GEOLOGICA BALCANICA, 33. 3-4, Sofia, Decemb. 2003, p. 15-22
Palaeogene sediments (Mechit Formation) near Panagyurishte and Strelcha (Sredna gora Mts.)
Ivan Boyanov, Ivan Zagorchev, Aleksander Goranov
Geological Institute, Bulgarian Academy of Sciences. 1113 Sofia; E-mail [email protected] (submitted: 1. 12. 2203; accepted for publication: 22. 12. 2003)
H6. DOJ/H06, H6. 3azop'le6, AA. ropaH06. - flaAeozeHo- Abstract. The newly-introduced Mechit Formation is a 6ble ocaoo'lHbte nopoobl (Me'lumcKaJ/ cGuma) 6 pauoHe continental (fluvial) sequence of conglomerates and flaHa210puwme u CmpeA'lU (CpeoHozopue). HosoycTa sandstones with occasional clays and coalefied plant de HOBJieHHall Me\fHTCKall CBHTa CJio:>KeHa KOHTHHeHTaJib bris. The pebbles derived from pre-Alpine basement HOH llOCJieJ].OBaTeJibHOCTbiO - pe'IHbiMH KOHrJIOMepa rocks (gneisses, amphibolites, granites, pegmatites) and TaMH H neC\faHHKaMH, MeCTaMH - C rJIHHHCTbiMH npOCJIO Upper Cretaceous (Coniacian - Campanian) sedimen liMH H o6yrneHHbiMH pacTHTeJibHbiMH o6noMKaMH. B tary, volcanic and intrusive rocks and ores. The forma raJi bKax npe.ncTasneHbi nopOJJ.bi .noaJibnHikKoro ocHosa tion is more than 570 m thick. It covers with unconform HHll (rHeHCbl, aM Boyanov, 1., Zagorchev, 1., Goranov, A. 2003. Palaeogene sediments (Mechit Formation) near Panagyurishte and Strelcha (Sredna gora Mts.). - Geologica Bale., 33, 3-4, 15-22. Key words: Palaeocene; Srednogorie zone; palaeogeography. Introduction rocks with the Middle Eocene sediments in the central parts of Stara planina (Balkan) range. The Palaeogene sediments south of the towns Dimittova et al. (,[(HMIHpoaa et al., 1984) clai of Panagyurishte and Strelcha have been first med for the same rocks a Late Cretaceous mentioned as polygenic conglomerate by (Maastrichtian) age. Similar sediments have Bonchev (EoHtieB, 1907). Hristov (XpHCTOB, been found in denudation pockets and nep 1953, 1960) made a thorough mapping (with tunian clastic dykes as a cover over the gneis area exaggeration at the expense of Upper Cre ses and granite of the Sushtinska Sredna gora taceous sandstones) and parallelized these block ("anticlinorium") (qyHeB et al., 1966), 15 and have been considered (together with all crops shown on the geological map 1: I 00 000. other post-Cretaceous sediments in the Pana Most of the sections are not sufficiently ex gyurishte and Strelcha areas) as Priabonian. posed. Therefore, we describe here (Fig. 1) only Recently (A.rra,.ll)Kosa-XpHcl.fesa et a!., 1991 ), the type section (Strelchanska Louda Yana the Palaeogene sediments south of Panagyuri south of Strelcha) situated in the Mechit strip, shte and Strelcha have been referred to the and the reference section situated near the marine Middle Eocene (Lutetian) Staropatitsa spring Rayna Knyaginya north of the village of Formation. Popintsi (situated in the Popintsi strip). The present authors made field revisions and Defining features. Mechit Formation consists palynological analysis aiming at a determina of coarse terrigenous continental sediments: tion of the age and lithology of these sediments conglomerates with smaller amounts of sand within the scope of the projects 503 (National stone and coal-bearing siltstone. The pebble Fund "Scientific Research") and "Geology of composition corresponds to 1) the composi Bulgaria" (Geological Institute of the Bulgar tion of the basement of the Srednogorie zone ian Academy of Sciences). The preliminary re exhibited mostly in the Sredna gora crystalline sults have been already published (Zagorchev block: Precambrian two-mica, biotite and et al., 2001a). The palynological analysis made hornblende gneisses, amphibolite, Palaeozoic by S. Chernyavska and P. Pavlishina hornblende-biotite, biotite and two-mica gran (Zagorchev et al., 2001a; Pavlishina, 2002) has ites, pegmatite and quartz as well as the Late proven a latest Maastrichtian - Danian age. Cretaceous intrusive and dyke rocks and the The present publication aims to summarize the ore related to them; 2) the composition of the whole stratigraphic evidence gathered for to Late Cretaceous Srednogorie zone: Upper enable further palaeogeographic and palaeo Cretaceous andesites, dacites and trachytes, geodynamic interpretations. tuff, sandstone and marl. The rocks of the for The death of our esteemed colleagues and mation build irregular beds. Denudation close friends S. Chernyavska and I. Boyanov pockets and neptunian clastic dykes are also came before the finalization of our studies. present. The Mechit Formation covers with This publication is also a tribute to their me depositional contact all pre-Palaeogene mory. rocks of the Srednogorie zone that crop out in the area. Mechit Formation Lithological composition (new formation: The Mechit Formation is built up mostly of MeqJfTCKa CBHTa) polygenic conglomerates. The dimensions of the pebbles broadly vary: from several millime Name. The Formation is named after the peak ters to tens of centimeters and up to 1.2-1.5 m. Mechit situated south of Strelcha, west of the The pebbles are usually well rounded, and the type section. forming rocks show different degree of weath Historical notes ering. A thin weathering crust is often visible. Hristov (XpHCTOB, 1953) mapped 4 strips of The lithological composition of the pebbles sediments attributed by him to the Palaeogene usually corresponds to the immediate neigh (Middle Eocene). The authors of the geologi boring environment, and namely: 1) Upper cal map on the scale I: 100 000 (MJIHes, Cretaceous volcanic rocks: almost black and KauKoB, 1990) fully accepted the northern massive basalts (with rare phenocrysts), red most (Mechit) strip, and considerably reduced dish and gray well-crystallized latites arid the area of the second (from north to south) dacites, greenish differently crystallized strip entirely rejecting the other two (near the andesites, and (rarely) light-gray rhyodacites villages of Banya and Buta, and the prolonga and dacites; 2) Upper Cretaceous intrusive tion to Popintsi). rocks: subvolcanic to hypabyssal monzonites, During our studies we have visited several quartzdiorites, granodiorites and syenodiori sections of all four strips mapped by Hristov tes; 3) Upper Cretaceous sedimentary rocks (XpHCTOB, 1953). The two southern strips as (marls, sandstones); 4) Palaeozoic granitoids well as most of the third (Popintsi) strip turned (from the Poibrene quartzdiorite pluton, or the to be built by Upper Cretaceous sediments. Smilovene granodiorites and granites) and Thus, the Palaeogene sediments are con pegmatites; 5) rarely and only in some expo firmed, with additional outcrop reduction and sures (but abundant in the denudation pockets some tectonic detailization, within the out- and neptunian clastic dykes NNW of Pana - 16 · . · .. . . - .... . : .. t.. ;,...,....,~tpn gyurishte) biotite and two-mica gneisses and (5) 2.5 m polymictic sanastone w1w • .,v""'"'.... migmatites, and amphibolites. pebbles, and polymictic conglomerate Sandstones are present as separate beds tens (4) 5 m polygenic conglomerate built up of me of centimeters to several meters thick. They are dium-sized to coarse pebbles of a grayish or yellowish colour. The grain di (3) 8-10 m coarse-grained polymictic sand mensions greatly vary, and the sandstones show stone with isolated pebbles all transitions from coarse-grained through me (2) 30 m polygenic conglomerate dium-grained to fine-grained sandstones and (1) thin (2-1 0 em) siltstone to shaly sandstone sandy siltstone. The cement is usually clayey, rich in coal substance sample 9j99 - coal and less frequently a carbonate one. Millimet bearing siltstone ric to centimetric pebbles are often included in - lower contact: tectonized surface striking the abundant sandstone mass. The clay content 160°/40-50°ENE over tectonized andesite. is relatively small. Coalefied plant debris are sometimes abundant, and the rock becomes a Reference section at the spring coal siltstone to sandstone. Rayna Knyaginya north of Popintsi (Plate I) Description of the sections (the section is strongly disturbed by normal Strelchanska Louda Yana - type section faults) The type section of the Mechit Formation is Part I, from bottom to top, from the first out studied along the path at the eastern bank of crops towards the fountain and spring: the Strelchanska Louda Yana River south of (basement: tuffs, marls and sandstone of the the town of Strelcha. Upper Cretaceous) - fault contact with the andesites, tuffs and - unconformable depositional contact marls of the Upper Cretaceous; the fault (l) 30m polygenic conglomerate, pebbles from strikes 120° and dips 60-80° NNE. 0.5 to 50-60 em built up mostly of Upper Cre (20) 45 m polygenic conglomerate built up of taceous volcanic rocks (andesite, dacite, rarely well-rounded pebbles from Cretaceous volca basalt) and intrusive rocks (monzodiorite, gra nic and igneous rocks nodiorite); pebbles derived from weathered ( 19) 12 m polygenic conglomerate with 3 coarse-grained quartz-diorites to plagiogra sandstone interbeds, each 0.6-0.8 m thick nites of the Palaeozoic Poibrene pluton are (18) 60 m polygenic conglomerate also abundant but less frequent ( 17) 2.5 m polymictic sandstone with isolated (2) 25 m thick-bedded yellowish to grayish pebbles and with thin seams of coal-bearing sandstone rich in mica grains, locally - with fine-grained sandstone; bedding 125of70°NNE coalefied plant debris; well exposed in the little sample I 1(99 quarry above the fountain; bedding 90o/25oN ( 16) 300 m polygenic conglomerate with sample M1/2000 interbeds (0.5-0.8 m) of coarse-grained sand sample M2/2000 stone with isolated pebbles (3) 40 m polygenic conglomerate, with the same ( 15) 0.4 m tectonized coal-bearing siltstone, composition, pebbles usually between 5 and bedding 140°f55oNE sample 10/99 20-30 em but reaching up to 120 em, within (14) 20 m polygenic conglomerate, pebble di abundant coarse sandy matrix within the con mensions up to 10-15 em, locally thin glomerate: low-angle normal fault, strike 130° I interbeds of polymictic sandstone 15osw, striae on the slickenside 200°/14 o imme (13) 3 m polymictic sandstone diately south of the highest point of the ridge: ( 12) 15 m polygenic conglomerate, pebbles up normal fault, strike 80-90°f60°S to 30-40 em North of the fault: about 20 m of tuffs, brec ( 11) 1.5 m coarse-grained polymictic sand cia and gray marls (Upper Cretaceous) in a stone narrow horst ( 10) 4 m polygenic conglomerate sample MS/2000: marl (9) 3 m sandstone; in the upper part - angular subparallel normal fault, strike about 95°, pebbles (up to 2 m) from reddish-gray marl steep dip angle; along the continuation of the (8) 50 m polygenic conglomerate section to the north, the whole sequence is in (7) 5 m coarse- to medium-grained sandstone, overturned position (southern dips) in the lower part - coarse breccia of marl an Part 2 gular pebbles (3a) about 5 m polygenic conglomerate (6) about 40 m without outcrops (2a) 15 to 20 m: thick-bedded coarse-grained 3 Geologica Balcanica, 3-4/2003 17 sandstone, bedding 90° /45°S, over fine-grained and hornblende gneisses, as well as Late Cre sandstone with slumping and cross bedding taceous quartzdiorite and granodiorite (in sample M3/2000 - sandstone, about 5 m be cluding such from the chilled margins). Some neath the lower boundary of the conglomerate of the pebbles are impregnated with pyrite and sample M4/2000 - fine-grained sandstone be chalcopyrite, and are similar to the porphyry neath the coarse sandstone copper ored quartzmonzodiorites from the Me (Ja) polygenic conglomerate (without clear det deposit. Pyritized and epidotized quartz outcrops, only scattered pebbles; undeter dioritic and granodioritic porphyries from the mined thickness) basement: sandstone, tuff, Late Cretaceous dyke formation are frequent marl, conglomerate; rare outcrops whereas pebbles from the Palaeozoic horn Thickness. The thickness of the Mechit Forma blende-biotite and two-mica granites are scar tion in the type section is about 570 m. Prob ce. The matrix is scarce, and is usually of a con ably it reaches up to 700-800 m at the traverse tact type. Quartz and feldspar grains are ce of the peak Mechit. mented by a fine-grained sericite-chlorite mass. Hydrothermal alteration and pyritization fol Palaeogene deposits north-west lows late intersecting fractures. Locally the and north of Panagyurishte gneisses are upthrusted on the conglomerate, and along the thrust surfaces both gneiss and The scarce outcrops of Palaeogene sediments conglomerate are hydrothermally altered and north of Panagyurishte have been found first pyritized. during geological mapping on the scale The outcrops north of the Medet porphyry 1:25 000 (lJyHes et al., 1963). They crop out in copper deposit are very small. In one outcrop side the Sredna gora crystalline block in two the conglomerate covers the weathered sur separate localities: Kyoy dere west of the Pana face of two-mica porphyry granite of the Late gyurski koloni resort, and on the road north of Carboniferous Koprivshtitsa pluton. The other this resort and the Medet open mine. It should occurrence is a neptunian clastic dyke striking be mentioned that this publication was the first NW-SE and dipping 60oNE, with a thickness to report the presence of neptunian clastic of 30-50 m and a length of about 5 m. The dykes in Bulgaria. The description hereafter pebbles (1 mm - 20 em, rarely up to 0.75 - 1 follows almost entirely the publication cited as m) are represented by two-mica granite (simi far as both localities have been changed (and lar to the host rock), chloritized gneiss, dioritic most of them disappeared) during the past porphyrite, spessartite, etc. The :1atrix is forty years. scarce in amount, and is composed of quartz, The Palaeogene in the locality Kyoy dere is K feldspar, plagioclase, muscovite, altered bi preserved as small denudation pockets (the otite and sericite. largest one followed on a distance of about 30 m) traced over a distance of nearly 450 m. The Fossil content and age conglomerates cover with depositional contact the eroded surface of weathered hornblende No fossils have been found up to now, and the biotite gneisses, and in one of the outcrops age has been assumed by wider correlations cover also a dyke of dioritic porphyrite (sup and general considerations. The present au posed Late Cretaceous in age). Two clastic thors sampled along the path parallel to the dykes (thickness 10-20 em; strike NW - SE, river Strelchanska Louda Yana the finer-grai dip 70-90osw and 55 -90oNE, respectively) ned sediments (fine-grained sandstone, silt have been traced at _distances of 7- 10 m and at stone, shale) that contain coalefied plant de ca. 1-2 m in depth. The conglomerate consists bris (including one thin bed of coal-bearing of unsorted, different in size (from 135 x 63 em shale). All samples contain abundant plant to 1 mm) semi-rounded to rounded pebbles debris, usually black and structureless. Two of and terrigenous grains. Locally the conglom the samples contain single light-coloured and erate passes into coarse-grained sandstone. transparent plant debris with clear cellular However, the bedding is hardly discernible. structure. The pebbles usually are covered with a thin The following taxa (Table 1) have been deter brownish crust. They are of variable composi mined by S. Chernyavska and P. Pavlishina tion, their provenance being both from the (Zagorchev et al., 2001a) and Pavlishina (2002). Sredna gora crystalline block and from the The conclusions of Pavlishina (2002) about Upper Cretaceous Panagyurishte strip to the the stratigraphic value of these taxa and their south. The pebbles from the immediate sur co-existence in the samples studied (the rounding are most frequent: two-mica, biotite Mechit Formation, respectively) are as follows: 18 Table 1 Fossil content of the samples studied (after P. Pavlishina; from Zagorchev et al., 2001° and Pavlishina, 2002) Taxa M-112000 M-2/2000 M 1112000 7/99 Nudopollis apertus (Pflug) Pflug + + Nudopollis thiergartii (R.Potonie) Pflug + + Oculopollis minoris W.Krutzch + + + Oculopo/lis extensus Weiland & Krieg + Tm dopollis hojrupensis Kedves + + Trudopol/is.arector Pflug + + Semioculopollis croxtoniae Kedves + + lnterporopol/enites fspp + + + Mi/fordia incerta (Th. & Pflug) + Plicapollis silicatus Pflug + + Talassiphora pelagica Eisenack + "The stratigraphic value of the discussed terized by the consistent occurrence of Normapolles species as well as the age assess Nudopollis apertus, Nudopollis thiergartii, Ocu ment of the whole assemblage is based on cali lopollis minoris, Semioculopollis croxtoniae bration of the stratigraphic range of the taxa and Interporopollenites spp. Most of the en within the Normapolles province and espe countered species in it are known from the lat cially in the type Maastrichtian and Danian est Cretaceous to the Middle Paleocene. sections. Although poor, the assemblage con Namely Nudopollis apertus, N. thiergartii, tains good elements for correlation." Oculopollis minoris and 0. extensus range "The palynological assemblage -· is charac- from Maastrichtian to Middle Paleocene, fl:J!' ~ ¥' l ~~~ I- MEDET PLI x -:iCiCI [=:J Neoaene, ~"' Quaternary · Bratiya-\: x .~ ! ' '\.. J f ..1 ') ~ ~~ '\../ ...1 /"'"\ ..1 ~ :..... ' }... _.,..../ "-.\ ,.../ STRI?T..£Hh. _.! \ _,../ '\7 ~~ ...J. PANAGYURISHTE .... I 1\ ~L~ '\._../ \'---1: / \ .'\ / '\. ,..J. :-- --..._/ 'Y7 l\ JT 'I .... ~ -~ 0:: ·' l2~ ~ ~all ~a ...... _ 4 ~ ~ li ~ , ~· ~..... ~ Rlt ®IY ~~ L / / J:1 / I[ rT1 lr u 1/ ' r.r-·1-U•· I Fig. I. Generalized geological map for the location of the Palaeogene sediments in the Panagyurishte and Strelcha areas. After Zagorchev et al. ( 1963; unpublished report and map I :25 000) and H.nHea, KauKoa (1990); with revision 19 PLATE I Field photographs from the reference section Rayna knyaginya l - polymictic conglomerate near the ridge (packet 3); detail from 2 2 - conglomerates with sandstone interbeds; packet 3 near the ridge 3 - sandstones interbedded with conglomerates (packet 2) with samples Ml and M2; spring and fountain Rayna knyaginya · 4 - Maastrichtian epiclastics (bottom right) covered by coarse polymictic conglomerates (denudation pocket) and well bedded conglomerates and sandstones; packet I , basal parts of the section Semioculopollis croxtoniae and Trudopollis these taxa suggests a latest Maastrichtian to hojrupensis are restricted to the Maastrichtian early Paleocene (most probably Danian) age - Danian interval. The concurrent ranges of for the conglomeratic formation. This age as- Palaeocene - Middle Eocene? 28° 0 50 100 km continent.al deposits fluvial system (locally coal-bearing) flysch -...... /. t.:..:o,;o~-.... marine dtposlts Olympos Oysch ptbblt provtnanct (mosdy ttnigenous) (metamorphosed) marine terrigenous and carbonate thrusts deposlt:s dry land nonnal faults and marine carbonate deposits higher dry land --- wrtnch faults Fig. 2. Early Palaeocene palaeogeography in parts of the Balkan Peninsula (without palinspastics). Modified after Zagorchev (1996) 20 Ivan Boyanov, ivan Zagorchev, Aleksander Goranov Palaeogene sediments (Mechit Formation) ..., GB, 33 . 3-4, 2003 sessment is well supported by the presence of Goranov, A. 2001b. First data on a Late Maastrichtian the dinocyst species Thalassiphora pelagica - Danian age of the conglomeratic formation in the sole of the Central-Balkan granite thrust sheet.- C. r. Eisenack in sample M-II/2000. The first oc Acad. Bulg. Sci., 54, 8; 57-60. currence of this characteristic species is very Alla.nJKoaa-XpHC'Ieaa, K., He.nMKoaa, II., U.aHKOB, LJ.. B. well documented in the uppermost Maastri 1991 . 1IHTOCTp3THrpa$j;fll H .nelj>opMaUHH naneore chtian in Denmark (Hansen, I977)." HOBblX OTnOlKeHHH B 3ana,nHOH H Cpe.nHeH '!aCTH Ope.n6anKaHb.ll H CTapa-OnaHHHbl. - Geologica Bal canica, 21 , 6; 49-90. liaKHpoa, A., liau-MowawaHnH, M., 6pelKH.IIHCKH, K., Correlations and conclusions reoprHeB, E., OHpOHKOB, n .• CnaBKOBCKH, H., CTO.II HOB, C., U.aHKOB, U.., j{powescKH, B. 1984. CTPYKTYP The newly-introduced Mechit Formation (up Ha.ll xapaKTepHCTHKa CTaponnaHHHCKoro rpaHHTHoro permost Maastrichtian - Lower Danian) is Ha.naHra MeJK.Lty r. ConoT H c. TblKa (LI.eHTpanhHbJe JianKaHH.Uhl). - TeomeKm., meKmOHOfPU3. U 2eOOU built of coarse sediments correlated through HaM., 17; 3-34. out the three distinct outcrop areas (Fig. I) on JiOH'IeB, f. 1907. 0eTpOrpa$CKH o6HKOnKH B Ji'bnrapHll. - the base of the similar composition (both of C6. 3a Hap. yMom8., ~tayKa u KHU:HCII., 22-23; matrix and pebbles). The age has been deter ,AHMHTposa, E., Ha'!es, H., Cnaaoa, H. 1984. CTpa mined by taxa of the Normapolles group THrpa$Hll Ha ropHaTa Kpe.na a OaHanopcKo. - llaAeoHm .. cmpamuzp. u AumoA., 19; 65-84. (Pavlishina and Cernjavska in Zagorchev et lilnHeB, K., KaUKOB, H. 1990. reonOlKKa KapTa Ha HP al., 200Ia; Pavlishina, 2002). The sediments in 6'bnrapHR M I: 100 000. OaHanopHme. BTC. Kyouy dere are slightly coarser, Jess sorted, Kapanoneaa, 10., KocTa.nHHOB, B., U.aHKOB, u. .. ro'!eB, n. and contain a smaller percentage of pebbles 1974. CTpoeJK Ha OaHanopcKaTa HBHUa H3TO'IHO OT p. from the Late Cretaceous igneous rocks, and TononHHUa. - 1138. reoA. UHCm. , cep. reomeKm .. 23; 231 -301. bigger amount of pebbles from gneisses and XpHcToa, P. 1953. OpHHoc K'bM reonorHRTa Ha o6nacrra amphibolites that crop out in the immediate MeJK.ny peKHTe CTpen'iaHcKa Jly.na j{Ha H 0RC'b'IHHK - surroundings. The formation is correlated with OaHanopcKO. - 1138. reoA. UHCm. GAH, 2; 127-138. the marine conglomeratic formation beneath XpHCTOB, P. 1960. reonorHll Ha paiioHa MeJK.ny peKHTe the Botev vruh thrust sheet (Zagorchev et al., Jly.na j{Ha H TononHHua. - roo. MuHH0-2eOA. UHCm., 6, 1-2; 181-202. 200 I b) dated as uppermost Maastrichtian - llyHeB, .n .. 3arOp'leB, lila., Pyceaa, M. 1963. naneoreH.CKH Danian on the basis of calcareous nannofossils KOHrnoMepaTH OT Cpe.nHoropcKHll aHTHKnHHOpHii. - and foraminifers. The whole setting suggests Cnuc. li'bA2. zeoA. 0-80, 24, 3; 324-327. the formation and evolution of a fluvial system that has drained the low-mountain area of the Srednogorie orogen. The fluvial system formed in an extensional normal-faulting environ Tia.neoreHCKH ce.nHMeHTHH HacnarH ment, and locally could create ponds or boggy (MetJHTCKa CBHTa) rrpH rpa..QOBeTe areas with coal. The drainage was directed fi TiaHanopHme H CTpeJPia (Cpe.nHa ropa) nally towards north and east (Fig. 2) where the waters with the sand and gravel entered the H. EO.RH06, H. 3azopt~e6 , A. ropaH06 shallow parts of the marine basin (now beneath the Botev vruh thrust sheet - Zagorchev et al., (peJIOMe) 200I b) - probably a gulf from the Emine fl ysch trough of the same age. HMe. Me\fJ.fTCKaTa CBHTa e HaHMeH)'BaHa no sp. Me \fHT (IO)I(HO OT rp. CTpenqa, Jana,ll.HO OT THOOBH.II paJpeJ). References OnpeOeA.RU{U 6eAe3u. Me\fHTCKaTa CBHTa ce C'bCTOH OT rpy6H TepHreHHH KOHTHHeHTaJIHH Ce,ll.HMeHTH: Pavlishina, P. 2002. Danian Normapolles from the con KOHfJIOMepaTH, npOCJIOeHH OT O.IICb\fHHUH H (p.R,ll.KO) glomeratic formation near Panagyurishte and Strelcha BbmenocHH anesporrHTH. CbcTaBbT Ha KbCOBeTe B (Sredna Gora Mountains, Bulgaria). - Geologica KOHfJIOMepaTHTe OTfOBap.R Ha 1) CbCTaBa Ha 2I HHTH, Ty 22