Geogr. ,:ù. Dilllmi. QUI//. 25 (20m), 95·//l0, 2 figg.

ADRIAN ClOAcA n & MIl-Il\ELA DINU ("c,,)

PLIOCENE-QUATERNARY EVOLUTION IN THE CONTACT AREA BETWEEN BRASOV DEPRESSION AND THE SURROUNDING MOUNTAINS ()

An5TRAcr: ClOACA t\. & DINU ,\01., Plioccf/e-Q//(/Iel'll(//)' evo/lilio/l iII 1131TOW glacis of the Pcr~ani Mts, extending gulf.likc insidc them in front Ibe CQlIl1u:1 (/I"ca belwcell art/iou Depre.uio1J al/{llbc mr/"Oltlldùlg mOllll· or [hc Vliidcni Passo laills (Romallia). (fT ISSN 0391·9838,2002)' l'he Plioccnc-Qwltcl"ll:lry e\'olurioll of Ihe picdmonts and [he glaeis ga\'e rise to a combination of genctic Iypcs of morphological Contact that Bra~O\' Depression is the brgcst illlr~moullt~inousdeprcssion in the hatl contribllted IO the compartmentmion of Bra~(lv Dcprcssion. The Romanian Carpathians. Its surface·arca of2,004 kn/ rcprescnts 10.8% of best developcd picdlllollts occtlr on thc sOllthern anel sotlth·wesrern mar­ thc Eastern Carpathians and 0.84 % of Romania. Bcing situated in thc in· gin. olHst~nding being Sohodol. Ramov, Bm~ov aml Sacelc. 011 tlle Carpathi~ll nel' Bend of the i\rch, thc Dcpression appcars as a disconti­ northcnl mal"j},in arc TUl'ia, , antl C~mplll Frulllos; on the castcrn nuil)' bctwccn Ih e sOUlhcrn sUl1lmits of the Easlcrn Carpmhians and the lTlargin is Ojdllia and Poian. On Ihe western margin, the Illorphological caste1'll summit's of the Sollt'hcrn Carpathians. lts formalioll is traceable cOlllact is marked by some narrow glaeis: Tohan, Vu1can, Codlea, Criz­ ro l'Ile Cllrp'lchi'lIl gcosync1ine, in (he wilkc of co/Japsc in che Ducian fal· bav, l"riiierus, t\para. Ormenis ancfl\ugustin. lowed b)' sLlbsidellce associated with scdinlCnl.nion.•1 continuous proccss IIp IO rhc Quaternar)' whcn bcustrinc accuLUulation bccmne dominam. KEY \,\1011D5: Morphocvoiulion, Conract arca. Bra~ov Depression. The margins of Ihe Dcprcssioll show several t)'pcs of morphological Romania. contact witb rhe sUlTounding mountains. the rcsulr of a distincti\'{:I)' dif­ ferelll Plim:ene/QlIatcrnar)' evoll1tion. In the soutb, Ihere is thc: Iarge REZUMI\T: ClOACA i\. & DINU M .• Evollf(ù/ flliocel1 - C/{alel'11al'J n al'iei l10nhcrn CScal'plllent of the Pi:um Cmilllui, Bucegi, Postavaru and Piatra d,· conlnct n DepI'esitlllii lJm~·ovullli CI( 1111I11(ii diII j/ll'. (IT ISSN 0391· Mare massifs, sliding down imo thc milder slopcs of the Clii.bucetele In· 9838. 2002). torsurii. Lots of picumoms gradually sliding imo thc plain, flntl ver)' mllch Ce:l tll:li 11l1insa deprcsillne illlra1l10mana din Carpalii ROlllalle~ti, De· fmgrncnted, recall the amplitudc of recent crusra/ mOVCIlIClUS in l'hcse Bnt~o\'ului, placcs wilh rnoumain upliftings by O\'cr +2 I1lrn/year on the one hancl, and prcsillne:l are o supr:lf:tlii de 2 004 km', ceea ce reprezilllli C~rpatilor ~i sLlpmfa~a ~iirii. sinkings of -4mm/year ar thc OlllRaul Negru junction, on the other. 10.80/0 din cca a Oriemali 0,84% din Situaia These COntinllnus lllovcmenlS, devc\oping in apposite dircclion, in Curbum imernii :I arcului carpatic, deprcsiunca aparc ca o aric dc dis· ~i wellt on rhroLlghollt the Upper Pliocenc/Qumcrnary imerval, gcncrating cominuitatc intre cuimile sudice alc Carpatilor Orientali cclc csticc aie Carpa~ilor escarpmellls fCStOOllCd ani)' by 5hon. yct very dccI' val1e)'s, a rnajor Sllp­ Meridionali. Dcprcsillnea s-a (OrlU3t in Aeosindinalul carpatic, prablJ~irea ply source of malerials far rhc picdmolHs cxtcnding m thc base of thc cs­ l'l'in clin dacian continuata cu o sCllfunclare sllbsidclltii inSOlita de sedimentare, puna in cuatcrnal' cand a predomin~t aClllllularea I:tcLlstrii. carprncnt which. in this wa)', acquired 'lppreciable elimcnsions. East­ wards and northwards, at the cOnlact with tbc Bretcll, Nemira, Bodoc Marginile depresiunii Sllnt marCate pl'in mai multe IipUI'i dc conlact amI Bamolt IllOllntains, movcmenrs had !ower amplitucles, whìch ac­ morfologic f.11ii de IIltllllii din jllr. rczultat al unei cvol111ii plioccn. COUI1tS far the cliffcrenl aspecr of the COntact area sioping stepwise to· cuatcrnarc difercniime. Astfc1, in sud, dcprcsiunca estc dominata dc abrupturilc nordice ampie aie munlilor Pictrci CmiLllui, Bllcegi, Postiiva­ warels the depressionary plain. J\lthough tbc s}'slem of pre-Hercinian rul ~i Pimra Mare, continuate cu versan~ii mai domali ai CliibliCete10r In­ horsts ancl grabens has not bcen recenti)' reactivated, )let the northern torsurij. O ntlll~illlC de piemontllri, Iarg cfilate dal' putel'llic fragmcntme, margin aquirecl a sinuous out1ine through Ihe pcnetratioll of depressional cvocii. ampiiludine:l mare a mi~ciirilol' crLlstalc rcccnte dc aici: mi~ciil'i de gulfs. inal~3I"e li munlilor cu valori de pesic + 2 mm/an in COntrast cu mi~cii.ri dc Oll thc western side, thc Per~ani Mis overlie che basemelll horst of sCllfundare ce ating -4 mm/an I:t connuenta Oltuiui cu Haul Negru. Ihe Zarnesti - Hoghiz - Oeland gravimetric axis, a zone of mediulll 111'­ Aceste mi~ciiri cominui ~i dc scns contrar, ce s·au lllcnlinut il) to! imcr­ Iifts (+1.0 - +1.5 mrn/year) adjoining a l"elativd)' balanced deprcssional valuJ Plioccn Supcl'iOr-Cwllernm", aLi 8cncmr abruptllrjJe flceSlOr IllllJl[i, area (O lllm/yearl. So, [he bound:lr)' of [he Dcprcssion is formcd from thc fcstonate doar de vai scunc dar pllternic adiìncite. fn acestc condi~ii, dc au alimentm cu c:ll1titàti imponante ùc lll3tcriale piemonrurile de la b~za abrupturilor, care :lU ciipala{ dimensiuni aprcciabile. Spre esI, ca ~i spre lIonl, la contactul cu mun~ii Bretcului, Nemirci, Botlocului ~i Bamoltului, ("') SpiI"/{ Hm'cl UniuNsily, Facult)' oJ Ceofl.rapby, 1011 Cbica slr., 13, ltli~ciirilc au fl\'ut o amplitudine mai mid, aSlfcl cii ~i aspcctul arici dc recl. 3, Bllcbal"('~-t 5. contact este altul: piemonturi restransc anate in prc!ungin::I culmilor cc ("'''') ROJl(a1/iflJl JlmeriCf111 Vl/iueHil)', Magberu, '-3, Seclor l, lJud)(/· coboar~ treptat sprc ~esul dcpresiunii. fn plus, faliile sistemullli de haI" re.r/, Romallin. sturi ~i gmbene prehercinicc, de~i nu au fast rcaeti\'atc rcccm, aLI impri-

95 m:Jt marginii nordice. un comur sinuos prin patrunderea golfurilor dc­ and 0.84 % of Romania's [erriwry. IL lies in the inner Bend prcsionare. Pc Iatura veslico. ;\'Iuntii Pe~ani se suprapun horstului de of the Carpathian Areh, being surrounded by the southern fundamelll al axului gravimctrie Zarn~ti - Hoghiz - Oeland, o arie dc iniiltare medie (+1.0 +1.5 mm/no) cc se invccineaza cu e parle rclmiv ranges of [he EaSlern Carpmhians ([he Bend Group) ancl of cchilibr:uìi Il depresiunii (Q mml:m). fn aceste condi\ii. limita depresiunii [he Somhern Carpmhians (Fi'igara§-Bucegi massifs). This o formeazli COlll

T8rt~~ Murgu Bodoc ca'P.inis 1193m 1241m v... 1018m Ula ulul ~. CMnet

1. GnIv" lInd dtrt Nndt; 2. loeuoid deporIb; 3..Gr...... MlldlIIIld Ioeuoicf deQotitI.;1 4, Badenlan (Tortonlan) tuffi Bnd mll1a; , 5, Helvetian congfomlfatea. And5\onea : and marll' 6 OIgocen.'1ChIItI and Gèrbova , ut\Òlton..; 993 m 7, Ma~m8lton.,llI1ped cl8)'l Ind MftIea; 8, SchIet~ lIy5ch (curblcorrticll); • ,"'"... ~.~S6~u~'H.L:.J,!.J-"~==~

g, Bucegl conglomerates;

lO, M8f'6.elInd8ton.~;

11. ~ndItone lIyach (8odoc FIyKh);

12, SancIIIone-Imelton. fIysch (SiNie Strlte)

13, Mic:Mc:NIts end peragn";

Flc. 1 - Comact Mea between Bra~O\' Oeprcssion and Per~alli, Baraoh and Bodoc l\·lountains.

96 norchern line a sinuous contour through the penetration of northern volcanic chain» hacl been considerably inolvecl in depressionary gulfs. To the west, the depression is c10sed its fonnation (lancu, 1957). in by thc Pcr§ani Mts, cxtcnding gulf-likc insidc rhcm in UPLlFrING - The Bcnd Moumain spacc had bccn sub­ the Vladeni Pass area. jected lO uplifring movemcnts thar culminated in the Savic The relief features by a re1ativciy concentrical stepwise orogenesis (Oligoeene.Aquitanian), conrinued in the Mio· display with picdmonts, glacis and aUuvial fans at thc con­ cene-Pliocene, with rhythmical uplifts thar engendered rhe tact with the mountain. Thc absolute alritudc varies from lUu $es and Gornovita complex sculptural surfaces. The undcr 500 m in rhe Olt Iloodplain (498 m at thc junction almost synehronous sinkings in the centrai axis produced with the Riìul Negru and 461 m at Augustin), to 850 m in rhe Depression of Bra~ov. Thc map of recenr verrical crus· thc Sohodol Piedmom. ral movemenrs in Romania (Har/a 1Jll$car;ior cms/ate vert;· The dominant aspecr of the Depression is that of a cale din Romania, 1987) providcs a clcar·cut image of local higher cxtcndcd and Ilat plain (ovcr 80% of thc arca), disparities in rhe direc[ion and rate of verrical movements. widely inclined towards the centrai part, more precisely lO· So, no \Vonder thar low and moderate inrensity uplifring wards rhc vallcys of thc Olt and of its triburary thc Riìul arcas (0.0-2.0 ml11/ycar and 2.0-4.0 mm/ycar rcspcctive!y) Negru. It appears as an associarion of several genetic have built rhe mounrainous relief, whilc the subsidence al'· types: plains of accumulation (Auvio·lacusrrine), piedmon· ea of medium and grear inrensiry (0.1·2.0 mm/year and tal fie!ds (520-550 m), rivcr plains, rcrracc plains, subsi­ 2.0A.0 mm/year, respectivc1y) reslllted in the formation of dence and divagation plains. Piedmoms and accumulation thc Oeprcssion. The sct of high massifs (Piatra Craiului glacis occupy rhc highcr ridgcs of thc Oeprcssion (850 m 2,238 111, Buccgi 2,505 m, and Ciuca§ 1,954 m) overlap thc in the Sohodol Piedmom and 550 m at the contacr with area of moderare upiifring intensity (top values of the thc alluvial plain), the comaet arca itse!f being markcd by Bend), while the Per§ani, Baraolr, Bodoc, Nemira, Vran· lines of springs. The best developed piedmonts lie on the cea ancl Clabucere!e Intorsurii Mrs., correspond to the sourhern and south·western edgc, outstanding being the low- intensity area (fig. 2 A). The emergencc, developmenr Sohodoi, Riì§nov, Bra§ov (Timi§J and Silce!e. The pied­ nnd Iasring preservarion of a lake \Vas a hypothcsis acl­ monts of Turia, Dalnic and Campul Frumos oceupy the vanccd by Orghidan, 1929, Mrazec, 1932, Tancu, 1957; northern side. Mihailescu, 1963. Thc formacion of a lacllsrrine cuvette in There is litde depth fragmentarion, comparable \Vith the wake of sinking in the Dacian, later drained towards rhc piain zones (50 to 150 111). The density of fragmema­ thc Transylvanian Depression, would cxplain the upfill of l don (0.5·0.8 km/km ) is the resulr of a host of rivers and Bra§ov Depression with Quatcrnary alluvia (over 800 m brooks flowing down from the mountains towards the thick) brought by the rivers from thc neighbouring mOUll­ io",cr base leve! of thc Olt (530 111 at Sfiìmu Gheorghe, rain regions (Mihaileseu, 1963). 498 m at the junetion with the Raul Negru River, 484 m Late!y, howcver, as ncw scdimentological nnd pali no· downsrream Feldioara, 46l m at Augustin). There are sev· logical evidcnce has kcpt piling up, most geomorpbolo­ eral areas of hydrographic convergence, ego at Lunea gists are inclined lO consider this area as marshland ar the Calnicului, Feldioara·Bod, Targu Secuiesc·Lunca·lmeni. most (Posea, 1981; Mihililil & Popcscu, 1977). Density and depth of fragmenration in the piedmonr zone The mountain summits around Bra~ov Depression are 0.8·0.9 km/knl and 150·200 m, respective1y. were already in piace when the Creraceous deposits, formo ing mainly rhe sourhern and wesrern massifs, srarred being eroded in thc condirions of an arid c1imare. As a matter of THE PLIOCENE-QUATERNARY EVOLUTTON facr, upliftings begun in the Senonian, led lO rhe expan­ OF THE BENO AREA ANO OF BRASOV sion of the weathered areas obvious in the Paleogene. The OEPRESSION Paleogenc erosion rcmovcd much of the mounrain land developed on Aptian-Albian conglomerates, generaring a The Depression emerged wirhin rhe Carpathian geo· host of terrigenous materials. syncline rhrough a sinking begun presumably in rhe Da· Thc modelling of a vast bm'der surface, bcgun in the cian era, follo\Ved by subsidcnce associated \Vith sedimen­ Pliocene on eirhcr side of the Bend Carpathians, wenr on ration, a process rhar lasted up lO the Quaternary. There unti! thc Middlc Plioccnc Rhodanic phasc. Thc subtropi­ are some low aUuvial plain secrors along the Olt Valley cal Meditcrrancan climate of che Pliocene \Vas marked by which stili undcrgo subsidcncc of -2 and -3 mm/ycar extreme periodical fluctuarions, from arid to pluvial, as re· (, Halchiu and Augustin scttlcmcms)_ vcalcd by lithological and sporopollinic analyscs. Thc Thc geological buiJr-up is fairly complex: sedimenrary strong iron-hydroxide pigmemations of the Per§ani mino· deposirs originating from the Creraceous f1ysch (sand· conglomerates are suggesrive of this subrropical c1imare SlOnes, IimeslOne) and volcanic formations (andesites·nor thar weathered continental dcposits. So, picdmom deposi· sectioned in the profiles from fig. 1) overlain by Quater­ tions on the edge of the moumain space indicate nor only nary deposits (sands, gravels and days). The Pliocene de­ the higher inrcnsiry of uplifring movements, bUl also che posirs (\Veakly·bollnd sandsrones, marls, and gravels), oc­ beginning of rhe first subsidence, ending up in the forma­ curring on the orogen rim surrounding the depression, led tion of the first erosion glacis (Cioaca & Dinu, 1996). lO the assumprion the sinking rook piace during the Plio­ TI-lE SEDIMENTtlTtON 01' TI-IlO OEPHESSION - Whilc gcol­ cene and rhat «tectonic and magmatie exrrusions from tbc ogy and geomorphology specialists have agreed in the

97 FIG. 2 - Bril~o\' Dcpprcssiorl. Thc 1b~>i map or rcecm erustal mo\'cmcms (Al; l, Uplirting arcas: 2, slIbsi­ 2§§ denee llre.IS .md Ihc typcs of 3~ morphologieal eOlUae( with (he slIrrounding moulllains (Bl; I. 4~ noocJpbins .md lo,,"cr [crmecs; 2. 6~ (errilccd pbins: 3. ;leclllllUhuions. gbeis: -L IarRe marginai pied­ S~ moms; 5. tcrrneed piecJmollls wilh crosion outliers; 6. narro\\' *=1 marginai picdmonts. slcp-like di­ si, ,I spb)'; 7, duncs; 8. aCIi\'C subsi­ 9lI] denee arcas tgrn\'imclric minima z -2 and --I mm/yead: 9, areas 10~ subjcclcd IO rcccnt posili\'e cm­ 11CZJ slal mo\'cmcOIS (:J\'cmge uplif­ 12~ ling; +1.0 IIp lO +1.5 Illm/ycar. maximal 2.0 mm/\'c'lrl; IO. cro­ sion olldiners: l i. rclicf unils bounds; 12. dcprcssion bOllnds_

course of rime 00 the uendeniable tceronie origio of (he laycrs of Liassic eoal aecumulation ar Codlc

98 memation within the channcl, or in the aftermarh of ex­ acting eluring the Viliafranchian ancl the Pleistocene in the tfeme flood evems with specific effects, has led to the for­ over 2,000 m·high moumains on either side of the teetonie mation of new holms, or tO the reshaping of existing ones. cOlTidor, showed up in the correlative deposits of the In the areas of hydrographic convergence flooding \Vas a piedmonr. Thus, the effect of che [wo seulprurai eycles was fl"equent phenomenon (every one or two-three years) with the fonnation of two piedmonrs in one ancl the samc area: negative impact on the floodplain. As from 1975, a pro­ an older piedmom conraining coarse materials, frequently gram of hydrorechnical works has been iniriated through uplifted ar the com'acr with the mounrain rim, and a which the meanelers of the River Olt have been Cut, cor­ younger piedmonr, stretching as far as Tara Barsei, anel recting its course. These works have resulted in the speeel­ containing finer grain-sized materials, often resulting [rom ing IIp of the river flow, whereas abandoneel creeks have the refashioning of the highcst part of the older pieclmont. been turned imo Icisllrc areas. Works bcing halted (in As a matter of faet, rhis scetol' of Bra~ov Dcprcssioll, 1983), the grollnd waters starred infiltrating imo the cm­ namely Sohodol Piedmom (over 850 m ald, is the highest banked areas. Thc ncw, lowcr base level of the alt, has and most fragmemed onc. The deepening of rhe elrainage brought abollt a frcsh phasc of tributary eleepcning, affect­ ner [har would form later, led lO pieclmollt ourerops of ing secondary dams through sidcways erosion. grea[ granulomcmry, largely in the depression-to-moun· tam contact. The Timi~ Piedmont (belween che Ghimbii~e1 and che TYPES OF GEOMORPHIC CONTACT Timi~ valle)'s) and che Tarlung Piedmont (belween lhe Ti­ BORDEJUNG BRASOV DEPRESSION mi~ anel the T5.r1ung valle)'s) cover a wider area. Besiclc, che rum taken by the T5.r1ung Valley towards rhe area of Thc key to understanding lhe Bra~ov Depression's relief maximum active subsiclence al (he jllnction with the R5.ul was to look imo the Pliocene-Quaternary cnvironmemal Negru, is associateci Wilh a fan-like opening of the T5.r1ung facto l'S, anel moreover to srudy the contact arca between Pieclmollt in the sa me direction. the Depression and the moumains around it, an area of Ali in aH, the geomorphic landseape of extendcd margi· great Illorpho-strllctural diversity. Since the margin of the nal pieelmoms features smooth or slighrly cumbered imer· Depression is largely overlapping the line separaling areas fluves, especially towards their axial parr. It is onl)' in the subjecteel to opposite vcrricalmovemems ~mcl since climat­ Sohodol Piedmom tha[ a hilly landscape, rransirional to rhe ic conditions were anel stili are rarhcr homogeneous, one mountain zonc, is seen on the mm'gin edging the Bran­ wOLlld expec[ thc contact relicf to be fairly mOllorollOllS. Dragoslavele teetonie corridor or the neighbouring massifs. Bue that is nor so, beeause gcomorphic processes are nor GLACIS represenr anorher rype of morphological con· the same cverywherc in this area, the)' reflecting borh the tacr between the moumains and Bra~ov Depression, wide­ variable uplift anel sinking amplitude and the differenr in­ Iy spread out under the massive conglomarate esearpmenrs tcnsit)' of erosion in rclation to rock complex, rclief step of the Pcr~ani, Baraolt, Inrorsurii and Bretcu mounrains and rhe distance berween loeal base levcls and thc sur­ (fig. 2, B, 3). The)' had emerged during che PleislOcene rounding esearpmcnts. These are sufficiem reasons to justi­ either in theRiss-Wurm interglacial period, when they had fy a distincr approach to each situarion, the morpho­ a \Vide eXlcnsion, or in thc coldcl" Pleistocene c1illlate, strucrural eomplexes ancl their forms of manifestation mak­ when solifluxion proeesses were particularly aetive. A spe­ ing the contact area geomorphic landscape hugcly diverse. eial rolc in the process of glacis fonnation was playcd by PIEOMONTS - As a contact area between mOllmain and the shorr torrential vaUeys deve!oped on the rim of the the low neighbouring zone, piedmonrs are typieal of the ll1assifs that used lO upli[t at a slower pace. On the eastern young ancl massive moumain ehains. Ahrough the Bend side of the Per~ani Mts., they penetrate imo the 1l10Lllltain Carpharians are of reeem age, the)' lack massiveness, so space along che Cepei, Nade~, Bozon and Horarul valleys; that the aecumulation contaet surface between mounrain in the Boraolt Mts., along the Malna" Ziilan, Arcu, and anel Depression meets onl)' inciclenrally piedmonr cl'iteria. other valle),s. On lhe northern sicle of rhe Inrorsurii Mts, An extended marginai piecimom, emerged in the Pleis­ the glacises penetrate up the valleys (Dobar1au, Lisnau, tocene, is seen on the southern si de of Bra~ov Deprcssion. Bclcli, Saciova, Boro~neu), ending up in rhe Depression, fts apprcciable dimensions should be undersrood in terms form rogether a narrow hill-like marginai step. of [wo basic facrors: the height of the mountain from (here Recenr and presem-day alluvial fans overlap fUllclional are the taUest massifs arouncl the Ddepression: Piatra pieclmonrs, aUuvial glacis respectively, even rhough pied· Craiului, Bucegi, Post3varu, and Piarra lvlare), and the monts are no longer forming lOday. Because of rhe re!a­ great elensity and expansion of drainage basins which had tive!y c10sed local base leve! on which subsiclence is going sculptured these massifs. Zarne~ti Pieclmonr cleprcssionary on, che alluvial plain alongside the 01, ond [he Raul Negru gulf appears to be a normal extension of rhe Dragoslavele­ valle)'s, the pieclmonr terraces and plains surrouncling Bran tectonic corridor spanning the Iezer and the Piatra them, have imposed upon rhe rivers nowing down from Craiului Mts in the west and the Leota ancl the Bucegi lvIrs the surrouncling mounrain zonc thm is re!ative1y stable or in the east (Cioaca, 1974). The piedmom is as narrow as mildly uplif,ing (0.5 mm/)'ear), a ,endenc)' lo continue the tecronic corridor, having fillccl up the narrow gulf of building some alluvial fans. Bnl§ov Depression imposed by the Per~ani and the Posra­ This type of geoll1orphic contact was eviclencecl at the varu mounrains. The robust morpho-strucrural sys[ems peripher)' or Vliideni gulf in the Per,ani Mts., 011 che west-

99 cm margin of che Baraoic 1\I1rs. between Iara§ and Bradu!, REFERENCES on rhe eaSCem rim of rhe Bodoc Nlts. berween Dalnic and Ca§inu Mic (Cioaca, 1981), ar che foor of che Nemira l'vhs ClOACA i\. (1974) . Depresùmi/e il1lY(1mOlllmll' dl' dl' pl' INdl'tI mpl'ri(){/ri/ il berween and Lomnia and ar the mourhs of rhe Dtimbovi{ei. Terra. \.46·.51. vaUcys emerging [rom rhe Vrancea Mcs. berween Bre!cu ClOACA A. (981) - Cilracferele Imifare ah, relie/ullii MUII{ilor Perf/mi. and Ghelin~a. Baraolt,/Jodoc. BuI. SI. Soc. Rom. Googr.. 6. (LXXVII. 11}·119. ClOAcA i\. & DINU ~'1. (19961 - Modificarea nrl'nldor dl' r/tl" gl'011Iorfn/ogic Ii bidmlogic ca l{ecl a Il/crori/or d" corl'clarl' il fdhil'i Dltlllui iII deprl'­ sùmeil Bralov. Ann. Uni\!. Oraclca. Geogr.. 6. ·H-52. CONCLUSIONS Gl'agra/iII ROllu;l1iei.lJI. (987). Edil. Acad. Romllne. Bucuresli. p. 21!. The largesr of Romania's mrramountainous depres­ Hartn lmIci/rilor cmstale verticale di" Rrmlllnia (19871. hm. Geolìz. Acatl. Rom. sions, bur also rhc besr known geologically and geomor­ IANCU M. (957) C(J/llrihll{ii la sluditll ullilf;li/or geommfologice diII phologically, Bra§ov Dcpression appears like a concentri­ depresiunea infermi il curburii Carpf/{ilor morsa. 5flilllu Gbl'orgbe. cal succcssion of relicf sreps (Geografia Romaniei, voI. III, Torgu 5ecuiesc. BaraolO. Partea I. Probl. dc Goow. EJiL i\cad. 1987). The rransi[ion ftom che alluvia1 plain in che centre Romàne. Bucuresti. 4. 127-165. to rhe surrounding piedmont rerraces aod ficlds is vcry M1I1AILA N. & POPESCU N. (1977)· Iisupra dcfilcului Ollll/Ili de /a Rncor. smoorh, wirhour any rraces in rhe landscapc. On the Q[hcr Terra. -4, 23-29. hand, che passage from rhe smoorh srep of rhe Depression MIHAILESCU V. (1973) - Les grandes divisioll de Ca,/J11I[.es de SI/d-Est. SL Geom. Carpo Baie.. 7. p. 80. ccnrre ro che surrounding mounrains runs rhrough a con­ MK,\ZEC L. (1932) - COllSidémtioll .fIIr l'origi,,,' d,'s til'pr,'.uinnJ i"lt'TIll·.f lacr area of great landscapc diversiry, which rcflcccs rhe des Cmplllbes Roumailll'S. Bui!. Soc. Géol. ROUlll •• I. 38· ... 7. correlation of rhe morphogeneric phases of Pliocene-Qua­ ORGIUD:\N N. 09291 . Observn(1i 11I01foiogicc iII I"{'gillll('a BmfovII/ui . rernary deposirs. The complexiry of rhe contacr arca de­ bazimd \fIi/delli. Tam Bàrsci. I. 83· lO.... pends on che 1irho1ogy of rhe massifs, rhe proximi[y or POSE!\ GR. (1981) - Depresit/11cf/ Brnrovldlli (CIII"IIl"ll'I"i:.nre gl'OlImr!n/o1!,idi). disrance bcrween areas unclergoing opposite venical crus­ I\nalelc Un iv. Bllcurc~li, Gcogr., 30. p. 213. tal movemenrs of differem inrensities, and rhe compan­ POSEA GR. & pOI'ESCU N. (1974) - Relie!u//{ollulllià. Edit. St., Bucu­ memarion of rhe Depression through some spurs penetrat­ re~(i. 99 pp. ing insicie it. (/IIs. recàvcd 15 MIIY 2002; (lCceplcd J I OCfo!Jcl' 20(}2)

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