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Original scientific paper Received: October 7, 2014 Accepted: October 15, 2014 Composition and importance of Upper Triassic (Upper Ladinian – Lower Carnian) breccia in stratigraphy of External Dinarides Sestava in pomen zgornje triasnih (zgornje ladinijskih – spodnje karnijskih) breč v stratigrafiji Zunanjih Dinaridov
Luka Gale1, 2, *, Dragomir Skaberne2 1Faculty of Natural Sciences and Engineering, Department of Geology, Privoz 11, 1000 Ljubljana, Slovenia 2Geological Survey of Slovenia, Dimičeva ul. 14, 1000 Ljubljana, Slovenia *Corresponding author. E-mail: [email protected], [email protected]
Abstract Izvleček A sequence of boulder breccia, separated by several emersion horizons is recognized as part of the Upper - Na območju Medvedice (osrednja Slovenija) smo v Ladinian – Lower Carnian Cassian Dolomite and Lime- zgornje ladinijski – spodnje karnijski formaciji kasi stone Formation in the area of Medvedica (central Slo- - janskega dolomita in apnenca prepoznali zaporedje venia). The composition of clasts, determined from thin blokovnih breč, ločenih z več emerzijskimi površina sections in the context of Late Ladinian – Early Carnian mi. Sestava klastov, določena na podlagi zbruskov ob platform models suggests their origin in the transition upoštevanju modelov zgornje ladinijskih – spodnje between the inner platform/lagoon and the back-reef - karnijskih karbonatnih platform kaže na sedimentacijo area, alternatively in the internally differentiated la- - apnenca na prehodu iz notranje platforme/lagune v za goon with swells. The emergence of the platform is sug- grebensko območje ali na notranje diferencirano lagun gested to correspond to the upper sequence boundary sko okolje z lokalnim reliefom. Emerzija platforme bi se of the Car1 depositional sequence from the Southern - lahko skladala z zgornjo sekvenčno meje depozicijske Alps. The platform growth subsequently continued un- sekvence Car1 Južnih Alp. Rast platforme se je nada til the uppermost Julian, when the second emergence ljevala do konca jula, ko je bila dokončno prekinjena (upper sequence boundary of the Car2 depositional z drugo emerzijo, ki ustreza zgornji meji depozicijske sequence) finally terminated the growth of the Cassian sekvence Car2 v Južnih Alpah. platform. Ključne besede: - ne Alpe, »cordevolski apnenec in dolomit«, Cassianska Dinarska karbonatna platforma, Juž Key words: Dinaric Carbonate Platform, Southern Alps, »Cordevolian limestone and dolomite«, Cassian platforma, sekvenčna stratigrafija platform, sequence stratigraphy 108
Introduction Geological setting
A substantial amount of the carbonate sequence Medvedica is a largely forested low hilly area of the External Dinarides and Southern Alps belongs to carbonate platforms established basin (Fig. 1). According to Placer[27, 28], this area after the cessation of Ladinian volcanism[1, 2]. structurallysituated on thebelongs SW brink to External of the GrosupljeDinarides, karst dur- Until the Early Julian, up to 600 m of limestone ing the Triassic and Early Jurassic situated on deposited, later mostly transformed to do- the southern passive continental margin of the lomite[2]. In terms of lithostratigraphy, these Neotethys (Meliata) Ocean[29, 30]. The evolution carbonates are known in the Slovenian litera- of this area was strongly affected by the Middle ture as the »Cordevolian limestone and dolo- Triassic extension, and, after cessation of tec- mite«[3–5] or the Diplopora Limestone[6, 7]. The tonic activity, by a gradual recovery of carbon- term Cassian Dolomite and Limestone Forma- ate production and levelling of topography[31, 32]. tion (CDLF) is used herein (see also[8–12]). The The following description of lithological units debate about the correct interpretation of age is based on author’s personal observations. of the CDLF mostly revolved around the correct determination of dasycladacean algae[10, 13]. Buser[20, 22] and Dozet[23]. The studied area is During geological mapping of a smaller area Reader may further refer to descriptions by
sequence of breccia with up to 2 m large boul- andsituated the Ortnek between fault two to majorthe west NW-SE (Fig. directed 2). Nu- derssouth-west was noted of Grosupljeinside the CDLF (central along Slovenia), the newly a merousfaults, namely minor faultsthe Dobrepolje create a complex fault to picture the east of cut forest road. The scope of this paper is to de- fault-bound blocks. This, however, is in contrast scribe and interpret the origin of breccia. with interpretation made by Buser[19], showing a generally undisturbed Lower to Upper Trias- sic succession. Previous research of the studied The oldest succession belongs to the Lower area Triassic Werfen Formation (Fig. 3). The lower part of the formation is missing, while the rest The first geological mapping of this area was of it consists of light brown or reddish cal- carried out by M. V. Lipold and G. Stache[14]. cisiltite and dark grey silty marlstone, and me- Their work, however, remained in the form of dium bedded oolite. Small flakes of mica are a manuscript map[15]. Stache[16] and Vetters[17, 18] later produced less detailed maps. In the scope LJUBLJANA of geological mapping of Yugoslavia, geological mapping was carried out by Buser and co-work- SLOVENIA N ers[19, 20] of Medvedica, was re-ambulated in the 1980s. . The area around Županova jama, east[21]; however, the supplemented geological map The results were published by Gospodarič is too general for the purposes of this study. Škofljica Buser[22] later gave a short description of the - Ig Grosuplje Pijava ofgeological Ladinian structure volcanoclastics between in Št.Medvedica. Jurij and The Ve Gorica stratigraphylike Lipljene. ofEspecially the wider notable area south is his andmention east Št.Jurij
[3–5, 23–26] Dozet . 5km of Grosuplje has recently been investigated by Vel.Lipljene Figure 1: Position of the studied area. The rectangle represents position of Figure 2.
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N laminated dolomite and micriticlaminated limestone dolomite and Št.Jurij 500m N micritic limestone
Udje Dobrepolje faultŠt.Jurij Jurassic 500m497m Udje Dobrepolje fault Jurassic faulted 497m faulted stromatolitic dolomite (Mainstromatolitic Dolomite) dolomite Vrbičje (Main Dolomite) Vrbičje bauxite, red clastics, dolomite (Mohorjebauxite, red fm) clastics, dolomite bxbx bx bx bxbx bx bx bxbx bx bx
Carnian Nor.-Rhae. breccia(Mohorje fm) bxbx bx bx bxbx bx bx bxbx bx bx Carnian Nor.-Rhae. brecciamedium to thick bedded limestonemedium to with thick green bedded algae M e d v e dc i a (CDLF)limestone with green algae M e d v e dc i a MMoravčeoravče e (CDLF) e d conglomerate/breccia, tuffite, MMoravčeoravče d v tuffaceousconglomerate/breccia, sandstone, micritictuffite, Ortnek fault e v bx bx bx limestonetuffaceous with sandstone, chert micritic ? Ortnek fault e d limestone with chert i bx bx ? bx d c VVelikeelike LLipljeneipljene i a VVelikeelike LLipljeneipljene medium-thick bedded or c massivemedium-thick dolomite bedded or
a Anisian Ladinian massive dolomite Predole beds (Lower Jurassic) Anisian Ladinian Predole beds (Lower Jurassic) Main Dolomite (Upper Tuvalian?-Norian-Rhaetian) Main Dolomite (Upper Tuvalian?-Norian-Rhaetian) calcisiltite, marlstone, oolite Mohorje Formation (Upper Julian-Tuvalian) (Werfencalcisiltite, fm) marlstone, oolite Mohorje Formation (Upper Julian-Tuvalian) (Werfen fm) Cassian Limestone (Upper Ladinian-Lower Julian)
Cassian Limestone (Upper Ladinian-Lower Julian) Lower Triassic Cassian Dolomite (Upper Ladinian-Lower Julian) Cassian Dolomite (Upper Ladinian-Lower Julian) Lower Triassic Volcanoclastics, limestone with chert (Ladinian) calcisiltite massive dolomite Volcanoclastics, limestone with chert (Ladinian) calcisiltite massive dolomite Anisian Dolomite marlstone massive limestone Anisian Dolomite marlstone massive limestone Werfen Formation (Lower Triassic) oolitic limestone boulder breccia Werfen Formation (Lower Triassic) oolitic limestone boulder breccia Fault (visible; covered; assumed) bedded dolomite bx bx bauxite Fault (visible; covered; assumed) bedded dolomite bx bx bauxite Normal geologic boundary tuff sandstone Normal geologic boundary tuff sandstone cherty limestone marly dolomite cherty limestone marly dolomite Figure 2: Geologic map of the studied area. The section with micritic limestone breccia is marked by bar. micritic limestone Figure 3: Schematic lithostratigraphic column for the characteristic. Various bivalves, gastropod Nat- Medvedica area (not in the scale). Note that the stratigraphic Munster, ammonite (? sp.) position of the breccia inside the Cassian Dolomite and iria costata Tirolites Limestone Formation (CDLF) is only tentative. and ichnogenus Rhizocorallium were found. Oolitic limestone may contain numerous small gastropods. tuffite, tuffaceous sandstone, conglomerates, In the upper part of the Werfen Formation, breccias, and black micritic limestone with thin to medium bedded dolomite of dusty ap- black chert and claystone partings follow. A si- pearance predominates, gradually passing into licified ammonite has been found in Medvedica medium-thick bedded or seemingly massive coarse dolomite. No attempt has been made to the genus Kellnerites (L. Krystyn, pers. com. to recover microfossils from the latter, and An- by B. Vičič in 2009, and questionably attributed- isian age is assumed solely on the basis of su- tabase[33], this genus ranges from Late Anisian perposition. byto EarlyB. Vičič). Ladinian. According Thus, to the the dolomite Paleobiology below Dathe The upper boundary of Anisian dolomite is unconformity is attributed to the upper part of nowhere preserved, so its continuation into Anisian dolomite, while the following volcano- younger units remains interpretative. One as- clastic, clastic and limestone succession rep- sumption is based on a road cut in the area of resents Lower Ladinian. The local emergence Medvedica, where an irregular palaeosurface is around Anisian-Ladinian boundary has been visible on top of stromatolitic dolomite. The pa- advocated before by Dozet and Godec[6] in the laeosurface is filled and covered with conglom- area of Bloke (southern Slovenia), but the age erate/breccia consisting of dolomitic clasts of the supposed unconformity is not supported and limonitic matrix. Poorly exposed greenish by fossils.
Composition and importance of Upper Triassic (Upper Ladinian – Lower Carnian) breccia in stratigraphy of External Dinarides 110
1 2
3 4
5 6
7 8 9
Plate 1: 1 Poorly sorted boulder breccia. | 2 Red surface of brecciated dolomite. | 3 Leached-out thalli of dasycladaceans. | 4 Red and green mudstone (emersion level). | 5 Dolomite clast embedded in mudstone. | 6 Emersion on the upper side of calcarenite bed. | 7 Interchange of light and dark grey levels with Tubiphytes. | 8 Detail from Figure 7. | 9 Breccia with bauxite matrix (base of the Mohorje Formation?).
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1 2
1 mm 0,5 mm
3 4
0,5 mm 1 mm
5 6
1 mm 1 mm
7 8 c
1 mm 0,5 mm
Plate 2: 1 Fine-grained breccia with reddish »haematitic« matrix. Thin section 207. | 2 Angular clasts with Tubiphytes-like micriproblematica. Thin section 207. | 3 Recrystallized wackestone passing into bioclastic grainstone. Breccia clast. Thin section 200C. | 4 Partly winnowed intraclastic-peloidal packstone. Breccia clast. Thin section 201. | 5 Winnowed bioclastic-peloidal packstone with dasycladaceans. Breccia clast. Thin section 202. | 6 Dasycladales. Breccia clast. Thin section 208B. | 7 Clasts of cementstone with cockades and Tubiphytes in partly dolomitized reddish »haematitic« matrix. Thin section 205. | 8 Tubiphytes-like fossils in peloidal grainstone. Note bladed spar encrusting grains and the corrosive cement (C) associated with reddish »haematitic« matrix. Thin section 205.
Composition and importance of Upper Triassic (Upper Ladinian – Lower Carnian) breccia in stratigraphy of External Dinarides 112
1 2
1 mm 0,2 mm
3 4
0,5 mm 0,2 mm
5 6
0,2 mm 0,5 mm
7 8
1 mm 0,5 mm
Plate 3: 1 Recrystallized winnowed bioclastic-peloidal packstone. Thin section 199. | 2 Tubiphytes sp. Note the coarse internal network. Thin section 207. | 3 Tubiphytes or similar microproblematica. Thin section 211. | 4 Tubiphytes sp. Thin section 200A. | 5 Tubiphytes sp. Note the internal cavity and the branched habitus. Thin section 207. | 6 Tubiphytes sp. in clast. Note the internal cavity and the branched habitus. Thin section 207. | 7 Tubiphytes sp. Thin section 208A. | 8 Tubiphytes sp. Thin section 207.
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1 2
0,1 mm 0,2 mm
3 4
0,1 mm 0,2 mm
5 6
S
0,1 mm 1 mm
7 8
S
S 1 mm 1 mm
Plate 4: 1 Endotebanella bicamerata Salaj in Salaj et al. Thin section 204. | 2 Endotebanella bicamerata Salaj in Salaj et al. Thin section 200C. | 3 Turriglomina mesotriasica (Koehn-Zaninetti). Thin section 208B. | 4 Duotaxis sp. Thin section 200C. | 5 “Trochammina” jaunensis Brönnimann & Page. Thin section 209. | 6–7 Corrosion of matrix and clasts, followed by deposition of clear mosaic spar (S). Thin section 200B. | 8 Clear spar (S). Thin section 208A.
Composition and importance of Upper Triassic (Upper Ladinian – Lower Carnian) breccia in stratigraphy of External Dinarides 114
The next lithostratigraphic unit, the Cassian Do- lomite and Limestone Formation (CDLF) covers large area, but its lower boundary is faulted. It dolomiteThis transition, with fromshale theinterlayers) uppermost to Selo the at Main Rob consists of light gray medium to thick bedded DolomiteMember of(bedded the Mohorje stromatolitic Formation dolomite), (bedded micritic limestone, which frequently contains is exposed along a steep foot-path east of the dasycladaceans and cockade textures. Equally large area is covered by seemingly massive, The Main Dolomite is distinguished from other coarse, very porous white dolomite to the west dolomiticstudied area, units in theby vicinitymedium of toPijava thick Gorica. bedding and south of the studied area (see Buser[19]). and the presence of stromatolites (see[35]). The age of the CDLF is a matter of great contro- Finally, the youngest pre-Quarternary rocks versies, fully explained by Celarc[10]. A Late La- belong to Lower Jurassic dolomite and bedded dinian and Lower Carnian age is assumed after micritic, oolitic and bioclastic limestone, i.e. [34], and Celarc[10]. Predole beds sensu Dozet[4] (also Krka Lime- Along a fresh forest road-cut, a succession of stone[36] [37–39]) . Pleničarclast-supported and Premru boulder breccias, subordinate calcarenites, and green and red claystone is ex- , and Podpeč Limestone Materials and methods blocks of CDLF. The thickness of this succession posed. The breccias consist of up to 1.5 m large The succession of breccias was measured along - is at least 15 m, with individual breccia beds at withleast 9.5 mseveral thick. tens The of brecciameters can thick be laterallyCDLF body. fol seaa forest level. road Due at to coordinates: several minor 45° faults, 54′ 44″ the (lat.), suc- Thelowed breccia for at interval,least 100 m, which and is seems here described to continue in cession14° 37′ 23″could (lon.) not andbe elevationreconstructed 410 mentirely. above detail, was overlooked by previous researchers To avoid misinterpretation, we present the due to the previous lack of fresh road cut and section in three segments, with no interpreta- a strongly karstified surface, which makes the - low amount of matrix poorly visible. The CDLF is overlain by clastics of the Moho- tion of succession (Fig. 4). Fourteen thin[40] clas sec- [4] sificationtions of size was 47 mm × 28 mm followed in describing and one of their size Formation in the surroundings of Medvedica texture,76 mm × 51 mm and semiquantitative were made. Dunham comparison rjecomprises Formation black sensuand red Dozet coarse-grained. The Mohorje quartz charts[41] used to estimate proportion of indi- sandstone, red siltstone, black shale, dark vidual components. brown siltstone, thin-bedded, brown, partly do- lomitized and bituminous limestone, red peb- bly sandstone with pebbles of lithic grains and Description of section quartz, and red and white, cross-laminated lith- Coarse breccia oolitic »bauxite« is common in the lower part of The predominant lithology of the measured theic-tuffaceous formation sandstones. (Pl. 1, Fig. 8).Red, According rarely also to gray,divi- segments is very poorly sorted coarse breccia, sion by Dozet[4], these lithologies correspond to with limestone clasts ranging from less than
thickness varies from a few tens of centime- gapthe Rupebetween Member the top from of thethe CDLFmiddle and part the of clas the- 1 cm to over 2 m in size (Pl. 1, Figs. 1–2). Bed ticsMohorje is assumed. Formation, No fossils so a notablewere recovered stratigraphic from hardly discernible irregular internal surfaces. Claststres to areover very 9 m. angular Such thick or may layers be subrounded.may contain Julian (i.e., Julian 2)-Tuvalian age was given to The amount of matrix is very low. Yellow or red- formationthe Mohorje by FormationDozet[4]. Transition during our to the fieldwork. Upper dish »haematitic« matrix is knead among clasts
is gradual, marked by medium-bedded dolo- contacts (stylo-breccia). In other cases, gray miteTuvalian with (?) a todecreasing Norian-Rhaetian amount Main of shale Dolomite part- spar(Pl. 2, fills Figs. 1, spaces 7), betweenwhich are clasts. in places Dolomitization in stylolitic ings between beds upsection (see also[4, 8, 12]). obscured a few layers to various degrees, but
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most common. Neomorphically altered mol- lusk shell fragments, echinoderms, foramin- ifera, green algae, ostracods and brachiopod fragments are subordinate. Thin encrusta- tion by microbiallites is sometimes present. ―In the cementstone, only Tubiphytes is rec- ognizable. Specimens are oriented approxi- ― mately in the same direction, separated by
to Tubiphytes. Cementstone may interchange withbladed bioclastic-peloidal spar. Rarely, peloidal wackestone packstone to clingspack- stone with Tubiphytes in decimetre-thick lay-
―Washed-out bioclastic-peloidal wackestone, packstoneers (Pl. 1, Figs. 7–8). to grainstone with dasycladacean ― algae is the next common clast type (Pl. 2, Figs. 5–6). In the field some several centi- metres long leached-out bundles of dasy- cladaceans are visible (Pl. 1, Fig. 3). Dasy- cladacean thalli are in places partly filled by peloidal packstone, and partly by brown- ish bladed spar. The intermediate space is filled with intraclastic-peloidal packstone. Tubiphytes is common, while benthic fora- minifera and fragments of mollusc shells are subordinate. The matrix (%) is rattled by patches of vugs filled with spar and resem- bling birds’ eyes texture. ―The next group of clasts is represented by peloidal and intraclastic partly winnowed ― packstone to grainstone and fine-grained Figure 4: Geological section of breccia succession. rudstone (Pl. 2, Figs. 3–4). These two textures may be present in the same clasts, separated composition of clasts can usually be readily ob- by dark, dense, more micritic boundary served in thin sections. No fossil remains were - found in the matrix of the breccia. In the clasts, ally. In packstone peloids predominate, but the following foraminifera were determined: a1–1.5 mm significant in proportionthickness, oris presentprobably individu of Tubi- Turriglomina mesotriasica (Koehn-Zaninetti), phytes »Trochammina« jaunensis Brönnimann & Page, to bioclasts other than Tubiphytes, such as Diplotremina placklesiana Kristan-Tollmann, echinoderms origin. andAround rare 10 %mollusc of grainsfragments. belong In Tolypammina sp., Reophax sp., Endoteba/En- fine-grained breccia, intraclasts with micro- dotriada sp., Duotaxis sp., and Duostominidae bialites, microproblematica (Tubiphytes), or (genus Krikoumbilica?). plain micrite, and peloids predominate. Echi- noderms, mollusc fragments and Tubiphytes Clast composition: are most notable of rare bioclasts. Dasycla- ―Among clasts, bioclastic-peloidal wacke- daceans and brachiopod shells are very rare. stone, packstone to grainstone with Tu- Few ooids were also noted. Clasts are bound ― biphytes remains is the most common type by blocky spar cement. Clear, mosaic spar - may also be present as the youngest cement, nowed away, and the interstices filled with cutting through older constituents (Pl. 4, blocky(Pl. 2, Figs. 2,spar. Peloids 8). The and matrix Tubiphytes is partly are win the Figs. 6–8).
Composition and importance of Upper Triassic (Upper Ladinian – Lower Carnian) breccia in stratigraphy of External Dinarides 116
―A special type of clasts is represented by in- Dolomite terchanging bioclastic-peloidal wackestone Coarse dolomite completely replaces limestone ― to packstone, and microbialitic bindstone, - forming laminated texture. The first type of ture sometimes points at the original breccia, laminae is similar to already described mi- orin bedsto horizontally of 5–30 cm inlaminated thickness. limestone, The ghost texde- crofacies types: peloids and intraclasts with scribed above. Tubiphytes predominate over other clasts (Tubiphytes, foraminifera, shell fragments, Red and green mudstone gastropods). Both types of lamina are rattled mudstone are clearly visible in segments A and part by calcisiltite and upwards by bioclas- BRed (Pl. and 1, Fig. light 4). green, The lower up to bed 10 boundarycm thick bedsmay beof tic-pelletalby vugs (30 % packstone, of total brownish area), filled bladed in lower spar slightly irregular surface, but this might also be and mosaic spar. due to differential compaction or dissolution. ―Oncoid rudstone is the next clast type. Other At least one of these layers contains broken grains besides microbialitic oncoids are Tu- pieces of dolomite, reworked into mudstone ― biphytes, echinoderms and shell fragments. ―Coarse dolospar clasts represent completely change laterally, but it is most often red. More dolomitized clasts of variable composition. subtle(Pl. 1, Fig. 5).than discrete The colour layers ofare mudstonereddish upper may ― surfaces of other beds (Pl. 1, Fig. 6). Packstone Subordinate to its coarse-grained variety is Platform characteristics
Internalpackstone bedding to fine-grained and lamination rudstone is sometimes (Pl. 3, Despite its large areal extent[42], the composition present,Fig. 1). Bed where thickness massive is fine from grained 5 cm to and 35 cm. in- of platform carbonates of the CDLF received versely graded horizons interchange. Allo- chems are represented by peloids, intraclasts macroscopic aspect of dolomite and limestone, (mudstone, pelletal packstone, microbial- withoutlittle attention. much detailed Researchers sedimentological mostly describe inves- ites), Tubiphytes, mollusc fragments, foramin- tigation. Platform carbonates are usually dolo- ifera (Endotebanella bicamerata mitised, and the primary composition is thus - pod fragments, ostracods, and calcimicrobes.Salaj in Salaj regarding composition of Late Ladinian-Early Theet al.) partly (Pl. 4, washed-out Figs. 1–2), matrixechinoderms, is recrystallized brachio Carnianstrongly platformsobscured. Thein the majority Dolomites of information area thus into microspar. derives from the study of isolated, mostly grav- ity-displaced blocks (cipits) of the platform rim Fine-grained rudstone and slope, which were sealed from dolomitiz- In fine-grained rudstone, reddish »haemati- ing fluids by the enclosing basinal marls[43–48]. tic« matrix is squashed between allochems, or Among these, blocks exhibiting boundstone fa- these may be in stylolite contact. Clear blocky cies received considerably more attention than spar cross-cuts clasts and matrix. Allochems other facies types, which might potentially give are mostly intraclasts with microbialites, Tubi- a better glimpse on the platform interior. In the phytes, fuzzy peloids, and rare bioclasts (echi- platform-to-basin transect, Biddle[44] succes- noderms, rare and questionable sponges). sively shows (from the interior towards basin) subtidal lagoon and dasycladacean meadows, Calcitulite (mudstone) intertidal sand shoals, algae dominated reef Subordinate to other lithological types is dense, flat, organically bound submarine-cemented gray limestone with horizontal lamination. reef complex, fore reef breccias and muds, and [49] lists a similar succession of depositional environments: in Bedding is thin, up to 10 cm in thickness. thefinally inner a basin platform plain. area, Reijmer dasycladaceans domi-
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nate over calcimicrobes, peloids, foraminifera, [55], Flügel[56], and micrite lumps; the back reef area is charac- Henrich[57], and Dullo and Lein[58]. Tubiphytes terized by algal-foraminiferal and sponge-coral andalso othernoted microproblematica,by Brandner and Resch however, are as- patch reefs; the reef margin with abundant sociated with sphinctozoan sponges and corals, Tubiphytes, other microproblematica, peloids none of which were found in Medvedica. and »evinosponges«, and the transition to the To finally summarise, for the time-equivalent upper slope with encrusting sponges, corals, platforms a cyclic peritidal sedimentation is peloids and diverse skeletal grains (including characteristic for the innermost platform. No dasycladaceans, gastropods, and Tubiphytes) such clasts were found in the Medvedica brec- [49], however, focused his atten- cia. The wackestone/packstone with dasycla- tion on composition of fine-grained slope/ba- daceans microfacies type fits well into the inner sinfollow. resediments, Reijmer with grains of predominantly platform/lagoon area, while the enrichment margin and slope origin. A more detailed analy- with Tubiphytes probably better corresponds sis of the platform top itself is given by Seeling to a slightly more outer position, closer to the et al.[50] on the example of Concarena buildup. In reef margin in the Cassian Dolomite model. On- the lagoon area, Seeling et al.[50] describe a reg- coid rudstone and more grainy varieties may ular alternation of peritidal carbonate cycles. be placed even slightly more towards higher- Tubiphytes framestone and early marine ce- energy environment of the back-reef area. Tak- mentation were found characteristic for tran- ing the predominance of dasycladacean and Tu- sition from the lagoon to the back reef area. A biphytes rich clasts into account, sedimentation monotonous cyclic sedimentation of subtidal, is considered to take place in the transitional peritidal and supratidal carbonate was noted zone between the lagoon and the back-reef also by Trombetta[48] and Keim and Schlager[51]. area or, alternatively, in the internally differen- Missoni et al.[52] recently investigated Wetter- tiated lagoon with swells. stein-type carbonate platform in Serbia. They could not recognize the platform top, but they do mention abundance of Tubiphytes in Ladin- Stratigraphic position and genesis ian to Lower Carnian platform carbonates. Ac- of breccia cording to Bole[53] the Wetterstein Limestone and Dolomite of the Peca massive deposited As already noted, the stratigraphic position of in back-reef and reef setting. The former con- the breccia succession remains dubious due to tains intraclastic-bioclastic, and intraclastic- coverage. The lower boundary is currently in- bioclastic-peloidal wackestone and packstone, terpreted as fault-bound, while the succession as well as limestone and dolomite with stro- seems to continue with the unbreciated CDLF matolites. Among bioclasts, codiaceans are the (Fig. 2). The lithology itself gives little oppor- most common, followed by bivalve fragments, tunity for a more precise determination of age, foraminifera and echinoderms. The reef car- rather than on the basis of superposition. The bonate is built by corals, sponges and also mi- only foraminifera found within the matrix in croproblematica. Oncoids are present in almost Medvedica is E. bicamerata, with stratigraphic all facies. In Ladinian-Carnian reef of Calabrian range from Anisian[59] to Norian[60, 61] or even Apennines, Boni et al.[54] distinguished between [62]. Endotebanella bicamerata is the the reefal boundstone facies with sphinctozoan usual element of Middle Triassic assemblages sponges, biogenic crusts, Tubiphytes, other mi- Rhaetianpresent within clasts[63], so the assemblage croproblematica and rare corals, the fore-reef within breccia clasts is not markedly differ- debris rudstone facies, and the dasycladacean ent (that is within stratigraphic resolution of- packstone-grainstone back-reef facies. Accord- fered by foraminifera at the time), despite the ing to Boni et al.[54], this reef association is simi- fact that truncation of calcite veins at the edges lar to the Wetterstein limestone of the Northern of clasts suggests a complete lithification of Calcareous Alps. The importance of microprob- limestone and their tectonic deformation pri- lematica at the Wetterstein platform edge was or to brecciation. Turriglomina mesotriasica,
Composition and importance of Upper Triassic (Upper Ladinian – Lower Carnian) breccia in stratigraphy of External Dinarides 118
restricted to Anisian and Ladinian[63], provides a The importance of emersion pre-Carnian (at most Lower Julian) age of CDLF. surfaces for correlations Unfortunatelly, we did not try to determine dasycladaceans. The uppermost boundary of Emergence horizons are a valuable marker as the entire CDLF is represented by clastics, vari- they allow precise subdivision and dating of ously named as Borovnica beds[11, 32, 64], Grosu- similarly looking dolomitized platform carbon- [23] [8, 9, 12, 65], Zaplaz For- ates which would otherwise prove to be impos- mation[3] [4]. Bivalves sible to distinguish[71, 76]. Moreover, as emer- foundplje-Orle in bedsthe lower, Raibl part beds of these beds include gence often results from eustatic sea-level drop, Lopha montiscaprilis, or as Mohorje (Klipstein) Formation (Umbrostrea? it may become possible to correlate lithostrati- montiscaprilis in Szente et al.[66]), indicative for graphic units on at least regional scale[71]. De- the uppermost Julian[67]. The measured succes- spite the lack of relative sea level curves in sion may thus be very conservatively placed the northern External Dinarides, to which the between the uppermost Ladinian and the up- Medvedica area belongs, we may resort to the permost Julian. sequence stratigraphy set for the Southern Poor sorting, angularity of clasts, and small Alps area. According to Gianolla et al.[71] and amount of matrix point at short transport of De Zanche et al.[76], the time frame from Late clasts. Green and red mudstone point at subaer- Ladinian to end-of-Julian in the Southern Alps ial exposure. Mudstone seems to correspond to comprises four sequence stratigraphic cycles, residual clay in Durn et al.[68]. The breccia can with systems boundaries marked on the plat- be thus interpreted as emersion breccia[69, 70], forms by emersions. The Car1 depositional or as dissolution breccia accumulated on sub- sequence (Late Langobardian to Early Julian) aerially exposed surface[68]. The repeated oc- represents a time-frame for deposition of the currence of emersion levels (residual clay) on Cassian Dolomite 1 platform carbonates. Its up- upper bedding planes, as well as rare intercala- per sequence boundary separates the Cassian tions of micritic and calcarenitic beds, however, [76]. The point at oscillating, rather than a single drop next sequence, Car2, comprises the entire Cas- of sea level, and the lack of bauxite deposits Dolomite 1 from the Cassian Dolomite 2 similarly discredit a longer-lasting emergence. Early Julian to the latest Julian. At the end of this Foraminifera, found in calcarenite, thus point at sequence,sian Dolomite 2 the intraplatform platform, ranging basins inwere age partly from intervals of re-flooding of the surface. levelled-out due to a high export of carbonate An example of megabreccia, formed concor- from the platform. The following sequence, dantly on platform top, has been reported Car3, lasting until the Early Tuvalian, saw the by Gianolla et al.[71]. According to Spence and final filling of the remaining intrabasinal space. Tucker[72], megabreccia may form on the plat- During this time, shallow-water siliciclastic- form-top during subaerial emergence due to carbonate sediments of the Dürrenstein Forma- the increase in stress on the sediment as the tion (sensu De Zanche et al.[76]) deposited. The interstitial pore-water drains from the system. lower system boundary is marked by erosion However, this example was set for the unlith- ified sediment, while clasts composing brec- platform, while the upper one represents an cias in Medvedica show marks of complete erosionaland carstification surface separating of the Cassian peritidal Dolomite 2 dolomite lithification of limestone before brecciation. of the uppermost Dürrenstein Formation from An explanation for this may be found in very early lithification of Ladinian – earliest Car- (Car4) sensu De Zanche et al.[76]. nian platform carbonates, largely governed by Withinthe overlying the given clastics time of frame, the Raibl the Formationobserved microbes[47, 50, 73, 74]. The third model for forma- breccia level most likely correlates with the tion of megabreccias may be cliff erosion[75]. upper sequence boundary of the Car1 deposi- This model, however, requires tectonic activity, tional sequence. This interpretation would be which would create steep relief. supported by the overlying CDLF in the same tectonic block. In should be mentioned, how-
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ever, that the changes in relative sea level de- Correlation of the emergence level on top of pend not only on the eustasy, but are also under the CDLF platform in the northern External Do- the influence of local tectonics[77]. Emergence of lomites with the Southern Alps is much more shallow platform may thus also result from the reliable as the Car1 sequence boundary, as it interplay of factors operating on a much more marks the sea-level drop of the second order, narrow area. a regionally much more widespread event[84, 85]. For example, the cessation of platform growth and karstification in Julian is correlatable in the Towards the sequence Northern Calcareous Alps, in the Carpathians stratigraphic framework and also in Serbia[52].
Breccias of similar composition to the one de- scribed in this paper, but located on top of the Concluding remarks CDLF, were described by Dozet and Godec[5], [8], Buser[9], Dozet[11, 23, 79] [78], In the area of Medvedica (central Slovenia, Ex- and Jelen[80]. Like the Medvedica breccia, these ternal Dinarides), a succession of breccia beds consistRamovš of angular, often very large, Pleničar clasts of separated by medium-thick limestone or do- CDLF in reddish matrix, but they differ in lack- lomite and mudstone beds was investigated. ing intermediate autochthonous carbonates Breccia consists of clasts belonging to Cassian and are overlain by fine-grained clastics. They Dolomite and Limestone Formation. Its lower are often described as being positioned above boundary is presumably faulted, while it con- the erosional surface on top of the CDLF and tinues upwards into the Cassian Dolomite and associated with bauxite, so they too represent Limestone Formation. Mudstone beds and emergence horizons (see[23]). Despite the lack weathered bed surfaces point at subaerial of fossil evidence form the breccia matrix itself, exposure. The breccia is thus interpreted as emersion breccia[69, 70], or as dissolution brec- Tuvalian in age[5, 9]. cia accumulated on subaerially exposed sur- Inthey our are opinion, considered this breccia as lowermost on top of Julian 2 the CDLF to face[68]. The emergence of platform top is cor- marks the second and final emergence of the related with the upper sequence boundary of CDLF platform and correlates with the up- the Southern Alps’ Car1 depositional sequence per sequence boundary of the Car2 (the lower of Late Ladinian age[71, 76]. The emergence, how- boundary of the Car3) depositional sequence of ever, could also result from local tectonics[77]. the uppermost Julian. Alternatively, it could be positioned at the lower sequence boundary of the Car4 depositional sequence[71, 76]. In the first Acknowledgements case, the emergence lasted through the entire Car3 sequence, which is thus completely miss- This study was financially supported by the ing, through the lowstand systems tract of the Car4 depositional sequence, and perhaps also P1-0011). The authors are thankful to B. Celarc through part of its transgressive systems tract. (GeologicalSlovenian Research Survey of Agency Slovenia) (program for the revisionnumber This emergence phase is thus sufficiently long of the manuscript, and M. Štumergar (Geologi- to allow for the formation of bauxite (see[13]). cal Survey of Slovenia) for the preparation of Alternatively, considering option of correlation thin sections. with the lower boundary of the Car4 sequence, part of the older sequences may be eroded. However, the latter option does not allow for References a time gap necessary for formation of bauxite, formation of which also requires humid and - warm climate conditions[81], which became es- elec, B., Novak, M. (ur.): Geologija Slovenije [1] Dozet, S., Buser, S. (2009): Trias. V: Pleničar, M., Ogor tablished soon or at the platform demise[82, 83]. . Ljubljana, Geološki zavod Slovenije 2009; str. 161–214.
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