DOLOMITES - Annexes 2-8 - Provincia di Udine

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NOMINATION OF THE DOLOMITES FOR INSCRIPTION ON THE WORLD NATURAL HERITAGE LIST UNESCO 36 The Recoaro Limestone transitionally passes through lateral heteropy to the Upper Serla Formation, which represents the second unit of the rimmed carbonate platform of the Anisian. This is formed of dolomites, light colored dolomitic limestones in meter-thick banks that appear sometimes amalgamated. There may be banks of light, crystalline dolomites with concentrated areas of Diploporeae and other bioclasts. Locally cavities appear with cements, sometimes with geopetal structures. Encrusting organism boundstones are often found along with calcareous chaetetid sponges bioconstructions and rare corals. A detailed analysis of the bioconstructors and of the microfacies of this carbonate platform is provided by Bechstadt & Brandner (1970) and Senowbari-Daryan et alii (1993), as well as by Blendinger (1983) and Fois & Gaetani (1984). The depositional environment can be referred to as a low-relief (biostrome) carbonate platform, characterized by a prevalently calcarenitic margin, locally stabilized by encrusting organisms (cyanobacteria, foraminifers, sponges) and with infrequent microbialite mounds and skeletal metazoan patch-reefs. In more internal and less articulate areas, or less controlled by differential subsidence, this interval is documented by thick succession of dolomitic limestones and dolomites organized into subtidal and/or peritidal cycles (Valsugana Dolostone, or Dosso dei Morti Limestone in Giudicarie). The landscape changed to either a peritidal or biostrome carbonate platform, which also had deep lagoons and basins. This change was the result of sea level trangression where synsedimentary tectonic events in some areas led to a new, important erosive phase preserved by the “Badioto-Gardenese Ridge” by Bosellini (1968). Erosion affected the rocks of both the Werfen Formation and the underlying Bellerophon Formation. Fragments of the latter flowed down small streams and were distributed as reddish pebbles along small and thin beaches now forming the Richthofen Conglomerate (Tretto Conglomerate in the Piccole Dolomiti or Val Perse Conglomerate in the Dolomiti di Brenta). These terrigenous units are mostly represented by (i) polygenic conglomerates, with clasts that derive from the underlying units, mainly from the Werfen Formation and the Lower Serla Dolomite; (ii) microconglomerates and lithic sandstones, with high carbonate contents, from coarse to medium-fine, in general brick red; (iii) red and gray siltites; and at the top; (iv) gray, highly arenaceous-siltitic marlstones and limestones. The conglomerates form lenticular bodies with a maximum thickness of a few dozen meters that extend laterally for a few hundred meters and can be interpreted as fills of incised valleys (the most famous are the ones below the Catinaccio/Rosengarten or the Odle/Geisler). More often, the conglomerates form prisms only a few meters thick, which extend laterally from a few hundred meters to a few kilometers, with mildly erosive planar bases. Towards the top the conglomerates turn into sandstones and red and gray siltites, that transition gradually into limestones more or less rich in terrigenous components from the Morbiac Limestone. With regard to the depositional environment, based on the depositional geometries and structures, and the morphometric studies of the clasts (Dal Cin, 1967), these units, of which the Richthofen Conglomerate is the most important, are interpreted as continental deposits, settled by moderately long rivers with torrential characteristics, in a semi-arid climate context. The continental character is highlighted by the presence of important trace fossils tied to the passage of terrestrial reptiles such as Rhynchosauroides tirolicus, Chirotherium sp. and Brachychirotherium sp. that are sometimes superbly preserved. Towards the top, the sea-marginal influence is documented (sets of fine sandstones and flaser- and wavy-bedded siltites, which evidence a tidal influence; wave ripples; marine ichnofossils). The fining-up evolution of these formations reflects the general transgressive trend of the late-Anisian succession, that continues in the superjacent Morbiac Limestone. In the basin areas, this erosive event is documented by an increase in the terrigenous component (siliciclastic turbidities) at the summit of the Dont Formation. Evidence of the new transgressive phase is the deposition of the Bivera Formation. The most diffused lithofacies in this unit is repre-
NOMINATION OF THE DOLOMITES FOR INSCRIPTION ON THE WORLD NATURAL HERITAGE LIST UNESCO 37 sented by nodular limestones that are more or less marly, which alternate red, green and gray siltiticargillaceous marlstones, in strata 1-10 cm thick. These nodular limestones are made of bioturbated mudstones and mudstone/wackestones with peloids, fossiliferous sediments with radiolarians, thinshelled bivalves (pelagic), foraminifers, ostracoids, and articles of crinoids. Fine strata of gray-green tufites (cinerites and crystal-tuffs) are spread all over the unit. The thick sediments (1-5 cm) reveal the initial acidic and explosive phases of volcanism which characterize the succession of the Anisian- Ladinian. In the upper part coarsening-upward/fining-upward sequences of dark gray packstones a few meters thick may be present. There are locations of sediment which consist condensed and hardground surfaces that are a few centimeters thick and are very rich in ammonites. The Monte Bivera Formation can be present at the top of the Upper Serla Formation and is an indicator of the drowning platform. The depositional environment sustained a pelagic lifestyle at variable depths. The deposition in the starved or current-swept deeper basins is documented by the most condensed sections or by sections reduced to hard ground. Based on the content in ammonoids (Paraceratites trinodosus, P. elegans, Flexoptychites spp., Bulogites sp., Proarcestes sp., Ptychites sp.) and conodonts (Gladigondolella tethydis, Gondolella cornuta,G. constricta), it is possible to attribute the unit to the Lower Illyrian. latter most Anisian platforms and basins As mentioned previously, the partial uplifting of the seafloor that generated the islands was followed by a new deepening involving various portions of the seafloor due as a result of differential subsidence rates. In a few areas in fact, subsidence was not so extreme which allowed shallow seas to remain (Morbiac and Contrin Limestone). In other areas subsidence was greater, creating deep-sea basins (Ambata Formation). Some areas were initially within the shallow photic zone, which is indicated by their shallow-water carbonate sediments, but were later subject to intense synsedimentary tectonics that increased the water depth, creating an anoxic basin filled by chaotic deposits and breccias (Moena Formation). Cronostratigraphic and sequential scheme of the Anisian units of the Central-eastern Dolomites, compared to the succession of Braies/Prags Dolomites (Piz da Peres)
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ANNEX 3 A3.1 LETTERS OF SUPPORT
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Systems: 1. Pelmo - Nuvolau 2. Marm
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visitors NOMINATION OF THE DOLOMITE
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others (malghe, alberghi, ristorant
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mountain cabins others (malghe, alb
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visitors footpath NOMINATION OF THE
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ANNEX 5 A5.1 PROTECTIVE DESIGNATION
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11. NOMINATION OF THE DOLOMITES FOR
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49. 50. 51. NOMINATION OF THE DOLOM
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ANNEX 7 A7.1 DVD (PHOTOGRAPHS) A7.2
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fauna NOMINATION OF THE DOLOMITES F
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ANNEX 8 A8.1 OTHER LOCAL AUTHORITIE
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DOLOMITES - Annexes 2-8 - Provincia di Udine

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