Matevž NOVAK in Miloš BAVEC: Geološke značilnosti Bleda in okolice / Geological Characteristics of Bled and its Environs V bližnji okolici Radovljice so ohranjeni vsaj štirje loki končnih moren Bohinjskega ledenika. Najstarejši so tisti na skrajnem vzhodnem robu radovljiške kotline tik pod Karavankami (Hraše, Šmidol, Lancovo). Zahodneje ležeče končne morene med Bledom in Radovljico so nastale v času taljenja in umikanja zadnjega, torej najmlajšega pleistocenskega Bohinjskega ledenika. Sled dveh zastojev njegovega umikanja se je lepo ohranila v obliki dveh grebenov čelnih moren pri Dobravci. Na ravnici pred ledenikom je zastajala voda in sčasoma so tu nastala močvirja, deloma še ohranjena na Blatih in Jezercih. Med umikanjem iz Blejskega kota je ledenik zastal vsaj še trikrat, kot dokazujejo grebeni čelnih moren pri Pecovci in nad severovzhodnim obrežjem jezera. Starost njihovega nastanka ni natančno znana, so pa mlajše od 20.000 in starejše od 14.000 let. Ledeniki drobirja, iztrganega iz podlage, niso odlagali le pred svojim čelom. Velik del so odložili pod sabo v obliki obširnih ravnih zasipov, ki jim pravimo talne morene. Talno moreno v večjem obsegu najdemo med Bledom in Savo Dolinko. Med Gorjami in Zasipom jo omejuje eden najlepše ohranjenih lokov končne morene pri nas. Posebnost talne morene je, da je neredko precej drobnozrnata in zbita, zato slabo prepušča vodo. S to lastnostjo je povezan nastanek omenjenih močvirij, predvsem pa nastanek Blejskega jezera. Za nastanek Blejskega jezera je pomembno tudi ali predvsem obdobje umikanja oziroma taljenja Bohinjskega ledenika ob ogrevanju ozračja po zadnjem ledeniškem maksimumu. Ko se je led talil, so vzpetine na južni strani jezera razdelile ledenik na dva dela. Zelo na grobo lahko ocenimo, da se je to dogajalo pred nekaj več kot 15.000 leti. En krak je ustvaril Ribensko, drugi pa Blejsko kotanjo. Slednja je bila očitno dovolj vodotesna, da se je v njej do danes ohranilo jezero. Najverjetneje je takrat kratek čas obstajal še tretji krak ledenika (Rečiški), ki je zahodno od gradu tekel proti severu. Podobno interpretacijo podpira tudi poenostavljeni model, ki je bil izdelan ob pripravljanju animiranega filma o Bohinjskem ledeniku na Blejskem gradu. S klimatskimi nihanji so povezane tudi terase, ki so jih odložile in vrezale reke vzdolž nekdanjih ledeniških dolin. Rečemo jim glaciofluvialne terase. Praviloma so reke ob ohladitvah podnebja nasipavale velike količine proda, ob otoplitvah pa so ga odnašale. Tako nastale terase so dobro vidne med Šobcem in Lescami, sicer pa prodovi in njihovi sprijeti ekvivalenti konglomerati (domačini jim rečejo labore) pokrivajo znaten del blejske pokrajine. Jezero Današnja »kotanja« Blejskega jezera je torej nastala v zadnji ledeniški fazi, v kateri je ledenik izdolbel razmeroma mehke sedimente v podlagi, vsekakor pa sta nastanek in oblika jezera povezana tudi s tektonskimi procesi že pred ledeno dobo in tudi po njej. Po fosilih, pelodu in sledeh vulkanskih tufov, ujetih v jezerski sediment, sklepamo, da je jezero v sedanji obliki staro približno 14.000 let. Nastalo je ob zadnjem umiku Bohinjskega ledenika, nivo vode pa je bil v prvi fazi za kratek čas nekoliko višji od današnjega. Očitno je umikajoči se led vzdolž doline Save Bohinjke določen čas dajal zadostno bočno oporo vodi in sedimentom, da se voda ni izlivala skozi sedanji iztok pri Mlinem, pač pa mimo Želeč po danes suhi strugi Dindola. Najnižja višina pretoka je tam pri 497 m n.v., torej je bil vodni nivo takrat za 21 m višji kot danes. Matevž NOVAK in Miloš BAVEC: Geološke značilnosti Bleda in okolice / Geological Characteristics of Bled and its Environs v konglomerat. Z oddaljevanjem od kopnega je bil sediment vedno drobnejši. Na muljastem dnu obrežnega pasu so živeli brahiopodi, trilobiti, morske lilije, mahovnjaki, polži, školjke in foraminifere, ki so se ohranili v apnencih. V nekoliko globlji vodi so nastajali manjši krpasti grebeni z algami, mahovnjaki in koralami. Najštevilčnejši fosilni ostanki tega bujnega življenja so se ohranili v glinavcih, meljevcih in apnencih v okolici Javorniškega Rovta nad Jesenicami in v Dovžanovi soteski pri Tržiču. Ob koncu starejšega perma, pred 270 milijoni let, so se gore spet dvigale. Na plimske ravnice ob vznožju gora se je sipalo raznovrstno kamenje in se sprijelo v trbiško brečo. Umikanje morja se je nadaljevalo in v vročem puščavskem podnebju so reke le tu in tam napolnile struge. Kadar je bilo vode dovolj, so se odlagali prod, pesek, melj in glina, iz katerih so nastale pisane grodenske kamnine. Prav iz obdobja, ko so se na območju Južnih Alp povsod odlagali samo ti vijoličnordeči kopenski sedimenti, je ohranjena morda največja geološka posebnost blejskega konca. Samo na Straži pri Bledu in nad Bohinjsko Belo najdemo t.i. neoschwagerinske apnence, ki pričajo o tedanjem morskem zalivu z majhnimi krpastimi grebeni ter kroglastimi neoschwagerinskimi foraminiferami, brahiopodi, morskim ježki in nenavadnimi polži, ki so živeli na karbonatnem mulju okrog njih. Morje je proti koncu perma znova začelo zalivati ta del sveta. Na slanih plimskih ravnicah, sabkah, je nastajal dolomit. Na meji med permom in triasom, pred 250 milijoni let, je življenje na Zemlji doletelo največje množično izumiranje v geološki zgodovini. Med mnogimi živimi bitji so boj za preživetje za vedno izgubili tudi gospodarji paleozojskih morij, trilobiti. Na obsežni karbonatni plošči so v zgodnjem triasu nastajale raznovrstne kamnine, ki jih najdemo po celotnih Karavankah, v Julijcih pa le v manjšem obsegu. Na enotni karbonatni plošči so v začetku srednjega triasa, v aniziju, nastajali samo sivi dolomiti in apnenci z redkimi algami in foraminiferami, ki gradijo ostenja Grajskega hriba in Blejski otok. Temu obdobju so sledili dogodki, povezani s tektonskimi premiki, ki so močno spremenili tedanje okolje. Kontinentalna skorja se je začela razpirati in obsežna karbonatna platforma je začela razpadati. Ob globokih prelomih so se veliki bloki ozemlja pogrezali v globlje morje. Tam so nastajale tanke plasti črnih apnencev s plastmi in lečami roženca. Tektonsko aktivnost je spremljal močan vulkanizem. Eksplozivni vulkani so izbruhali velike količine pepela, ki se je sčasoma sprijel v tufe. Predornine so prihajale na površje tudi v podmorskih vulkanih in ob globokih prelomih. Najbolj slikovit zapis tega obdobja je ohranjen v zelenkastih in rdečkastih vulkanskih kamninah širše okolice Kamne Gorice, ponekod na Jelovici in na Pokljuki, v Bohinju in v Karavankah. V poznem triasu je plitvomorska Julijska karbonatna plošča pokrivala velik del Gorenjske, južno predgorje Julijskih Alp pa je bilo pogreznjeno za več sto metrov v morske globine, kjer so v tektonskem jarku, imenovanem Slovenski bazen, nastajali temni apnenci in dolomiti z roženci. Plimski pas na karbonatnem šelfu so prekrile prevleke modrozelenih cepljivk, ki so v kamninah ohranjeni kot stromatoliti. V podplimskem pasu so živele velike školjke, megalodontide. Najvišji deli platforme so občasno pogledali iz vode in zakrasevali. O življenju v tedanjem morju priča okostje ribe iz ostenja Triglava. V zelo podobnem okolju je živel tudi nekoliko starejši amonit, ohranjen v kamniti mizi iz rdečkastega hotaveljskega apnenca na blejskem grajskem dvorišču. V zgornjem triasu je na Julijski karbonatni plošči nastalo kar do 1200 metrov dachsteinskega apnenca in glavnega dolomita, katerih skladovnice gradijo večino gorskih vrhov Julijcev, Karavank in Kamniško-Savinjskih Alp. Zaradi počasnejšega izločanja karbonata v globokem morju se je v Slovenskem bazenu v približno enakem času odložilo samo do 350 metrov temnosivega baškega dolomita z gomolji ali lečami roženca. Najdemo ga v pasu od Kobarida do Kranja. SCOPOLIA Suppl. 6 - 2013 Plitva podmorska plošča se je na začetku jure počasi potapljala in v vse globljem morju so plavali različni glavonožci, predniki sip in lignjev. Hišice amonitov so se ohranile v rdečih gomoljastih apnencih tipa ammonitico rosso na pobočju Begunjščice v Karavankah in v Dolini Triglavskih jezer v Julijskih Alpah. Morsko dno so poseljevali različni brahiopodi, polži, školjke in morske lilije. V začetku krede, približno pred 140 milijoni let, so se začeli tektonski procesi, ki so pripeljali do nastanka Alp. Ozemlje se je počasi dvignilo in bilo kakšnih 40 milijonov let kopno. Šele v oligocenu, pred približno 30 milijoni let, je del Gorenjske od zahoda še zadnjič preplavilo morje in se razširilo v osrednjo Slovenijo, kjer se je odlagala morska glina ali sivica. Tektonsko dogajanje je spremljal močan vulkanizem. Značilna vulkanska kamnina iz tega obdobja je zelen andezitni tuf. Po kraju, kjer so ga v kamnolomu lomili, ga imenujemo peračiški tuf. Kljub vulkanizmu je življenje v oligocenskem morju cvetelo. O tem pričajo številne korale, polži in školjke, ki jih najdemo na Poljšici pri Podnartu. V miocenu se je morje za vedno umaknilo iz teh krajev. Na kopnem so se začeli površinski geološki procesi. Posebno močan vpliv na oblikovanje površja je imelo dogajanje v kvartarju, občasno polarno hladnem obdobju v zadnjih dveh in pol milijonih let. V ledeni dobi, končala se je šele pred dobrimi deset tisoč leti, so Alpe od severa občasno pokrili ledeniki. Led je prekril tudi gorati del Gorenjske in v obliki dolinskih ledenikov vzdolž alpskih dolin segal tudi v predgorje. Iz manjših stranskih dolinskih in pobočnih ledenikov se je zbiral v Bohinjskem, Dolinskem in Radovinskem ledeniku. Ob drsenju je brusil površje in oblikoval značilne ledeniške doline v obliki črke U. Tudi ledena doba ni bila ves čas ledena. V dveh milijonih in pol letih so se izmenjevala bolj in manj hladna obdobja, občasno je bilo podnebje celo zelo podobno današnjemu. V zadnjem zelo hladnem obdobju pred približno 20.000 leti sta vzdolž današnjih Save Bohinjke in Dolinke ledeniška jezika segala do širše okolice Radovljice, medtem ko je Radovinski segal nekako do Gorij oziroma do vhoda v Blejski Vintgar. Tam sta se Radovinski in Bohinjski ledenik v nekem obdobju celo stikala. Ker sta vsak s svoje strani narinila velike količine kamninskega drobirja, je na njunem stiku nastal greben, imenovan morena, ki ločuje velika naravna amfiteatra. Bohinjski ledenik je bil največji ledenik na ozemlju Slovenije. Ob zadnjem poledenitvenem višku pred približno 20.000 leti je najverjetneje presegel debelino 900 m, zato mu je postala dolina Save Bohinjke pretesna in je prekril tudi del Pokljuke. Segal je do loka med Zasipom, Lescami, Radovljico in Selcami. V bližnji okolici Radovljice so ohranjeni vsaj štirje loki končnih moren Bohinjskega ledenika. Najstarejši so na vzhodnem robu radovljiške kotline (Hraše, Šmidol, Lancovo). Tisti med Bledom in Radovljico so nastali v času taljenja zadnjega, torej najmlajšega pleistocenskega Bohinjskega ledenika. Sled dveh zastojev njegovega umikanja se je lepo ohranila v obliki dveh grebenov čelnih moren pri Dobravci. Med umikanjem iz Blejskega kota je ledenik zastal vsaj še trikrat, kot dokazujejo grebeni čelnih moren pri Pecovci in nad severovzhodnim obrežjem jezera. Starost njihovega nastanka ni natančno znana, so pa mlajše od 20.000 in starejše od 14.000 let. Velik del drobirja, iztrganega iz podlage, so ledeniki odložili tudi pod sabo v obliki obširnih ravnih zasipov, talnih moren. V večjem obsegu jo najdemo med Bledom in Savo Dolinko. Med Gorjami in Zasipom jo omejuje eden najlepših lokov končne morene pri nas. Posebnost talne morene je, da je precej drobnozrnata, zato slabo prepušča vodo. S to lastnostjo je povezan tako nastanek močvirij, predvsem pa Blejskega jezera. Za nastanek Blejskega jezera je pomembno tudi obdobje umikanja oziroma taljenja Bohinjskega ledenika ob ogrevanju ozračja po zadnjem ledeniškem maksimumu. Ko se je led talil, so vzpetine na južni strani jezera razdelile ledenik na dva dela. En krak je ustvaril Matevž NOVAK in Miloš BAVEC: Geološke značilnosti Bleda in okolice / Geological Characteristics of Bled and its Environs Ribensko, drugi pa Blejsko kotanjo. Slednja je bila očitno dovolj vodotesna, da se je v njej do danes ohranilo jezero. Današnja "kotanja" Blejskega jezera je nastala v zadnji ledeniški fazi, v kateri je ledenik izdolbel razmeroma mehke sedimente v podlagi, vsekakor pa sta nastanek in oblika jezera povezana tudi s tektonskimi procesi že pred ledeno dobo in tudi po njej. Sklepamo, da je jezero v sedanji obliki staro približno 14.000 let. V prevladujoče karbonatnem sedimentu v osrednjem delu jezera močno prevladuje detritična komponenta, ki jo pritoki prineso v jezero v obliki majhnih okruškov starejših kamnin, v nekaterih plitvih delih jezera, na primer v Zaki, pa nastaja prava avtigena jezerska kreda, nastala s kemijskim ali biološkim izločanjem iz nasičene vode. Sediment je bogat z organsko snovjo, žal pa je zaradi lokalnih dotokov tudi nekoliko onesnažen. S klimatskimi nihanji so povezane tudi glaciofluvialne terase, ki so jih odložile in vrezale reke vzdolž nekdanjih ledeniških dolin. Praviloma so reke ob ohladitvah podnebja nasipavale velike količine proda, ob otoplitvah pa so ga odnašale. Tako nastale terase so dobro vidne med Šobcem in Lescami, sicer pa prodovi in konglomerati pokrivajo znaten del blejske pokrajine. Summary A view from Bled Castle over the hilly Gorenjska reveals that the region is composed mostly of light carbonate rocks - limestones and dolomites. The sediments from which these rocks were formed had been deposited in warm marine environments on shallow continental shelves. Life was particularly diverse on reefs, in lagoons and on shallow coasts. The geological historical record from the widest environs of Bled, however, also bears witness to deep seas, deserts, volcanoes and great tectonic shifts. The oldest rocks in the Gorenjska region date back to the beginning of Devon some 400 million years ago. In those times, reefs with corals, sponges and other reef organisms began to grow in the tropical belt's shallow sea. Lagoons behind the reefs were lined with meadows of sea lilies, while deep waters in front of the reefs were teaming with trilobites, orthoceras and fish. The region peeked out of the sea for the first time in the Carboniferous period some 300 million years ago, when varistic mountain chain was formed. In the vast deltas, the deposited quartz pebbles cemented together into conglomerate rock. With increasing distance from the mainland, the sediment was becoming increasingly finer. The silty bottom of the coastal belt was inhabited by brachiopods, trilobites, sea lilies, bryozoans, gastropods, seashells and Foraminifera, al of which have been preserved in limestones. In somewhat deeper waters, smallish lobed reefs with algae, bryozoans and corals began to form. The most numerous fossil remains of this lush life have survived in claystones, siltstones and limestones in the vicinity of Javorniški Rovt above Jesenice and in Dovžan Gorge near Tržič. At the end of the Early Permian about 270 million years ago, the mountains began to rise again. All kinds of stones piled up on tidal flats at the feet of the mountains and gradually cemented together into Tarvis breccia. Retreating of the sea continued and in the hot desert climate the riverbeds were filled with water only occasionally. When water was plentiful, gravel, sand, silt and clay were deposited, from which colourful Groden rocks were formed. Perhaps the greatest geological peculiarity of Bled and its environs has been preserved from the very period when only these violet-red land sediments were deposited all over the Southern Alps. Only at Straža near Bled and above Bohinjska Bela, the so-called neoschwageri­ne limestones can be found, which bear witness to the former marine bay with small lobed reefs and spherical neoschwagerine Foraminifera, brachiopods, sea urchins and unusual gastropods that lived on carbonate silt around them. 27 SCOPOLIA Suppl. 6 - 2013 Towards the end of the Permian, the sea began to inundate this part of the world once more. On salty tidal flats, dolomite began to form. At the turn of the Permian to the Triassic Periods some 250 million years ago, the Earth was hit by the most radical mass extinctions in the geological history. Amongst many living beings, the fight for survival was lost for good by the masters of Paleozoic seas, the trilobites. On the vast Early Triassic carbonate plate, very diverse rocks were formed, which can be found all over the Karavanke Mts as well as in the Julian Alps, although to a much smaller extent. At the beginning of the Middle Triassic, in the Anisian, only grey dolomites and limestones with rare algae and Foraminifera, of which the rockwalls of Grajski hrib (Castle Hill) and Bled Islet are composed, were formed on the uniform carbonate plate. This period was followed by the events associated with tectonic shifts that immensely changed the environment of that time. The continental crust began to open up, and the vast carbonate platform started to fall apart. Along deep faults, huge blocks of land began to sink into the deeper sea. This is where thin layers of black limestones with layers and lenses of chert were formed. The tectonic activities were accompanied by mighty volcanism. The explosive volcanoes spewed great quantities of ash, which agglutinated into tuff. Volcanic rocks reached the surface also from underwater volcanoes and along deep faults. The most picturesque record from this period has been preserved in greenish and reddish volcanic rocks in the vicinity of Kamna Gorica, in some places on Jelovica and on Pokljuka, at Bohinj and in the Karavanke Mts. In the Late Triassic, the shallow-sea Julian carbonate plate covered the greater part of Gorenjska, whereas the southern fore-mountains of the Julian Alps were sunk several hundred metres in the depths of the sea, where dark limestones and dolomites with cherts were formed in the rift valley known as the Slovenian Basin. The tidal belt on the carbonate shelf was covered by mats of cyanobacteria, which have been preserved as stromatoliths in rocks. The subtidal belt was inhabited by megalodontits, the giant seashells. The highest platform parts peeked out of the water occasionally and were gradually karstified. About the life in the sea of that time speaks the skeleton of a fish found in Mt Triglav rockwall. A very similar environment was also home to the somewhat older ammonite preserved in a stone table made of red Hotavlje limestone, standing in the courtyard of Bled Castle. In the Early Triassic, no less than 1,200 metres of Dachstein limestone and major dolomite, the stacks of which compose the greater part of mountain peaks of the Julian Alps, Karavanke Mts and Kamnisko-Savinjske Alps, were formed on the Julian carbonate plate. Owing to the slow carbonate secretion in the deep sea, only up to 350 metres of dark grey Baca dolomite with tubers or chert lenses were deposited at approximately the same time in the Slovenian Basin. It can be seen in the belt stretching from Kobarid to Kranj. In the Early Jurassic, the shallow underwater sank gradually, and the increasingly deep sea became home to various cephalopods, the ancestors of squid and cuttlefish. Ammonite shells have been preserved in red nodular limestones of the ammonitico rosso type on the slope of Begunjscica in the Karavanke Mts and in the Valley of Triglav Lakes in the Julian Alps. The sea floor was inhabited by different brachiopods, gastropods, seashells and sea lilies. In the beginning of the Cretaceous Period some 140 million years ago, tectonic shifts began to take place, which eventually led to the origin of the Alps. The territory rose gradually and remained a land for some 40 million years. It was as late as in the Oligocene, approximately 30 million years ago, that part of the Gorenjska region was inundated by the sea for the last time from the west. The sea and spread into central Slovenia, where marine clay was deposited. Tectonic activities were accompanied by powerful volcanism. One of the characteristic volcanic rock from this era is the green andesite tuff. After the place of the quarry in which it used to be excavated, it is called the Peracica tuff. In spite of the powerful volcanism, life in the Oligocene Matevž NOVAK in Miloš BAVEC: Geološke značilnosti Bleda in okolice / Geological Characteristics of Bled and its Environs sea was flourishing, as witnessed by the numerous corals, gastropods and seashells found at Poljscica near Podnart. In Miocene, the sea retreated from this part of the world for good. On land, surface geological processes began to take place. A particularly strong impact on surface formation was exerted by the events in the Quaternary, the occasionally polar-cold period in the last two million and a half years. In the Ice Age, which ended only a good ten thousand years ago, the Alps were now and then covered by glaciers from the north. The ice encased the hilly part of Gorenjska and reached, in the form of valley glaciers along the Alpine valleys, the fore-mountains as well. From smaller side valley and slope glaciers it piled up in the Bohinj, Dolinski and Radovinski glaciers. While sliding, it was grinding the surface and forming the characteristic glacial U-shaped valleys. The Ice Age was not permanently icy either. In the two million and a half years, more and less cold periods exchanged, and at times the climate was even very reminiscent of the climate we have today. In the last very cold period some 20,000 years ago, the glacier tongues along the modern-day Sava Bohinjka and Sava Dolinka Rivers reached the wider environs of Radovljica, while the Radovinski tongue reached the area of Gorje or the entrance to Blejski Vintgar (Bled Gorge), where the Radovinski and Bohinj glaciers were even in direct contact in a certain period. As they both folded huge quantities of rock debris from their own sides, a moraine was formed at their contact, which separates the great natural amphitheatres. The Bohinj glacier was the largest glacier in Slovenian territory. During the last glaciation peak about 20,000 years ago, it most probably exceeded the thickness of 900 metres, which is the reason why the Sava Bohinjka Valley became too tight for it. Thus it covered part of Pokljuka as well, reaching the arc between Zasip, Lesce, Radovljica and Selce. In the vicinity of Radovljica, at least four arcs of terminal moraines of the Bohinj glacier have been preserved. The oldest are located on the eastern edge of the Radovljica Basin (Hrase, Smidol, Lancovo). Those between Bled and Radovljica were formed during the melting of the last, i.e. the youngest Pleistocene Bohinj glacier, with traces of its retreat well preserved in the form of two ridges of the frontal moraines near Dobravca. During its retreat from Bled Corner, the glacier came to a standstill at least three times, as evidenced by the ridges of frontal moraines near Pecovca and above the northeastern shore of the lake. The precise age of their origin is not known, but they are certainly younger than 20,000 years and older than 14,000 years. The greater part of the debris torn from the substrate was deposited by the glaciers also beneath them in the form of vast ground moraines, to a larger extent between Bled and the Sava Dolinka River. Between Gorje and Zasip, it is bound by one of the most attractive terminal moraine arcs in our country. A special feature of the ground moraine lies in its fine granular structure and therefore in its low water permeability. Closely associated with this property is the origin of marshes and, above all, of Lake Bled. Significant for the origin of Lake Bled is also the period of retreat (melting) of the Bohinj glacier owing to the atmospheric warming after the last glacial maximum. During its melting, the slopes on the south side of the lake divided the glacier into two parts, with one arm creating the Ribno basin, the other the Bled basin. The latter was clearly sufficiently watertight for the lake to be preserved in it till this very day. The modern-day »basin« of Lake Bled was formed in the last glacial period, when the glacier chiselled out the relatively soft sediments in the substratum. In any case, however, the origin and shape of the lake is closely associated with tectonic processes even prior to the Ice Age and after it as well. It is believed that in its present form the lake is some 14,000 years old. In the prevailing carbonate sediment in the central part of the lake, the detritic component greatly predominates. It is brought to the lake by its tributaries in the shape of older rocks' SCOPOLIA Suppl. 6 - 2013 fragments, while in some shallow parts of the lake, for example at Zaka, a true authigenic lake chalk is formed, originating through chemical and biological excretion from the saturated water. The sediment is rich with organic matter but is, unfortunately, somewhat polluted owing to the local inflows. Closely associated with climatic oscillations are also the glaciofluvial terraces, deposited and incised by rivers along the former glacial valleys. During climate cooling, the rivers brought, as a rule, huge quantities of gravel, and washed it away during the climate warming. The terraces formed in this way are well visible between Šobec and Lesce, with gravel and conglomerates otherwise covering a significant part of the Bled landscape. Literaturni viri: ANDRIČ, M., J. MASSÄFERRO, U. EICHER, B. AMMANN, M. C. LEUENBERGER, A. MARTINČIČ, E. MARINOVA & A. BRANCELJ, 2009: A multi-proxy Late-glacial palaeoenvironmental record from Lake Bled, Slovenia. Hydrobiologia 631: 121-141. BAVEC, M., 2006: Razsežnost in dinamika Bohinjskega ledenika v poznem Pleistocenu = The extent and the dynamics of the Late Pleistocene Bohinj glacier. V: B. REŽU N (ur.) 2. slovenski geološki kongres, Idrija, 26.-28. september 2006. Zbornik povzetkov, Idrija: Rudnik živega srebra v zapiranju: 35-36. BAVEC, M., M. 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