CASE REPORT

Geomorphodiversity of the San Lucano Valley(Belluno Dolomites, Italy): a Well-Preserved Heritage

Bruno Testa & Barbara Aldighieri & Alberto Bertini &Wolfgang Blendinger & Grazia Caielli &Roberto de Franco & Danilo Giordano &

Evelyn Kustatscher

Received: 5 April 2012 /Accepted: 28 February 2013# The European Association for Conservation of the Geological Heritage 2013

Abstract The San Lucano Valley (Belluno, Italy) was the coretopic of the symposium: "L'armonia fra uomo e natura nellevalli dolomitiche” held in Agordo (Belluno) on the 12th and13th November 2010. In this work the valley is analysedaccording to the following features: geological, geomorpholog-ical, structural, stratigraphic and ecological. The purpose of thispaper is to review these features in order to establish the originsunderlining the intrinsic geomorphodiversity of this unique areain dolomites. By walking along the river and observing land-scape geomorphology or reading micro- and macroscale evi-dence on the mountainsides, the valley clearly reveals the keysto comprehending the geological history of dolomites fromTriassic to present. A full list of geomorphosites has beenappended in order to improve the scientific documentation ofthis valley.

Keywords Geomorphodiversity . Landform evolution .

Fossil plants . Knickpoint . Seismic stratigraphy .

Geomorphosite

The San Lucano Valley: a Rich GeomorphodiversityInherited from a 200 Million Years Old History

As defined by Panizza (2009), geomorphodiversity is acritical evaluation of geomorphological characteristics of aterritory. Based on such a study, some peculiarities of theDolomites Mountains, when compared with other alpinechains, both European or extra-European, are considered"unique" in relation to the forms of "structural" relief thatshow. In particular, they show such a high degree of extrin-sic geomorphodiversity to be potentially worthy of theUNESCO listing of “World Heritage” status (Gianolla etal. 2008). These intrinsic characteristics reinforce the rea-sons for such a definition, and those located in the SanLucano Valley were in 2009 considered to be part ofWorld Heritage area (Fig. 1).

Geological Framework

The San Lucano Valley is a deep valley carved into thecarbonate platform of the Pale di San Martino–Civetta, thelargest of Ladinian cliffs of the Dolomites. The Pale di SanMartino group is slightly curved into a gentle syncline(Leonardi 1968; Doglioni 1987, 1992; Castellarin et al.1996) and settled between the line of Valsugana, the geo-logical southern limit of the Dolomites and a back-thrustconnected to the same. The geological complexity of thevalley is remarkable. The oldest strata belonging to theWerfen Formation, which is overlain with a heterogeneousAnisian sequence witnessing an intense phase of tectonicactivity coeval to sedimentation, which continued even dur-ing the Ladinian (i.e. volcano tectonics). The Valley is aprivileged place to observe the relationship between carbon-ate reef, basin and Middle Triassic magmatism (intrusive

B. Testa (*) : B. Aldighieri :G. Caielli :R. de FrancoInstitute for the Dynamics of Environmental Processes - NationalResearch Council, Via Mario Bianco 9,20131 Milano, Italye-mail: bruno.testa@idpa.cnr.it

A. Bertini :D. GiordanoTechnical Industrial Institute of Mining “U. Follador”,Agordo (BL), Italy

W. BlendingerTechnische Universität Clausthal, Geology and PaleontologyInstitute Clausthal University of Technology, Leibnizstr. 10,38678 Clausthal-Zellerfeld, Germany

E. KustatscherMuseum of Nature South Tyrol, Via Bottai 1,39100 Bolzano, Italy

GeoheritageDOI 10.1007/s12371-013-0079-3

and extrusive with sedimentary volcaniclastic rocks) whichare directly connected to the genesis of the landscape.

The outcrops in the San Lucano valley range from Lower(Werfen Formation) to Upper Triassic (Cassiana Dolomite)and although the time interval is relatively short (about 20million years), they are abundant and varied due to themagmatism of Cima Pape. For this reason, it is better torefer to a stratigraphic relationships model (Fig. 2) instead ofa conventional stratigraphic column.

The Morpho-Structural Heritage (Secondary and TertiaryEras)

Lithology and Tectonics Factors Determining"Geomorphodiversity” of the S. Lucano Valley" and "Paledi San Lucano"

Morphotectonics (or morpho-tectodynamics) studies the rela-tionship between relief forms and tectonic movements(Panizza 1992), that is, the geomorphological consequencesof diastrophic shifts that have occurred from the beginning ofthe area’s geological history until now. In this case, theexisting San Lucano Valley drainage network is a LateMiocene heritage and by examining the temporal relationshipbetween tectonic setting and waterways one can observe that

the valley of the Cordevole river follows the first uplift phase(Sella-Tofane zone) before the raising of the ValsuganaAnticline, cutting sharply in a NS direction. The rapid anticli-nal uplift in the Pale di S. Martino area, generated a series ofstream valleys oriented along the structural slope (i.e. conse-quent valleys), for instance the Angheràz Valley (Fig. 3). TheSan Lucano Valley has an E-W orientation and has the char-acteristics of a subsequent valley, parallel to the tectonic axis,where weak formations and/or tectonic factors are presentcontrolling the valley setting. The peaks of the chain Agnèr–Croda Grande (Fig. 4) as well as the Pale di San Lucano(Fig. 5) are furrowed by deep gullies (“borai”, “van”), werethe rocks are cataclastic, easily eroded and associated with afault and fracture network (Angheràz Valley, Fig. 3).

The morpho-tectodynamic processes found in SanLucano Valley are obvious landscape dynamic examples,with significant gradients between mountain peaks and val-ley floors. The Dolomite’s peaks are sculpted along frac-tures in the form of towers, spears, pinnacles and ridges,such as the Agnèr Mt. (Figs. 4 and 10). They are also aperfect example of the original Mesozoic shelf slope, whichslopes down to the basin bottom.

Based on both bibliographic data and field observations,two geological sections were drawn (Fig. 6): the first cutsthe valley at Mezzavalle NS from San Lucano Mt. to Spiz

Fig. 1 Geographic sketch ofAgordo Area: San LucanoValley belongs to the thirdUnesco System

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d’Agnèr, the second, with a direction NW-S from Lastia ofGardès to Agnèr Mt. In the first example, the profile is quitesymmetrical, whilst the second section underlines the strongasymmetry of the valley’s profile, which is not attributableto the direction of the line of section. The steeper north side(Pale di San Lucano) is supported by layers of tenaciousdolomite, perpendicular to the slope and cut by a fault. TheAnisian-Scythian formations outcropping at the foot of thewall are partly covered by slope debris and rockfall rubbles.The Agnèr Anisian layers on the southern side, however, arefractured and tend to induce landslides. The asymmetricshape of the basin seems also to be attributable to structural

controls (Giordano 2011). Indeed, the geomorphology andgeomorphic indexes (Testa and Aldighieri 2011) support thehypothesis of a primordial structural-type control of thevalley, over which early glacial, fluvioglacial and finallyfluvial processes modelled the valley (Bini et al. 1999;Castiglioni 1964; Giordano 2011; Caielli and de Franco2011).

The result is that Quaternary deposits of both postglaciallandslides and debris flows are more extensive and powerfulon the southern slopes, inducing a gradual northwards mi-gration of the Tegnas thalweg where debris contribution isless frequent.

Fig. 2 Simplified relationshipsdiagram of San Lucano Valley(more information in Giordano2011): 1 Werfen Formation, 2Lower Serla Dolomite, 3Voltago Conglomerate, 4Agordo Formation, 5Richthofen Conglomerate, 6Morbiac Limestone, 7 ContrinFormation, 8Moena Formation,9 Livinallongo Formation, 10Sciliar Formation, 11Monzonite, 12 Pillow lava, 13Monte Fernazza Formation, 14Wengen Formation, 15Cassiana Dolomite

Fig. 3 Angheràz and Reianevalleys viewed from thesouthern side of Cima deiVanediei. Centre of picture theBordina creek valley truncatesthe Ladinian reef. S Schlernformation, L formation ofLivinallongo, V volcanics; 1Pian della Stua landslide, 2deep gravitational slopedeformation below the Pale deiBalcoi, 3 active debris flow inAngheràz Valley

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Due to the morpho-tectostatics, the rectilinear directionof the San Lucano Valley owes its origin to the presence ofstructural faults. A hypothetical fault line cutting the valleylengthwise, below the Quaternary cover, accounts for thedifferent thickness of the Anisian formations on both sides.These important facts are confirmed in high-resolution seis-mic surveys carried out near the church of San Lucano(Caielli and de Franco 2011). More specifically, there is noevidence of active or recent tectonics, marked by faultscarps and plans, incisions and torrents, river bends, dislo-cations of the ridge etc.

Morphoselection is generated by selective or differentialerosion when geological structure plays a passive role. Ifone refers to the lithological composition, this can be termedmorpho-lithology. When rocks are subject to the erosiveaction of morphogenetic agents (rivers, glaciers, snow-

frost, karst etc.) they have "morphological responses"according to their mechanical and lithological characteris-tics. The variety of rock formations leads to a selectiveseries of shape types, with steep cliffs and peaks in contrastto more gentle slopes, for example arenaceous-marly slopesbelow steep thick walls of dolomitic limestone. Hence, theSan Lucano Valley lithotypes can be divided into the fol-lowing four classes (Fenti et al. 2001), including rocks withsimilar behaviours:

A. Alternation of different lithological layers (sandstones,siltstones, marly limestone, marl and dolomite). Themechanical strength at the sample scale is variable,but the layers show a homogeneous mechanical behav-iour, determined by the dense layering and lithologicalalternation. They are characterised by a lack of

Fig. 4 The Agner–CrodaGrande chain and theunderlying Angheràz Valley.The influence of tectonics inlandscape genesis is very clear:the highest peak (the AgnérMt.) is separated from Spizd'Agnér (left) and the TorreArmena (right) by a doublegullies fault. Further to theright, the Van delle Scandole isset on a transcurrent fault, whilethe intense tectonics sculpts thecrest of Angheràz Valley into apiers and pinnacles landscape

Fig. 5 View of Pale di SanLucano Group from Grotta diSan Lucano. The slope to the leftof Lastia di Gardes is a structuralsurface coinciding with the Paledi San Lucano cliff slope, itsinclined stratification wellvisible; on the other hand, on topof Spiz Lagunaz, layers arehorizontal (inner lagoon, SciliarFormation). At the base of theTerza Pala a fault (in red) parallelto the wall is shown, whilst alarge mirror tilted fault can bedetected just below the summit.F.A. Agordo Formation, F.C.Contrin Formation, C.M.:Morbiac Limestone, F.S. SchlernFormation, F.L. LivinallongoFormation

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morphologic evidence, mild and rounded forms, not verysteep slopes, ledges, low rock walls and are easily erodedbecause they have been shattered by frost action (WerfenFormation; Voltago Limestone, Richthofen Limestone,Morbiac Limestone; Moena Formation, LivinallongoFormation; Zoppé Sandstones, "Heterogeneous Chaotic").

B. Volcanic rocks, sub-volcanic, conglomeratic rocks andvolcaniclastic sandstone. The cliff rocks are coarselystratified and not very fractured. They have medium to

high morphological hardness, and reach to more than100 m in height. Due to their basic composition theyare subject to surface alteration and break up easily (e.g.monzonites, latites, andesites, basalts of the M. FernazzaFormation and the "Marmolada Conglomerate").

C. Dolomites, carbonate rocks, limestones, arenaceouslimestones and sandstones layers outcrops in thickcompact decametric layers. However, the total thick-ness of the formation is generally moderate, so they

Fig. 6 Geological cross-sections through the SanLucano Valley: 1 Quaternarydeposits: alluvial/debris andlandslides, 2 WengenFormation and M. FernazzaFormation (Upper Ladinian), 3Monzonites, gabbros andsienites (Upper Ladinian), 4Sciliar Formation and CassianaDolomite (Ladinian–Carnian),5 Livinallongo Formation andMoena Formation (LowerLadinian), 6 Contrin Formation(Upper Anisian), 7 MorbiacLimestone and RichthofenConglomerate (Upper Anisian),8 Agordo Formation and LowerSerla Dolomite (Anisian), 9Werfen Formation (Scythian)

Fig. 7 Boral di Lagunàz. Thewall shows different degrees oferodibility of anisianformations. Agordo Formation(F.A.), Richthofen Limestone(C.R.), Morbiac Limestone(C.M.), Contrin Formation(FC), the trace (red) of a faultplane is also shown

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generate large steps from 10 to 50 m high, connected byinclined ledges. Here the morphologic evidence ismedium-high, as these are poorly degradable rocks, al-though being subject to rockfall by undermining of weak-er rocks at their foot (Lower Serla Dolomite, AgordoFormation, Morbiac limestone and Cassiana Dolomite).

D. Carbonate rocks, dolomite and limestone in massiveformations of hundreds of metres thickness. They havea solid limestone-dolomite appearance or are some-times decayed and with cavities, heavily layered orwithout stratification; the morphologic evidence is veryhigh, they form sub-vertical, vertical and overhangingcliffs, towering several hundred metres (Pale di SanLucano, Agnèr Mt. etc.) and are less erodible and

degradable. The high slope causes rock falls (ContrinFormation, Sciliar Formation).

This classification is reflected in the detailed review ofthe morphological evidence observed on the valley sides(Pale di San Lucano, Bordina Valley, Agnèr Mt. andAngheràz Valley). By observing the profile of the TerzaPala from the base, the layers of Werfen Formation andSerla Dolomite (Fig. 5), partially covered by landslide de-posits, make a gentle slope, then a first step corresponds tothe Agordo Formation bank, the Richthofen marly arena-ceous and Morbiac limestone layers then form another gen-tle slope interrupted by the overhanging wall of ContrinFormation before reaching the summit carved in the Sciliar

Fig. 8 Cascata dell’Infernoalong the Bordina creek is aclassic example of selectivemorphology; the threshold iscarved in Agordo Formation.Under the waterfall, on theright, separated by a fault, thecolourful Voltago Limestonelayers outcrops

Fig. 9 The Cima dei Vanidieirepresents a classic example ofa structural crest with slightlyinclined layers, originated byselective erosion. The top layeris constituted by thick tenaciouslayers of MarmoladaCconglomerate. On the hillsidebelow, outcrops layers of theless resistant of Fernazza Mt.Formation. Where slopeincreases, pillow lavas outcroptoo

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Formation. Beneath the Lastia of Gardès, an initial 50–60 mhigh wall carved in "Morbiac" nodular limestone pushesupwards with a large sloping ledge moulded into thin layersof Livinallongo Formation. The slope continues verticallywith the Sciliar Formation, occasionally interrupted byLivinallongo Formation and Sciliar Formation interdigita-tions. Observing the Boral di Lagunaz, on the left side of thevalley, from the San Lucano church the step modelled by theAgordo Formation can be easily recognised, protrudingfrom the eroded mountainside profile (Fig. 7).

The Cascata dell’Inferno, along the Bordina stream, is alsoa typical example of selective erosion (Fig. 8). In the upperpart of the Bordina valley, the effects of the heterolithic faciesof the Ladinian on the landscape are very striking. Other forms

due to selective erosion are the Cima dei Vanidiei structuralcrest (Fig. 9) and the steps of Prademur Mt. slope.

Pale di San Lucano: a Unique Example of PlatformCarbonates and Their Dolomitisation

The development of the Pale di San Lucano (Fig. 5) de-serves special attention due to its importance for studyingdolomitisation. Here, it is possible to recognise a first gen-eration of reefs (pre-volcanic and syn-volcanic SciliarFormation) prograding first and then aggrading, with a finallayer of the overlying Carnian rocks (De Zanche andGianolla 1995, Blendinger et al. 2007). Both are part of acurved carbonate platform which delimits the volcanic cen-tre of the Triassic Dolomites in their southern and easternsectors (Fig. 10). The thickness of approximately 1.5 km ofMiddle Triassic (242–238 Ma) carbonates is of exceptionalimportance for two reasons:

1. The Pale di San Lucano is one of the very few exampleswhere a progradational platform top is directly visible.The other two examples are the Capitan reef complex(Permian) in North America, and the Pighera Mt., thesouthernmost outlier of the Civetta massif adjacent tothe Prima Pala di San Lucano. The progradational in-terval is about 110 m thick and thins out towards theNW. The bedded carbonates are laterally replaced bysteeply inclined clinoforms (30–45°) and contain a“marker bed” (Fig. 11) about 3 m thick, which corre-sponds to the maximum progradation and provides ev-idence of the volcanic “event” of the Dolomites.Progradation was about 750 m to the NW, but the fullsymmetry is nowhere preserved. Therefore, it is notclear whether the progradational interval was a genuine“platform top” or merely a terrace at the foot of a moundchain in the SE, such as the chain of Agnèr Mt.

2 . A potent ia l ly grea ter impor tance is f rom ageomorphodiversity point of view, as the progradationalinterval offers a unique possibility to resolve the mysteryof dolomitisation of the Dolomites, because of its onlypartially dolomitised. In the same outcrop, two types ofdolomite occur: a white, saccharoid type (Figs. 12 and

Fig. 10 Edge and the north face of Agnér Mt

Fig. 11 Three-dimensionalmodel of the Contrin Formationunder the Pale di San Lucano,looking northward, andhypothesis of its internalstratification. The Contrin"platform" is not just anaggrading platform, but it showsa "mound" under the Quarta Palaand laterally migrates to thebasin and towards stratifiedcarbonate sediments

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13) and a yellow towhite very finely crystalline type. Thelimestone is typically pale grey and, in thin section,shows a boundstone fabric which is very similar to trav-ertine, but a sparse marine fauna is often present. Relictstructures are also well preserved in most of the dolo-mites, indicating that they are a dolomitised limestone.Limestone passes both laterally and vertically into dolo-mite, showing numerous dolomitisation fronts, in whichthe calcite passes into pure dolomite within a fewdecimetres (Fig. 14). These dolomitisation fronts are alsopeculiar because of the mineral paragenesis: the dolomitecrystals are corroded by fibrous calcite cement, which isthe most important cement mineral in the adjacent lime-stone. This indicates a very early dolomitisation at thesediment water interface and immediately below. Theyellow dolomite is similar to the so-called “cycle caps”of the Latemar, but its vertical and lateral distribution isvery irregular and most likely to not be the result ofsubaerial platform exposure (Fig. 15). Another peculiar-ity of the Pale di San Lucano carbonates is the geochem-ical record, which is, of course, not observable in the fieldbut requires laboratory measurements (for more detailssee also Blendiger et al. 2011). The dolomitisation of thePale di San Lucano was most likely caused by fluidssinking through the platform, as a continuous processaccompanying deposition, but it is not yet entirely clearwhat caused the distribution of limestone and dolomiteand the higher-than-seawater density of the fluids. Theso-called ‘reflux model’ has long been suspected to beresponsible for the dolomitisation of other platforms inthe Dolomites, but has recently been challenged in favourof a hydrothermal model with exactly the opposite flow

Fig. 12 a Thin section of a saccharoid dolomite with several smalltubular voids like bacteria colonies, in blue due to impregnation withcoloured plastic. The preservation of the round shape, smaller thandolomite crystals, suggests that dolomite recrystallised before the bac-teria disappearance. b Thin section of a "cycle cap"- type dolomite, cut

by a vertical fracture filled by saccharoid dolomite. The micritic texture“boundstone”-type is very similar to limestone, even if macrofossilsare not present. Voids are filled by fibrous dolomite, but a light porositystill remains

Fig. 13 Direct contact between a saccharoid dolomite and a yellowish"cycle cap"-type dolomite bank

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direction. The problem has not yet been conclusivelyresolved and the Pale di San Lucano continues to be akey natural laboratory to test dolomitisation models.

Fossils Plants: an Added Value to the Geomorphodiversity

Plant fossils are generally rare in the Dolomites, althoughremains are known from the Upper Permian (e.g.Bletterbach, Cuecenes, Mölten), from the Middle Triassic(Anisian, e.g. Kühwiesenkopf/Monte Prà della Vacca, Piz daPeres; Ladinian, e.g. Seewald, Ritberg, Corvara) and fromthe Upper Triassic (Carnian, Heiligkreutz, Stuores Wiesen,Rifugio Dibona). For more details, see Wachtler and VanKonijnenburg-van Cittert (2000), Visscher et al. (2001),Broglio-Loriga et al. (2002), Kustatscher and VanKonijnenburg-van Cittert (2005), Kustatscher et al. (2004,

2010, 2012). The discovery of plant fossils from the MiddleTriassic of Agordo area, therefore, adds important informa-tion on the composition of the Middle Triassic vegetationand on the distribution of emerged land during this timeperiod (Kustatscher et al. 2011).

Palaeogeographic reconstructions for the Anisian (lowerMiddle Triassic) suggest a marine environment with anextensive island extending over the northern and centralDolomites. Several plant horizons have been found northand west of this island, but until now only limited informa-tion was available on its southern extension.

The recovery of plant fossils in Anisian sediments of SanLucano Valley is, therefore, of particular palaeogeographic inter-est and, furthermore, increases the valley geomorphodiversity—even though only a few plant fragments (~30) have beenrecorded. These plant fragments belong to the horsetails, ferns,seed ferns, cycads and conifers. The most abundant group in theflora are the conifers which include Voltzia sp., which is partic-ularly interesting because it shows some characteristics that havenever been described in the Dolomites. The lateral shoots arisealternately from the main shoot and are covered densely andhelicoidally by the leaves. The leaves are fine, narrow and falcateand referred to Voltzia recubariensis (De Zigno) (Schenk 1868;Broglio-Loriga et al. 2002). The genus Albertia is well knownfrom the Anisian of France (Grauvogel-Stamm 1978). Thehorsetails are represented by stem and rhizome fragments, bothprobably belonging to the genus Equisetites. Unfortunately, themissing microphylls on the stem fragments does not allow amore detailed taxonomic attribution. The ferns are representedby four different taxa: Anomopteris Brongniart 1828,Neuropteridium voltzii (Brongniart) Schimper 1879 andScolopendrites sp. are typical for the Anisian of France andGermany (Fuchs et al. 1991) and belong to the Osmundaceae,a family today well distributed in the tropical and subtropicalarea. Cladophlebis remota (Presl) Konijnenburg et al. 2006 is aspecies well known in the Ladinian and Carnian of Europe (e.g.Heer 1877; Leonardi 1953; Kustatscher and Van Konijnenburg-van Cittert 2005). Only one fragment of a female organ with an

Fig. 14 Net, but wavy shaped,contact between a limestoneand a saccharoid dolomite in abank. The 87Sr/86Sr ratio valuesare outside the marine field inboth rock types

Fig. 15 3-D model of dolomite and limestones belonging to theprograding portion of Pale di San Lucano, seen from the SSE. a Blockdiagram resulting from interpolation among mineralogical facies oftwo dolomite type and limestone. b The same model "eroded" by theunderlying progradation surface and the topographic roof, showing thecurrent distribution of layers

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umbrella-like shape (Peltaspermum sp.) belongs to the seedferns. A single leaf fragment of the cycad Taeniopteris sp. hasbeen found, an entire margined lamina with no secondarybifurcating.

The flora found in Agordo Formation, although only frag-mentarily preserved, corresponds to a typical Anisian flora. Themain markers such as Equisetites (Fig. 16) in the sphenophytes,Anomopteris (Fig. 17), Neuropteridium/Scolopendrites in theferns and Voltzia (Fig. 18) and Albertia (Fig. 19) in the conifersare all there. Additionally, there are fragments of the seed ferns(Peltaspermum) and cycadophytes (Taeniopteris) that are welldocumented from the Anisian of the Dolomites (e.g. Broglio-Loriga et al. 2002) but appear in the fossil record of theGermanic Basin mostly within the Ladinian. Although the areahas an important and complicated geological history withsynsedimentary tectonics, the plant fossils of AgordoFormation reflect a well-defined flora. The plant remains aremostly fragmented and small and often badly preserved, indi-cating a long transport from the growing to the depositionalarea (Kustatscher et al. 2011). The relative high amount of fernfragments in the flora, considering biases due to taphonomic

selection, indicates that the flora was rich in ferns, probablyreflecting a warm and humid climate. Additionally, the florashows the presence of some emerged lands nearby, covered bythe Anisian vegetation typical of the Dolomites (Kustatscher etal. 2011).

The Quaternary Heritage

Glacial Landscape

The Cordevole valley is a very ancient fluvial valley (UpperMiocene), which existed prior to the Belluno Dolomites upliftbut continued to be excavated during the latter period. Thefirst major glacial expansion dates from 2.4 Ma. From thisdate until the first part of the Quaternary (0.9 M.y. BP), manymoderate glacial fluctuations have occurred (Bini et al. 1999).

During the Last Glacial Maximum (LGM), the "Cordevole"glacier in the Agordo zone exceeded 1,500 m in altitude(Castiglioni 1940) and it joined the glaciers coming from theCivetta (Corpassa Valley) and Pale. The secondary San LucanoValley is unexpectedly wider and deeper than the main

Fig. 16 a Fragment ofEquisetites beam; b Plants ofEquisetum, a recent sfenofita

Fig. 17 a Fragment ofAnomopteris mougeotii beam; bplants of Osmunda regalis

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Cordevole Valley—this can be explained by its geographicalposition which is characterised by higher rainfall than the restof the Dolomites and the ‘zero isotherm’ located at loweraltitudes than in the northern Dolomites. The "San Lucano"glacier was probably one of many tongues derived from theplateau icecap and was supplemented by snow avalanchesfrom the deep Agnèr gullies. The valley cross-section has aflat bottom and steep sides, which indicates glacial wideningand some downcutting. For examples, the furrows excavatedby rivers in the bedrock of Tegnàs at the San Lucano churchare over 200 m deeper than the present floodplain (Caielli andde Franco 2011; see chapter 1.3.3).

Other examples of glacial erosion forms are the massiveglacial cirque of Angheràz Valley (Fig. 20), suspended cir-cuses (Pian del Miel, Seconda Pala) and roche moutonéedeveloped in dolomitic rocks (Fig. 21). Accumulation formsare modest but very significant: Castiglioni (1939) identified aseries of moraines, attributed to the Buhl stage, slightly up-stream from Taibon (Torte locality) and the terminal and sidemoraine of the Gschnitz stadium in the Angheràz Valley.Recently, other terminal moraine banks (attributable to Daunstage) were discovered at around 2,000 m above sea level nearthe Tromba di Miel (Fig. 22).

At the Pont locality, outcrops consisting of sandy clay anddark silt layers with frequent dropstones, have been identifiedas lacustrine deposits of a glacial contact lake (Fig. 23),attributable to the early glacial retreat. Other lacustrine

deposits of clay and silty clay were identified by a 50-mmechanic bore at the Paluc locality, near San LucanoChurch. These clays, covered by fluvial gravel and cobbles,reveal a dammed lake correlated with buried moraine banks ofthe Buhl stage. The permeability of different soils in this areacompared to the innermost part of the valley is also underlinedby the spread of springs (see Tegnas River Geomorphology asa Morphodynamic Witness).

Gravity-Related Forms

The variety of the landslides has produced an importantexample of intrinsic geomorphodiversity at a regionalscale: the complexity of their categories, causes, age,lithology, motion, extension etc. (Soldati et al. 2004)make the San Lucano Valley an open laboratory forworldwide research. Glacial remains, perched on thenorth facing slopes, currently generate deformationswithin surface discontinuities. Gravity is the most im-portant morphogenetic action, since the disappearance ofthe glaciers, due to the exceptional gradients of theslopes. Massive mudslides (debris flow) are widespreadin the Angheràz Valley and Van de Mez, where acontinuous detrital aquifer, consisting of coalescing al-luvial fans and deposits of landslide surrounds bothsides of San Lucano Valley. Large postglacial landslidescame from slopes and collapsed towards the valley. The

Fig. 18 a Detail of Voltzia sp.branch with visible falciformneedles; b branch of Araucariaplant

Fig. 19 a Fragment of leafAlbertia sp. b Fragment of leafAlbertia sp

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largest, located below the Pale dei Balcoi (Fig. 3)(Castiglioni 1939; Zampieri 1987), is probably a deepgravitational slope deformation. Observing the morphol-ogy of the southern slopes below the Agnèr togetherwith the fracturing of rocks (Fig. 4), it can be assumedthat similar phenomena have also affected the slope infront of Lagunàz and Borselle localities. The rubble ofthe landslide is mostly buried beneath the alluvial coverwhich is very deep in this area, as the ice over-excavation exceeds 200 m. Another extensive landslidedeposit is found in the Reiane Valley volcanics of Piande la Stua area. The best known landslide is the rockfallof Pra Lagunaz, which detached in 1908 from the Cimedi Van del Pez (where unstable masses are still observ-able) (Doglioni and Bosellini 1987; Doglioni 1987,

1992, 2007; Castellarin et al. 1996; Zattin et al. 2008;Stefani et al. 2007).

Revealing Buried Geomorphology UsingSeismostratigraphy and Seismic Tomography

To determine the hidden physical structures of the San LucanoValley, two high-resolution seismic lines were executed by theIDPA-CNR (Milan unit), across the Tegnas stream toobtaining information on seismostratigraphy, wave propaga-tion speed and the morphology of buried structures (seismictomography; Fig. 24). The same data was also interpretedusing a multirefractor method to give an image of discontinu-ities directly from the seismic sections.

Fig. 20 a Northward view ofCima Pape and Lastia diGardes, taken from the top endof Angheràz Valley. In theforeground of the picture arevisible a landslide debris and adebris flow, the small woodedhill in the picture centre is amoraine embankment of theGschnitz stage

Fig. 21 The Fradusta Glacieron the Pale plateau, seen fromCime dei Vanidiei. On the left aglacial circle suspendedbordered by a fault scarp (Piandel Miel); on the right asuspended glacial valley (ValReiane). The action of LGMglaciers is recognisable fromerosion ("montonatura") ofdolomite rocks

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The data generally has a good signal/noise ratio and thesections obtained are shown in Fig. 25. The final seismicsection on line 1 (Fig. 25a) reveals the reconstruction ofburied structures to a depth of about 200 m. The reflectivitycharacteristics of the seismic basement and sedimentarycover found in glacial-type valleys are described in a previ-ous paper by de Franco et al. (2009).

From the top to the bottom of each section, observethe presence of three seismic units can be observed, themost superficial of which is characterised by a P-wavevelocity up to 1,700 m/s and reaching a maximumdepth of about 60 m comprises recent sediments satu-rated by water. Below, there is a second seismic unitcharacterised by P-wave velocity greater than 2,500 m/s.This layer is made up of compact sediments 100–110 min depth, but decreasing northwards and southwards andreaching, respectively, depths of 30 and 40 m. A third

unit of maximum thickness and at the maximum depthof approximately 200 m southward, showed velocitiesof over 3,200 m/s and may comprise portions of col-lapsed basement. The final seismic section obtainedalong the line 2 (Fig. 25b) shows similar characteristicsto those described for line 1.

The images obtained show the presence of a refractor at adepth of approximately 60 m which further deepens south-ward; this discontinuity may be interpreted as a boundarybetween the more recent (i.e. post glacial) unconsolidatedalluvial deposits and the underlying compacted fluvial–gla-cial deposits.

The processing of seismic data acquired in the SanLucano Valley provides: (1) an 'echo' image from subsurfacereflection points, (2) the velocity of compressional seismicwaves and (3) the refractor image.

The interpretation of the images has allowed thereconstruction of both the geometry of the main refrac-tors of recent deposits and the geometry of the bedrock.It also suggests the presence of multiple depositionalsequences and a maximum depth of a few hundredmetres (up to 250 m). Integration of results with thegeology, structural geology, surface geomorphology andgeostratigraphy allows the characterisation of the phys-ical valley structure (geometrical and geo-mechanicalparameters) and the reconstruction of the seismic stra-tigraphy of the sedimentary cover and seismic basementand the location of buried morphological structures. Forboth lines (Fig. 25) we can hypothesise a depositional-centre migration from south to north, probably due toboth superficial and deep gravitational collapse thatmoved northward during the alluvial process. Positionsof an older depositional-centre can also be identified,respectively at a depth of 60, 135 and 240 m.

Fig. 22 Frontal moraine levees(Daun stage) in Val del Miel

Fig. 23 Clayey-sandy silts with glacio-lacustrine dropstone near Pont site

Geoheritage

Tegnas River Geomorphology as a Morphodynamic Witness

The San Lucano Valley is a tributary of the main CordevoleValley (Belluno). It retains a clear glacial imprint and itsaverage entrenchment is nearly 2 km deep, having crossedthe nucleus of the largest cliff of Belluno Dolomites (wherecarbonate and detrital sedimentary rocks are intimately asso-ciated with intrusive and extrusive igneous rocks). The water-shed rises to an elevation of over 3,000 m above sea level,

confining a drainage network of 167 km (approximately46 km2) across a catchment area confined between the twovertical walls of the Pale di San Lucano and Agnèr Mount. Inthe westernmost part of the valley (see Fig. 31) two fourthorder tributaries collect rainfall from a 29-km2 watershed. Oneof them, the upper Tegnas, flows northward through theAngheràz Valley while the other (Bordina stream) flowssouthward, converging at 850 m above sea level (Col di Pralocality) and giving rise to the main fifth order Tegnas stream.

Fig. 24 Above, two images of San Lucano Valley: orthophotomap(left) and eastward view of the 3D model (right), showing two seismiclines (line1, A–A1 and line2, B–B1) and their location in respect to San

Lucano Church and to the knickpoint. - Below, the arrows indicate thetwo seismic lines on two topographic sections cutting the valley inNNE-SSE direction

Fig. 25 Final stack section obtained along line 1 a and line 2 b after static corrections, converted to depth. The lines show limits of identified units

Geoheritage

This stream runs eastward, mostly on flat land with less than2% of slope, interrupted by a few rapid steps for 4 km until theSan Lucano church (750 m above sea level). The slope

steadily increases until the stream meets the Cordevole Riverat 610 m above sea level after 3 km.

The land use in the San Lucano Valley is not intensiveand there has not been interference to the riparian zone sincethe flood of 1966, during which the majority of the existingtrees (mainly conifers) were uprooted. After the flood of1966, an exceptional riparian forests of Alnus incana and

Fig. 26 Fluvial terraces of Tegnas River upstream from the SanLucano Church. Above an old streambed; below the highest level is arelict of 1966 event floodplain

Fig. 27 Tegnas stream near Coldi Pra' village. Thalwegchanges observed and mappedbetween Bordina creekconfluence and the path toCozzolino Refuge, from the last35 years

Fig. 28 Tegnas stream view: San Lucano Church is located over aknickpoint where a buried dam causes a thick gravel upstreamdeposition

Geoheritage

Fraxinus excelsior with some Mountain Maple and Sprucetook over. These forests are of high natural interest for theEuropean Community (site BL28 from Natura 2000 net-work in ARPAV 2001) and the area is now conserved andconstantly monitored. For these reasons, the lower Tegnasriver has become an open laboratory to study the stream andhow it adjusts to both past and recent morphodynamicevents. The geomorphology of this stream is also evidenceof channel changes over a 50-year period (Figs. 26 and 27).

These geomorphological processes are reflected in thechanges of the stream (Rosgen 2003; Powell et al. 2004;Testa and Aldighieri 2011). By observing fluvial geometry,such as bankfull stage indicators (Leopold et al.1964), riv-erbed entrenchment and sinuosity, changes in granulometryalong the stream, riverbed slope, aggradation or erosionprocesses, changes in the type of stream can be tracked(Harrelson et al. 1994). Following the Rosgen StreamClassification (RSC) (Rosgen 1994, 1996), these authorsidentified two main stream behaviours upstream and down-stream from San Lucano Church (Figs. 28 and 31). Thechurch is located near to the river, where the valley bottomis filled with 200 m of fluvial deposits due to a waterproofseptum (see Glacial Landscape). This septum comprises aburied moraine (Castiglioni 1939; Giordano 2011) which is

probably overlain by a collapsed deep landslide (Caielli andde Franco 2011), generating a natural break point in thelongitudinal profile of the stream: a "knickpoint". Thisknickpoint underlines the sudden change of the hydraulicregime and along few hundreds of metres the following canbe observed:

Upstream, a meandering sequence of unstable F4 andstable B4 and C4 stream-type channels, as described byRosgen (2001, 2003, 2006) (Fig. 29) digresses andmoves an amount of sand and gravel material unexpect-ed for the discharge and watershed size, to an aggradingD4 stream type and makes a large and deep (more than200 m) gravel deposit (lake sediments were found in adrill).

Downstream, a steep B2 stream-type, probably ofrelatively recent age, entrenches its bed with flow con-trolled by the gravel reservoir and increased spring-timewater. The stream then progresses to a more confinedchannel morphology (G-type and F-type) (Fig. 30) carv-ing its alluvial fan until it reaches the Cordevole river.With the current climatic conditions, only centennialfloods will probably be able to reach the highest naturalbanks (Fig. 30—B2), which, therefore, remain as “rel-icts” of past hydro-climatic conditions.

Fig. 29 Tegnas, upstreamstream-type sequence,classified by RSC method.Stream reaches are locatedbetween Bordina creekconfluence and San LucanoChurch: after an initialerosional occurrence (F4),riverbed is aggrading (D4) untilthe knickpoint. (C4 view isdownward, all others areupward)

Fig. 30 Tegnas, downstream stream-type sequence, classified by RSCmethod. Stream reaches are flowing downstream from San LucanoChurch to the Taibon village: starting from a bedrock controlled reach

(B2) the riverbed is more and more entrenched, depositional processesare quite absent (B3) until the confluence with Cordevole river. (B3view is downward, all others are upward)

Geoheritage

Enhancing the San Lucano Valley Geoheritage

Geomorphosites Assessment

Introduced by Panizza in 2001, the term "geomorphosite"shows the “characteristics of the landscape with particularand significant geomorphic attributes that qualifies the sameas part of the cultural heritage of a territory" (Panizza andPiacente 2003). The San Lucano Valley shows an assortmentof notable geomorphological features and an abundance ofgeomorphological and geological features that constitute aninheritance of global significance (Fig. 31). Among these,karst features such as karren-type fields (rillenkarren,rinnenkarren, trittkarren and kamenitza) are distributed onthe reef slope surface of the Pale dei Balcoi and in Pian diMiel. Sinkholes are also frequent in the Pale di San Lucano,the Pale di S. Martino plateau and along the fault of Costondella Vena (about 20 m deep). There are also several karstsprings, among which the best known is the Livinàldell’Acqua, which flows with more than 100 l/s, and two

curious rock arches, the Besanel arch at the top of Boral deLagunàz and "El Cor" on the Pale dei Balcoi, characterised byan unusual heart shape. A complete set of interesting sites,already known in literature (Bertini 2011), was taken intoconsideration for the assessment of their “scientific quality”index (Q), by using the Coratza and Giusti (2005) method, asreported in Panizza (2005).

In the previous sections, three geomorphosites of remark-able significance regarding the geologic, palaeoclimatic andmorphodynamic evolution of the valley were comprehensive-ly explained: the first is the Ladinian dolomite/limestoneoutcrop (Figs. 13 and 14), the second the Anisian fossil plantsdeposit (Figs. 16, 17 and 18), and the third is the knickpoint ofthe Tegnas river near to San Lucano Church (Fig. 28). In thissection we assess a Q value for them, so as to calibrate theeffectiveness of the cited method (Coratza and Giusti 2005).To obtain the quantitative assessment, each geomorphositeshas been assigned to a category according to the Carton et al.(2005) outline: Area (e.g. moraine deposit, glacial circus etc.),Line (e.g. stream or river, waterfall, gully etc.) and Point (e.g.

Fig. 31 Orthophotomap of SanLucano Valley watershed:location (points, lines andareas) of geomorphosites listedin Table 4 and main toponyms

Table 1 Score values assignedto each parameter

The “null” value can be assignedonly to Z

Observations Score=0 Score=0.25 Score=0.50 Score=0.75 Score=1

S Low Medium High Very high

D Low Medium High Very high

A (% of total area) <25 25–50 % 50–90 % 90–100

R Several Medium Few Unique

C Bad Medium Good Very good

E Occulted Partially occ. Easy to see Well exposed

Z No value Poor value Medium value Important v. Essential v.

Geoheritage

erratic boulder, tower, small cave etc.). Coratza and Giusti(2005) have suggested that the letter Q should be attributed tothe sum of the parameters (capital letters) that experts on andor observers of the area denote according to the followingformula:

Q ¼ sS þ dDþ aAþ rRþ cC þ eE þ zZ

Where: S=“scientific research”, D="didactics", A="ar-ea" (total area of geomorphosite), R="rarity" of similargeomorphosites in the same area, C="state of preservation",E="exposure" and Z="added value".

Furthermore, the computation of Q is finalised by multi-plying each score to its corresponding weight (lower case).In our case the assigned weights are: s=0.75; d=0.75; a=0.5; r=1; c=0.75; e=1 and z=1. An assessment score(Table 1) to each of the above parameters is attributedfollowing the criteria resumed below:

S: This factor cannot be null, otherwise the geositecannot be considered. Particular importance is givento this parameter so, as to attribute a high “S” score,i.e. numerous publications and research projects arenecessary.D: The geological processes in the site must beexpressed as evident and of exceptional importance.A: Area of geosite divided by the total area of similartypes of geosite. It is important to be aware of theextension as the bigger the geosite is, the higher itsscore will be.R: Rarity with respect to other nearby geosites. In thiscase the rarity of the geosite is compared to thosenearby; the geological must be unique within a certainstudy area and work scale.C: The preservation level of the site is evaluated todetect if the initial integral status has been modifieddue to of natural factors (e.g. weathering), anthropicactions (e.g. buildings) or acts of vandalism.

E: Evaluation of the site’s exposure. To determine thelevel of visibility or presence of anthropic elementswhich impede direct access.Z: The importance of the geosite is not exclusivelyin relation to its geological content but also aconsequence of its ecological, historical and/or tour-istic values.

Therefore, to express the scientific importance of thegeomorphosite so as to be able to compare the results withothers assessed with different methodologies, the sum (Q) ofthe scores is normalised between 0 and 1 following theformula:

Q norm ¼ Q=Qmax in this case Qmax ¼ 7ð ÞThe computational procedure of the Q value for all three

tested geomorphosites is displayed in Table 2.Finally, the ultimate value of a geomorphosite is

obtained by adding to the Scientific Value “Q” anAdditional Value, assigned following the indicators

Table 2 Detailed score values assigned to each one of the test geomorphosites

Knickpoint Fossil plant of agordo FM Dolomitisation outcrop

Score Weight Q Q_norm Score Weight Q Q_norm Score Weight Q Q_norm

S 0.25 0.75 0.19 0.03 1 0.75 0.75 0.11 1 0.75 0.75 0.11

D 0.75 0.75 0.56 0.08 0.5 0.75 0.38 0.05 1 0.75 0.75 0.11

A 0.25 0.5 0.13 0.02 0.25 0.5 0.13 0.02 0.25 0.5 0.13 0.02

R 1 1 1.00 0.14 1 1 1.00 0.14 1 1 1.00 0.14

C 0.75 0.75 0.56 0.08 0.5 0.75 0.38 0.05 0.75 0.75 0.56 0.08

E 0.5 1 0.50 0.07 0.5 1 0.50 0.07 1 1 1.00 0.14

Z 0.5 1 0.50 0.07 0.25 1 0.25 0.04 0 1 0.00 0.00

SUM 4 3.44 0.49 4 3.38 0.48 5 4.19 0.60

Bold items are the parameters expressed by the formula in the text

Table 3 Description of the “additional-values” added to Q for theassessment of the ultimate geomorphosite value

Additional value Description

NR Nature rarity

ME Model of evolution

DE Training example

PE Paleoenvironmental highlights

EV Ecological value

SHV Historical–scientific value

MV Mineralogical value

PV Paleontological value

SCV Scenic value

PRV Prehistoric value

CRV Religious cultural value

SEV Socio economic value

Geoheritage

Table 4 Geomorphosites of San Lucano Valley, ranked by decreasing value of scientific quality (Q)

Label Geomorphosite name Type Scientific quality/value (Q) Additional value

1 Pizèt Point 4.56 ME, DE, DHV, SCV, CRV

49 Dolomitisation outcrop Point 4.19 NR, ME, DE, PE, SHV

2 Brecce Pónt, Cave Marmo Nero Area 4.19 SHV, CRV, SEV

3 Cascata di Pónt Line 4.06 ED, DE, SCV

4 Forcella Gardès Area 4.06 DE, PE, ME

5 Circo Testata Valle Angheràz Area 4.00 ME, DE, PE, SCV

6 Parete Nord Dell'Agnér Line 4.00 NR, EV, SCV

7 Frana Prà E Lagunàz Area 3.94 SHV, CRV

8 Deposito di Pónt Point 3.88 NR, ME, PE

9 Cascata Dell'Inferno Line 3.81 DE, PE, SCV

10 Pian di Mièl Area 3.81 ME, DE, SCV

11 Sill di Malgonera Area 3.75 NR, DE

12 Van Del Pez Area 3.56 NR, DE

13 Livinal Dell'Acqua–La Sfèsa Point 3.56 DE

14 Morene Stadiali Valle Angheràz Area 3.50 ME, DE, PE

15 Le Peschiere–Lago Area 3.50 PE, DE, ME, SEV, SCV

16 Frana Postglaciale di Péden Area 3.50 PE

17 Campanile Della Besàuzega Point 3.44 DE, SCV

48 Knickpoint Point 3.44 NR, ME, DE, SHV

19 Forcella Cesurette Area 3.44 PE, SHV, MV, SCV, PRV, SEV

18 Fossil plants of Agordo FM. Point 3.38 DE, PE, SHV, PV

20 Conglomerato Interglaciale Point 3.38 NR, PE

21 L'Anfiteatro Seconda Pala San Lucano Area 3.38 DE, PE, EV, SCV

22 Campo Boaro Area 3.38 DE, EV, MV, SCV

23 Piano Inclinato Area 3.25 DE, SCV

25 Cascata Val Reiane Line 3.19 DE

26 Faglia Bordina Line 3.19 DE

24 Crepe Rosse Line 3.06 DE, ME

27 Le Peschiere–Masarèi De Le Tòrte Area 3.00 ME, DE PE

28 Tromba di Mièl Point 3.00 NR, DE, SCV

29 Circhi Sommitali Pale San Lucano Area 2.94 ME, DE, PE, SCV

30 Grotta San Lucano Point 2.81 DE, SHV, CRV

31 Sass Da Le Cròss Point 2.81 SHV, CRV

32 Boral di San Lucano Line 2.81 DE, SCV

33 Torre Armena Line 2.81 DE, SCV

34 Valón De Le Scàndole Line 2.81 DE

35 Alveo Epigenetico Bordina Line 2.81 NR, ME, PE

36 La Ghiacciaia Point 2.75 NR, DE

37 El Cor Point 2.56 NR, DE, ME, SCV

38 Boral De La Besàuzega Line 2.56 DE

39 Boral di Lagunàz Line 2.56 DE, SCV

40 La Scudèla Area 2.56 DE, PE

41 Corn Del Bus Point 2.56 DE, SCV

42 Covol Mont Point 2.31 ME

43 Arco Del Bersanel Point 2.31 ME

44 Cól De L'Usèrta Point 2.19 SHV

45 Pòles Point 2.13 NR, ME, SCV

46 Sorgenti di San Lucano Point 2.06 ME

47 Roa Del Forn Line 1.94 PE

Bold items are the test geomorphosites of Table 2

Geoheritage

expressed in Table 3. This added information does notmodify the Q value, but gives a further qualitative contri-bution to the site description.

Discussion and Limits

This study has considered the various parametersaccording to a census of the geomorphosites, evaluatingthe connection between their heritage importance, thesurrounding landscape and its use. “The ScientificQuality of the site is only a numeric indicator, subjectto variation according to the observers judgment andgeneral characteristics of the studied area” (Coratzaand Giusti 2005).

The scores have been given following the guidelinesof Avanzini et al. (2005), which have been modifiedaccording to the requirements of the San Lucano Valley.The result is the list of Table 4: the highest Q valuescorrespond to a site (Pizet) that is strongly connected tothe local community history (quarry activities, land-slides). The test site of Dolomite outcrop came in sec-ond place. The excursion itineraries and touristicallyimportant landmarks also obtained a high score.Geological, ecological or geomorphological elementshave an intermediate value of Q (peat bog, knickpoint,faults, fossils, glacial moraines) irrespective of theirscientific importance. Low marks are given to the “pe-culiarities” which are part of either collective imagina-tion (El Cor, la Scudela, la Ghiacciaia and Roa delForn) and/or ecological–technical properties (SanLucano springs).

The principal limit with this method is tied to the influ-ence of the operator’s personal experiences. Another limita-tion stems from the attribution of the so-called weightingthat does not follow a clear and univocal line of thought. Inthis case, the weighting has been assigned according to thegeological and geomorphological characteristics of the areawith the purpose of enhancing the San Lucano Valleygeoheritage in a geotouristic context and the values, there-fore, are high especially with regards to “rarity”, “exposure”and “added value”, but this result can be reached in otherways.

Final Considerations

The San Lucano Valley is already well known for its naturalattractions. This paper has documented the abundance andassortment of geological and geomorphological sites of thearea as witnesses of a 200 million years old history, and howthese elements are still preserved and also show the mostrecent landscape evolution. Furthermore, attempting to ap-ply a pre-existing analysis and classification, the current

authors employed a method that, notwithstanding its limita-tions, enabled the application of the scores, ranging from0 to 1, to a set of geomorphosites, in order to enhance theirimportance from the geotouristic perspective.

This study, therefore, classifies the San Lucano Valley asan important inheritance of global significance and as aunique geomorphosite within the Dolomites area. Indeed,in 2009 this valley, together with other dolomitic groups,was included in the UNESCO program and the scientificimportance of this area could, therefore, be promoted asfollows: informative boards along the valley, tourist-information points, publication of geotouristic guides andmaps and other modern forms of communication (i.e.through web facilities, GIS, WebGIS and Apps for mobiledevices).

This promotion could be achieved with collaborationbetween local authorities, official governmental authorities,territorial administrations, non-profit organisations, togetherwith research institutions. As predicted by Desio in 1947, itcan be confirmed that the leading role of local geologyexperts is an important key for the widespread of the geo-logical culture.

Acknowledgements Many thanks go to all the authors whoattended the Agordo symposium together with the chairman ofthe conference Eng. Luciano Sabbedotti, who helped with theinitial preparation of these notes. Many thanks also go to thecolleagues of ARPAV (Belluno) who worked in the field and tomany local people and undergraduate students that worked hard todevelop public awareness. Valuable acknowledgements to the re-viewers Prof. Mario Panizza, Prof. José Brilha and an anonymousreviewer who provided a substantial contribution to the finalversion of this manuscript.

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