr l-adiniln. In the upper Anisian, the periridal In the Eastern Carnic Alps, in the eastcrn part of carbonate plarform broke up and duc to rhe uplifr of the thc "Palcocarnic chain", only rhc Ugovizza Breccia ap- northern part of thc irrca an E-\X/ orìented rìdgc (Anisian pears (Fois & Jadoul I 983; Jadoul & Nicora 1986). Thìs Paleocarnic Rìdge)

Julian Alps Idrija and Stopnik area Gianolla et al. (1998) described terrestriîl sediments Terrestrial sedimentary rocks wcre iormcd in a tccron- from four levels from the Southern Julian Alps (Piz da ic trench as a consequence of the Lower and Middle Triassic Peres CGM, Voltago CGM, Ugovzza Breccia, and Rio tectonic activiry in rhe area of Idrija and Stopnik. Among Anisirut ttnesoitl setlìnerts h tfu Biihh llountains 673 them, rhe Idrija tectonic rrench s,irh mercun'ore dcposits ing sedìments rvere depositcd in shallow marinc environ- is the nrost inrportant. It had started ro form in thc Lorver ments. The scction indic:rres that rhe rifring failed aftcr a Triassic. Thc first tcctonic moyements producing a flerulc short period of Middle Triassic volc,rnic rctivity and after are nrarked lrv inrraformation brccci,rs in the upper plrt of it a shallorv marine deposirional reginre rvas re-esrablished, rhc I.orucr Tri.rs'ic dolonrirc lPl.rcer & C.v 1977). s'hich lasred throughout the rcst oi thc Mesozoic. In thc Upper Anisian thc unifornr Anisian dol- omite platfornr, or rilmp was cut by subvelrical faults. Radoièiè (1987) strres rhrt Anjsian block-faulting af- Sonre blocks u'erc uplifted and becamc partl) drv land. fecrcd the entire Dinarides rnd was succceded by polyphase Subarcal wcathcring produced bauxitic sandy sediruents volcanism (Anisian-Ladiniln). Synsedinrcnrarv faulting was (which arc only prrtly prcservcd) ond dolorritic clastic nrorc intensive in thc southern sector and began somcwhat sedinrcnts that werc mostlv rransported into,r sh,rllorv earlier - probabll' as earlr' .rs rhe end of thc Lon'er îiassic. 'fhe sea (Òar & Caclcl 1977). resulr was the uplift of a large rcgion in the Dinaric Car- In rhc Uppcr Ladinirn, Longobardian, the rrc.r .. as bonatc Plarform (cxternal zones). In rhe l-are Anisian a large differcntiatcd into uplifted and subsided blocks. Sonrc up- pirrt of thc Dinrridcs u.as charlctcrised bv rhe association lifted blocks nerc crodcd don'n to the Carbonifrcrous shale. oi H,rn Bulog (rmmonitic tvpe facics) and bcddcd or nodu- Thc clastic sedinrents originating from the uplilt are shale, l:rr hcmipclagic limcstoncs and chcrrv linrcsroncs (Radoièiè sandsrones lnd conglomerirtes, s'ith distinct tcrrestrill ho- 1990). Ladinian is represcnted by thc Porphyrite-Chert Fbr- rizons and volcrnk rocks. ln the othcr casc thc sanrc r1,pc nrarion a group of nragnraric rocks ;rnd bedded limestones of conglorreratcs are cleposited on thc top of Triassic rocks rvìth chert. In the Middlc Carniln, l tectonic event caused of different agcs. Thc conglomerates mav reach r thickness enersion :rgain. Radoiòiò (1990) menrions thick sequences of more than ó00 n. In the Stopnik area they consisr of of congÌomerates and brcccias of Anisi:rn rge from the Di- pebbles of differcnt types of limestone, dolomite, volcrnic n;rrides, Lrut.he givcs no detailed dcscriprion. rocks, tuffs, tuffnccous sandstone and conglomcr.rte. Thev represcnt nrainly rescdirnenred rocks of the Lowct Ladinian Jadar Block and Anisian :rgc. The sedimentary complcxes of the Stop- Protié et al. (2000) gavc rn iccoun! the Podbukovi nik conglomcrrtes nerc intcrpreted as allulial frns ancl pre- Conglomcrates thar lie bc'tn'ccn the Anisian Dolomitcs doninantly fan dcltrs (Car & Skaberne 2003). rnd the Lorvcr Ladinian lolcanics (Tronosa Fornrarion). The rvhole arc:r subsided at the end of Longobard- ian. Thc subsidcnce rvas acconrpanied bv volcrnic lctir'- Bosnian it1- producing, ap:rrt fronlvolclnic rocks, also tuifaccous Trubclja (2003) describcs Middlc Triassic bauxites that sc.limcnrs in which rhc r oungcsr singenr'tic nìrrcurl or( lic on the karst surface of the Middle Trirssic dolostone and wls formed in Idrija. The tuffaccous sed;ments wcre cov- ,rre ovcrlaid bv a grey beddcd dolosrone, nrarl, sandsrone and ercd bl Corder olian dolomite. r chcrt sedinentrr], complex oI Uppc'r Triirssic age.

Dalnratia At Muc, the Canpilian Bcds are cor.ered bv thc Conclusions Otarnic Brcccia (Mar janac 2000). Its agc is Anisian. The maxinrum thickness is 25 nr. It is conrposed of verv co:rrsc Ag. debris and the matrix is somerinres bauxiric. It reprcsents alluvial fan to fan-delta deposits. The brcccia is overlaid Exacr agc data are known onll,fronr the Dolonritcs, by dolomìte and this is followed bv black carbonatc clas- Carnic Alps, Julian Alps and K,rrarv,rnks. On this basis, tics with Iithoclasrs, skcleral frrgmenrs and chert nod- rhc following statcments can be mldc: in the Dolomites, uÌcs, showing oidcnce ot sliding and slumpine. Thcsc tcrrestrial scdimcnts rverc describcd in thrce levels (Gi- sedinrents ,rre overhid b1'pyroclasts that :rre covercd bv anolla ct al. I998; see rheir n'ork mentioned previously in black gradcd calcarenite-radiolarite and overlaid b1' clayev rhis papcr). To rhc east oi the Dolomites, in thc Carnic ash. Sediments of I-adinian rrge are represented bv bitunri- AIps, Julian Alps and Karau.anks, and in thc neigbour- nous ln:rss flow cllcarcnitcs, rnarls and brcccja intcrbcds, hood oi Idjija (N Dinarides) a youngcr conglon':erate containing abundant phnt debris in rddition to molluscs, lcvel also appears in rhe upper Illvrian-Lower Ladinian: echinoderms, corrrls and lnrmonoids. Ugovizza lìreccia 2 (Fig. l0). According to Marjanac (2000), the Oternic Breccia was deposited during:r significant sea-levcl fall and asso- Tectonics versus sea level change ciared emersion. Thc Late Anisian pyroclasts have bcen attributed to rifring (Belak 2000 in Marianec 2000). It All the authors cited in rhis p'rper cnrphasise the was inrerprcred:rs thc result of a subaerial explosive vol- role of tectonics in thc appearance of thc Anisian terres- canism. Largc plant dcbris and coarse clastics suggest the rrial scdimcnts between the thick platfornr carbonates proximirv of an area covercd with vegetation. Thc ovcrlv- (e.g. Assercto et i. 1977; Castellarin et al. 1979). lr r,lries ri,hat thei, thought rhe pr.ìnrllr causc of boundarv thc platfornrs aÌrerdy re:rch a rhickness of 500- the lppearlncc of thc Anisien tcrrcstrjel sedìments n'as. 650 m. Conscqucnrlv for rhe Reìtzì, Secedensjs, Cur.ionj Whcther it q'es tcctonics or sc.r lclcl oscillltion. Horveler. zones a subside'nce of 900-1050 nr can bc csrim:rtcd. thìs supposition hrs chenqed in the course of tìnre. In According to M,rurcr (2000) rhe subsidence slowed thc 1970s and 193Cs, the cited author:s rll consiclerccL thrt down in rhc Cr edler i :rnd Archelaus zones, reaching onll tcctonics pl.* cd thc prinr,rrl rolc, l hilc in p:rpcrs ru ittcn 50 Bubnoffs. in the 1990s Ììr:'u1\ iutlìors (De Zrnche et rl. 1992; De Alre,rdv Bosellini (1991,1993) had suggested thar Zanche et rl. 1993; Gianoììa & Jacquin 1998; (ìirnollr et el. in rhe Middle-Lete L:rdinien thc subsidcncc "ccrscd slrd 1998) ret.rrd se,r-ler,cl oscìllatior as bting the prinre t.lctor clenlv over alnost the whole Dolorrirc Rcgion". in rhc iornr:rtion oi the terresu-j,rl sccLinrcnts irnd put theìr A simillr: terìdcÍìc)-cen bc obscr-r'cd in thc Brikk .rppeir:1rìce to the boundirv of the J" ordcr cvclcs; cven ìvlountair.is (VeÌledits 2000). Thc Uppcr Anisian lacus- .,' rrer .rill .t,c..cd tlc tL. t,' e '. r-,r,,rti,.. rrinc scdimcnts lrc coverccl bv lirmìnìtic calcareous merls Bascd on thc crlcuÌarioùs of Rfifler 6. Ziihlke (1995) deposited ìn rn anoxic basjn and these are ovcrleid b) ra

;rncl Ztihlke (2C00) ittasprolc<1 thrt diffcr-c rr t pl-rs of th c cliolrrite of Ì,rte F,rssenian,rge. Radiolrrite is followcd bl Gonds anl contincnt,rl sheli .r,ere pr:ob,rbì1' coltroìled br- chcrty limcsronc of Uppcr l-adinian Rhaetien age. Be- upliit in onc pìecc,rnd bv sea-Ìevel lall in other pleces. r1'een the deposition oi the tcr rcstrial sedìnrents :nd the radiolrrite thc subsìdcnce of the basement \\'as ver) rîpid The primacy of tectonics is implied by the fol- in the Bilkk lvlountrins: i.e. more than 5-600 m netrcs lorving facts: cluring e ferv nillion ve,,us. Thc movcmcnt of thc crust is rhc slnrc in both arc l) Thc Lcr rcstrirl scdinrcnts volcrnitcs-pcÌrgìc sccli as: ì.c. crnelgcncc i1r rhe end of Anisian thet is foÌÌowed by nrcnts (*,irh rhe exception of thc occurrencc in Delml- rrpid subsidcncc. The repid subsidcncc slo*'s dorvn in the Il:ìJ OCCUr tOgCtllCl. \lifJl.-l rr. Lrdir i'r. \ 'r.l,.iJ.r,. ,'l .rrcl r de"-t-L i.rtr In seleraÌ insr,rnces the l'eìsonjrn/Illr-ri:rn terrcs bc cxplaincd onll,bi.tectonic ìro\,enents, though rhe rise l-ì.rl serlinrents ire coevil n ith the loìclnites or precede in sca-levcl probablr-coincidcd q.ìth thc subsidence oi the tl-rcnr dircctli.. Thc volclnitcs;ue lolÌorvcd verr frequentÌv crust. Due to the rîpid subsidcncc aftcr thc uplifting, anoxic bi pel:rgìc formations. or ivith verr thick crrbonatc pl:rt- basins frequenrlv canre into beirg (e.g. in rhe Bùkk: Vclicdirs fornr ser-ìes.'l'hese ,rre repl.rced by shallou *,:rtcr c.irbon 200C ancl thc l)oìomites: Senorvl>arj ct al. 1993). These rvere .1tcs onlt in the I-ongob;rrdi;rn. Ìatcr rcpleccd bv n'cll oxl.gcnarccl clccp.oatcr scclinìcntation. This r:efcrs ro thc hct that thc uplilting ilr thc end of the Anisi,rn r.as ioìlon,e,:l bv the rrpid subsidence of 2) Discordancc. the crusr rvhìcìr slot'ccl clrl'n in the Lrte Lrdinirn. The 1'ounger tcrrcstrial sedinrcnts (Richthofen Con- l his tcnclcr-rcy' c,rn bc vcn- u,cll obscn ccl in rhc Wcst- gÌoner-rte, Ugovizzrr Breccìa 2) rr'crc dcposìtccl frequentlv crn Southefn Alps (WSA), Dolonrìtcs, Cnnìc AÌps, South- virh r significant discorclance on Pernrian ol Carbonif- jn crn Karawrnhs, Julian Alps and thc Biikk N'lountains. crous beds (Erstern C:rrnic Alps Fois & Jadouì 1983; In the \VSA Gretrni ct aì. (1998, Fig.4) dcscribed Jadoul 3t Nicore 1986; ldrija Phcer & Car 1977). trvo pcrìods t'ith acceler-rted subsidence: rhe first in the Angular discordancc berween the terrestrial sedi- I-ltc Anisian. rnd the second in the nricl-Norian. Thci ments and their footweÌl hes also been described scvcr:ri crplain it t ìth tectoric rcrjlitr,. tinrcs (borchole Villaverla- 1, AGIP - GianoÌle et eì. 1998; 'Wcstern In Dolonritcs rhe Richrhofen Conglomerrte is Carnic Alps ler,rbegoli & Lev:rnrì 1982; Vicen- rhc jotm.t) coi'ercd by rhc sh,rllon'nrarine Morbiac-, and Contlin For- r.rr.-n Arp.. R(.o lo .rre.l: ; ro l0 u tcor B.tr -fhc nlrtion. olerlr-ing Buchenstejn /Livinrllongo Formr bieli er rÌ. 1977). rion rcprcscnrs the pelagic sedinrents, rvhich .rrc hetcropic In the Dolomitcs, on thc Adigc platform, pcbbles of u,irh the thick Schlcrn platlorn carbonates. These scdi- thc Richdrolcn Conglorreratc were deposited on an erosion úrerìts ire repleced bl pl:Ltform c;rrbonetc's in thc Longo- :rl sur.trce: lùi/crfcn Formetion (Lower Triassic) to Bellcro- brrdian ,rfter the \\'enscn loìcanìtes. Meurer (2000) pointcd phon I;ormation (Letc Pcrnian) (Brandner 198a, fig.2i). to tlìe frct thlr rhc rarc of subsidence considerlblv acccl crrted in rhe lrte IlÌr,rien-E:rrh L.rdinien (Reìtzi, Secedcn- 3) Thc Anisì:rn terrestrixl scd;mcnts arc distributed sis, Culioni zones). He esrirìrrte \ 200 Bubnotfs (n/Ma) regionellr,. During the Pelsonian Ill)'rien tclrcstrirl sedì- for this pctiocl. T,rkìng into consìdcrrtion thc f;rct thrt in nlents èppcar on the Gond$,ana norrhet n continental sheÌl'. rhc \\'cstcrn Doìonitcs rt Llie Reìtzi/Scccdensis boundatv Thc dcgree of erosion reiches up to several hundred mctrcs rhe plltiornrs ìn the l estern I)olomitcs rìreadl t-c,rched l (,+ 500 m) xt some phces. Ncvettheless, on the northern thìckncss of rpproxinretclv l0O nr (lVIaurcr2O00), r subsid- margin oi the Vardar-Mcliatr branch of the Nco Tcthys, cnce for the pcrìod of Reitzi, Secedcnsìs. Curjonj zones of in the Nolthern Crlcrreous Alps (NCA) rnd the \!'esterr 600-7CC nr c;ur be esrim.rted. ln the central Dolonritcs and Carpathians (WNC), hugc perts of thc carbonate pìatforms C:uni.r, rhe subsidence is highcr. At rhc lìeìtzi/Sececlensis (Stcinalm Lsr.) ncrc drowncd at this tinie. Thc cxact dating .ltttsi,út tcrre:uitl :ulìut\t: n tlr lJiikk.llotntaìn: 675

for the pl.rtlornr droiyninss in the NCA ,rncl irr the'\YNC pelcnce of the terrcstrial sedinents.ìnd thc presence of h:rs not becn :rsccrtaincd ls let. Pclsonirn dro\\ rìing rvcnts r olc.rnitcs :rre chrracteristic, on the norrhern nrîrqin thc :rlc describcd fronr thc NCA bl Schhgcr & Schijl]bcr!:cr dron n ing of plltforms .rnd rhe Ìeck of volcanitcs arc tht' (1973). Mrndl (2000)..rntl fÍonr thc NNC b| Mello ct .rl. rìrosr noriccrblc tendcnq. Thercforc in the Anisian the (1997). Iìeiflin g/Sch tcic r.rlnr/N:iclLrs li.r l-irrrcstones ol b.r- developnrcnt tcndencies of platfornrs ilrc conrriìstirì!Ì ir'ì sin facics s erc depositecl orr rhc rop of thc ì.rsloonìl Stcirr- thcir n:rture. lln Linrcstoncs. Anorher clrorvning cvcnt \\'.ìs dcscribctl bl Schlager 3i Schóllbcfger (I97.1) .rs "lìt'iiìin.:er'\\cnclc". Sincc thc hisrorv oi rhc deleloprrcnr of rhe Bùkk I-ein (l9SZ) describcd rhis rvirh respect ro rhe NCA. .ud Ilount.rins in the Anisiiln lccords rveil s'ith thc assvnetri- Mcllo et ,rl. (1997) nr.rdc .r s imilar dcscriprion iorrhc\\'N(l. c:rl riltin!a of rhe Vardar-Meliirtl branch of rhe Neo-Tethys Ncither terrcstrial sedinrcnrs no considerlblc lolcanires .rlc occ;rn (Vclleclirs 1998/:r, 1998/b), the origins of rhe dn' knon'n flonr this intcrlll e'irhcr-frorl thc NCA or fronr hnd scdirrrcntrrion of thc lìlkk in rhc Anisian c:rn be the WNC. linked ro rhe elcv.rtion oi the updonring s'ins. The simi- Ccrtrinh; rhe sc.r-ler cl oscill:rtion rficcred sedinrcn- ìar fc.rturcs oI the Anisian-Lirdinian strlta of rhc South- rîtion also in tlrc Anjsirn (givcn th;rt it is r continut>Lrs crn Alps - I)inlrides sullscsr rhev coulcl hrLVc been closc phenomenon). The tcrrestrill scclinrcnts .rrc colerecl bl to erch othcr in rhe Triassic. Horvcler, in order to detcr- i transgressivc series (c.g. Morbilc Forrrrlrion,/Contrin nrine the errenr ro s hich the rifting of rhe Vrrdrr-Meliara Fornretitln/Buchenstein Forrnation) r.hich cln alsq be br.ench of rhe Neo-Tethts ocern aliecrcd rhc delclopment s'cll-erpllincd bl a rise ìn thc se..r-loe'l. Prob.rbll thc rinrc' of srrrr:r ol the Southcrn Alps-Dinarides in thc Anisiln- of uplifting coincidcd rvith rhc lorvsrancl. Thc degrc'e of L.rtlini.rn, fulthcr inlcsrigarions rvill lre rcquired. the subsidence follos ing rhc tleltest uplifr, lrorr'eler'. flr exceedcd thc order of rhe custltic seir-lelcl risc. .lckrl'tlu{yncnts. Tìrc ,rLrth,rr is inclebrtd ior dercrm;nin$

rhc lossil' to Anikc; Bór'czi,\l.rkk 1 lor.rnin iicr.r ì. Ols.r Pilx (tl.rr\.cl.r- 1-he precisc drtins of rhe upliftinr: oi rhc soutlr- rhcc.rn'r. \lilLlr \lonosron to\rt,ì.od\), Sindor K(r jcs ((orì( tìnrs.. H.ìì\. Sjndrn Kolics .rncl C..rb.r Pe,r; (Acìderrlic;rl (ìcolosic.ll crn nl:lrgin lnd thc tirrrc oi rhe drosning cr.cnrs orì rhc Jjno\ Rcsc.rrch (ìr'oup, IìLrrl.rpest) lrc rh.rnkcd for rheir corrsrrucrrlc. r.rsclul nor thern Ìrì.ìr'gin of thc Vrltirrr-Nlelirt.r br,rnch of rhe Neo- rdri... ()rrol!r Szr.rna, is :rcknos ledged for hff hclp in ìntcr.pretint Tcthvs occln ;ìre unknol rì .rs 1'et. Furthcrnlor',-'. it is to- rhc r,:r'rr.rlirl i.rcitr. I .rm ren rh.rnkiul to Dr;rgonrir Sk;rbernc nx the dl'unclear rvhethcr rhc uplifrinr: on rhc southern nr.rr- truitlLrl Jircursirn rb,rur theldri.r.rrer.Thi:srrrkr.rs.upporrcdbr rhe gin l as cocr'.rl u'ith the nings rhe \rrionrl scjt rrritìc Rrsc.rrch l:uncl 1O lKA. proiccr nulrl[ìer: TC]77.17). clrol on n()rthern nìir- 'ì he ru r lroI ir g|rrclul ro R:rinel Ziihlke for rlc thorough rc|iew oi rhe gin, or rvhcthcr the uplifting ercnrs prcceclccl rhc drou,n- nr.rnurclipr,.rnel ior his criric,rl comnrenrs r.hich inprwed rhe Iirst drrft inss. $/hiìt cln cert:rinìr'be estrblished is th.rt rvhile on ol rhe,ìì.ù,r'(ipr. I,rot. crerrni critic.rlh rericscd diiier.'nr sr.rgcs oi the' southcrn nrargin rhc uplifrinr of plariolnrs, the .r;'- rhc m.rnu'rripr. IJis criricisn r.r..crv rluch.rpprcci.ted.

I'I,ATI: I nrieririe m.rrrir. In rhr upper lcir corner oi rhe photo brrozo.rn ir'.rgnrcnr crn Le obscned. Ir i. r sedinrenl,i rhe rJeeir!.l ,Ìild Borehol.' lli'ìr,'lc- l a s.rtcr prn of rhc l.rqoon or'.r r,:rlinrenr lesrtked fron the pl,rr- .r-c, I'or.rrrrinilcr.r.rncl.rl{.ìe trt'nr rhc Srcinlln t-ìnc'rt'nc: S. l()rr to lhe birin. 95.5 rr. N =llìr. .t. I'ildnninr,{enú I,.rnrii. l'lorchole lllisl{olc-10, ll+.3 11.1.65 Ir. \l= 7C\. I'l.Afl: l 6. .ttuuln:pìmtell.' \p.. ll6.l n,. \=7a \. c. Pbts,'1tnlù p;t;1,'rr.' 1C iìDìbcl ) /,,.r,.4',"r.' B\\rfi.k\', lì6..{ Scbc\\i/!ijlg\ Sccr;on nì. N=:s\. r. Seberriz Clonql.,nrerlc. Slirllrh rorndcd dolon;rc pcbblcs ot il-l For:rnrinilcr.r fronr thf fesorkcd pcl)br.\. r.rrr ing size in retl cllel nrrrrix. À. .rlunln:pir.ntlLr !p., s./.,/5 s9.S nr. N=7C\. b. /lf .rrr.r \p.. -\.. = 7C\. e. .tl e.onh o4' ìrt I ifl.o.rìrr K, rch.rn sk i Dc\iJ(NP.ìrìria.(,e.5n,.\=7:\. cd. /;,41r",,,,,.,'p.. N-70\. i. .tt ranlro|trclla :n,irr'l S.ìhj. tÌ9.9i-s!).s rrr. N = 70\. (ìr.rinrronr.Thc originrl con'riturnrs rclc ci,nrider.rbh .rkercd q. li'1orfo,/.r \p., I l6.5 rìr, N=lti\. rub'equcnrh: I nnet prrts ol rhu inrr rcl.rsrs s elc dissolred, rhcir h. P.rrt oi rhr conqlonrer'.rtc lrlecci;r l.rrcn lUnir ll1. l:.rbric ol r[c nx,uld. rr.' Iill(l io br dokrsp.rr. N=4tr. rock i. gr'.rin-supponeil..ì/e rnJ Í,un,ln$.,'i rhe pebblt'.rrr L tl t,n,l.':7 t n,ttJitn at,r S.rh j. \ = 7cr. (ir.rins rrn inr. ol rcrcr.rl

I.-

I :.a 1,...' r. i_ i

,*" fì'

.-t Atttstttlt ttrr(stl.tal ttdil t)tt5 tbe Bnlch t, ,lloLtntains 677

,|' 't-

.l'

PLrlfF_ 2 o7S l: \'alledis

REFERENCES

Allen PA. E: Allcn J.R. (1990) - Basin An:rlvsis. Principlcs & De Z:rnchc \1. lir.rnzin A.. Gienoll.r Iì, I{ictto 1ì & Sìorpecs (ì. Applic.rrions. V of 4St pp.. Blaknells, Oxford. I l99l) - Thr I)iz dr Percs \rcrion (\'a|leor:r-C)l;rng, Pustc- Ahiner D. (1993) Third renrnrk on rhe scolosl oi K,ìr.ìks.r ril Y.rllcr, It.rìt1. -\ rerppr;rìsrl oi rhe -\nisirn srrarirraphl basin. Arr Anisian nrcg:rblock ìn nonhcrn CentÌ.1! Anr in thc Dolonrircs. Icl. Ceal. Hdi.,3i,'l: l]7-111, Bascl. tolìa: microp:rlcontologic, srrarigr:rphic and tccronic inr- Dc Zrnchc \i, Cirnoll.r P, Nlictto [ì, Siorpacs O. El Vai. PR. plicarions for the rìftinq srigc of Kar:rkl'a basin, Tr.rrkcr: (199i) Tri.rsric sequcncc s!rtriliriphl jn rhc f)oionritcs Rer de hrléogìologie, l211: 1-17. Genér'e. (lt:rlrJ:.l1orr. Sc. Geol.. 1i l-17, Padov.r. 'lopo:raphic Asserero R., Brusca C., Geerirni M. & JadoLrl F. (1977) -îhe Dixon T.H.. Irins f..R. & Fr.rnhlin 13.J. (1939) Pb-Zn mineralization irr rhc Triassic oî the f)olnnrircs. .rnd lolcenic .rsvlrrretrl rround rhc Red Sc:r: cor,strains

Geological hisrorl' and qenctic interprcriìrì ons. L ì *l t I r ia on :.if t models. Ti tt on i c s, 3 1 6: 1 1 9-l 12 i 6, \\r,ìshin!:ton. ,IIùeftlin, 231: 1-34, lVIiìeno. Dosztílv l-. & Jr;zs.r S. (1992) (ìcochronoloqic.ll cveluation Brìogh K. (1961) Die gcoloqischen Bildunecn des liikli of ìllcsozoic forrl;rrions of D.rlnó Hill xt l{ec\k on rhe Gebirges. - ,Ann. Huug. Geol. Itst., l1ì: 2-15-719, b,rsis ol radiol.tri:rns and li-,\r .rgc dere...ltt r Ca!. Hntry., Bud:lp€st. ,15t1: j/l 393. Budapest. B.rrbìcri G., Dc Zrnche V, Di Lallo E., Mierro Iì & Sccle.r lì. F:rrabegoii E. & I-c'r'irntj D. (l9S:) - Tri,rssic Strirtlglephl .rnd (1977) - Middle Trirssic enrcrsion phirscs in rhc Rcco;rr o Nljcrof:rcics of the Nlontc Plcros (Vestcrn Crlnie, ILall ). arca (Vicentian AIps. N.E. ftalv). N./0. Geol. htliont. Àrcrc,s, 6: 37-5S. Erlenqen. ,ì10., 9: 523-5i1. Stuttgarr. Farrbcsoli E.. J;rdoul li. S \lanincs ì1. (l9St) Srrarigrriia IJcchst;idr T. & Brandncr R. (1970) Das Auis ztischcn Sr. c prìeoqcoqr:rii.r ;rnisiche dcllc A[i Giulie occidentali Vigil Lrnd dem Hòhlcìrsteinral (Priuscr- und C)lrrnscr (Àlpi Melidion,rll - h.rli.r). /lri. Ir. Palaont. Srrat.,9l/2: Dolonrirc, Súdtirol). - FesLbanl Geol. Inst., ))a-Jahr- ll7 196, ìvIil:rno. Feier, Unit Innsbruck,9- 103, Innsbrucli. Fois E. N Jedoul Ir. (l9S-i) La dors:ìlc peleoc:rrnicrr :rnisice dei Bclrczì-tr4akk A. ( 1996) Forrninifera of thc îiassic form.rrions Prrntebba. 1lr;. It. Paleou. Sar',rr., S9: i .lC. Ilil.rno. of Alsó Hill (Northcrn Hungary). P.rrt f: Foreruinifcr G,rer:rni \1., Gn;rccc,lini l\1.. J.rdoul Ij. N Gerz;rnri c. (1998) L" - '.'.-\lr.', ^I sr.in.l", I n,c\rnns I-or- :ricn..1rr.r JVlultiordcr sequence srrirtigllphl in thc Trirssic slstrm Geo[. Hung., 39,r2: 175-221, Budepcst, ol rhc Wcstern Southern Alps. In: Mcsozoic rnd Ceno- BoscÌlini A. (1991) Geologv of the Dolonritcs. An introcluc- zoic Scqrrcnce Str:rtigrephr ol fluropean B.rsins. -!EP,l1 tion. Dolomier.r Conference on Certron;rrc l)lariornrs lnd Slcc. I'ub.. (,C: 701 7t7.'ltrlr.r. Dolonritiz.rtion. V of .12 pp., Ortisci. Girnoll.r Iì El J.rcquin T. (199S) Ttirssic scqucncc srrrlisraph- 13oscllinì A. (1998) Geologic' dcr Doìomitcn. \{ of l9l pp. ic hanren'ork of rvcstcrn ELI()p.;ìn basins. In: Nlesozojc Ver l;r gslrrsurk Athesi:r, Bozcn. iì d Cenozoic SeqLrcnce Strltiu|lphv of .rn Basins. Brandner R. (1972) ,,Sùd:rlpines" Anis in den Lienzr:r .SIP,ll Sptc. Dr1.,.. 6C: 6-{]-650. Tulr.r. Dolomjtcrr (DreLrzur) (cin Beitrag zuralpin-dinarischen Ciarroll.r Il. Dc Z.rnchc \'i N llir rro Iì ( l99S) - Tri:ìssic seqùence Grenzc). ,ì/i.r. Ges. Geol. Bergbaustul., 21 : 1-13-l(rl, Strerigraphr in rhe Southcrn r\lps (Norrheln Italr'): dci- Innsbrucl<, inition of sequcnccs and b.rsin clolution. In: Mesozoic Brandner R. (193.{) - Meererspiegelsch*'anl