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Gran Sasso Massif, Centralltaly) Landform Analysis, Vol. 2: 37-43 (1999) The extent of Pleistocene glaciations in the western part of the Campo lmperatore (Gran Sasso Massif, Centralltaly) Carlo Bisci, Bernardino Gentil; Francesco Dramis Depanmelll ofEarth Sciences, Department ofGeological Sciences, University ofCameril/o, Third University ofRome, via Gentile III da Varcmo, Camerino 1-62032, Italy Largo Sail Leonardo Mllrialdo /. 1-00/46 Rome.Italy Sirio Ciccacci Adam Kotarba Departmelll ofEarth Sciences, Department ofGeomorphology alld Hydrology, University "La Sapienza ", Polish Academy ofSciences, p. A. Moro, 1-001, Rome, Italy 11/. sw. JOIIO 22. P-31018 Krak6w. Poland Ab.~(rac(: The Campo lmperatore is a virtually undrained tectonic depression located in the inner part ofthe Gran Sasso Massif. the highest rclicfwithin the Apennines (2,912 ill a.s.\. at Como Grande). LA This paper reports some major gcomorphologie featurcs of the westcrn part ofthis deprcssion. which represents :I specific and very fine: example: of glaciated mountain landscape, where landfonns typical of glacial erOSion arc commonplace over 1,800 m a.s.1. Most ofthe glacial cirques are charactcrized by kafl;tified bedrock topography, in places covered with thin drift deposits. Distinct recessional moraines are also present at various altitudes (i.e. around 2.250: 2.180: 2.000 and 1,740 m a.s.I.). However, the most typicallandfomls on the floor of the main depression are those due to glacial deposition. There. at altitudes ranging around 1.640-1.590 m a.s.1 .. stagnant ice deglaciation pauemsdominate in the form ofa widc lobate moraine system which rises 25-30 m above an outwash plain covered by glaciol1uvial.lacustrineand alluvial deposits. Within the latter. small (less than 10 m high) hills, comprising glacial drift, protrude from the flal valley floor. The remnants ofthese strongly degraded, lransfonned and laterally-eroded moraines denote the maximum extent ofan older glaciation, some 1.5 km remote from the main system. Key words: glacial morphology, stagnam ice topography. Pleistocene glaciatiOllS, Central Apennines Introduction derone glacier, which is located on the northern slope of Coma Grande (Gran Sasso Massif, Central Apennines) The cold phases ofthe Pleistocene period contrib­ between 2,867 and 2,676 m (Smiraglia & Veggetti, uted effectively to the landscape evolution ofmost of 1992) the mountain area!> of the Italian peninsula. Along the The aim of this paper is to contribute to a belln Apermines, in particular. it is possible to observe many knowledge of the effects of past cold periods In the well preserved relict landforms and deposits, typical uppennost portion of the Apennines, by identifymg ofeither a glacial environment (e.g. glacial cirques and and describing the landforms and deposits associated moraines) or a periglacial environment (e.g. rock gla­ with the glaciations which affected the Campo lmper­ ciers and stratified slope-waste deposits). atore valley (Gran Sasso Massif) during the Late Periglacial morphogenesis is still active locally at the Quaternary (Figs. 1,2,3). highest elevations (Dramis & Kotarba, 1994; Giraudi & Frezzotli. 1997; Bisci et al.. in press). while only one sma] I debris-covered cirque glacier i!> present: the Cal- 37 Carlo Bisci. Sirio Ciccacci. Francesco Dramis, Bernardino Gentili, Adam Kot8rba Description of the study area Also. strong earthquakes recorded ID adjacent areas (up to 10 MCS ID the L' Aquila basin. located The Campo Imperatore IS a wide :f\,'W-SE treading about 10-15 km to the west) clearly mdlcate the tectOniC depresSIOn located m the mner pan ofthe Gran mtensity of present-day teetomc activity (Postplschl. Sasso Masslf(2,912 m), The study area, which will be: 1985; Societa Geologlca Itallana, 1989). ThiS exten­ descnbed below, is ItS mitlal western pan. This is more slonal tectonics has been accompanied by lectomc than 13 km long and c. 4 km wide. with elevations uplift. the intensny ofWhlCh IOcreased considerably ranging from 2.494 m a.s.1. at Its northernmost end (Mt. by the end of the Lower Plelstocene. This has en­ Aqulla) to about 1,480 m a.s.!. at Its lowest point. hanced the relief by up to 1.000-1.500 m (Deman­ The present-day climate oflhe Campo lmperatore geot. 1965; Ambroseni et al., 1982: Dufaure et ar. IS charactenzed ofan average annual ramfall of 1.120 1989). mm. Wllh mlllimllffi precipitation in wmter and sum­ The Campo Imperatore depression IS partially mer (as recorded In the meteorological Slallon located filled by Quaternary deposits which. as discussed with m the study area. very close to Albergo Campo below. are pnmarily of glaciaL glaeiofluvial, allUVIal. Imperatore. at 2.138 m a.s.I.). The mean annual tem­ colluvial and lacustrine origin. The thickness ofthese peralUre IS 4,7 °C, with an annual range of monthly scdimcnts is considerable. as confirmed by a deep averages of 16.2 °C (Demangeot, 1965). The 0 °C borebole. drilled in the uppermost portion ofthe val­ mean annual temperature IS located around 2,900 m ley, which wenl through some 200 m of continental a.s.I.. close to the highest peak of the Gran Sasso sediments (Co.Ge.Far.. 1979). \rlasslf (Coma Grande. 2912 m a.s.1.). The elevation The study area represents an excellent example of ofthe \Viinn snowline was about 1.800 m. I.e. c. 1.100 claSSical glaciated mountam landscape (Klebelsberg. m lower than at present (Demangeot. 1965). 1930-31: SUler, 1939; Demangeot, 1965: Ghtseltl et The bedrock comprises of the following units al.. 1990: Bisci et al., 1993). Both erosional and (Ghlsem & Vezzam. 1986: Ghisettl er al., 1990): deposltlOnallandfonns are present. showing eVidence massive dolomltes (Lower Lias). blOclastlc grainstones ofboth Alpme glacial morphology (at altitudes above (Dogger Lower Cretaceous). marts, shales and cberty c. 1,800 m a.s.l.) and a stagnant ice deglaclauon Fig. 1. General \ ICY, 10 Campo Impe'ralore tectonic depression from easl. Como Grande (2.912 m a.s.I.) In the oock­ ground. Frontal look al Coppe di Santo Slefano ternunal mornine system mudstones (Upper Llas - Tnhoman). bloclastic mud­ pattern. characteristic ofa flat-floored topography (al stones with cherty levels (Upper Jurassic - Lower lower altitudes. along tbe valley floor). Cretaceous), pelaglc mudstones, marly mudstones and The effects ofthe two malO Pleistocene glaclauons gramstones (Upper Cretaceous - Middle Eocene), can be recognised throughout most of the investigat­ packstones and grainslOnes with marly mudstones ed area (Biscl et al., 1993; Glraudi, 1994). These gla­ (Focene - Ohgocene) and lammated marls and marly cial episodes have been distinguished by local names' mudstones (Lower-Middle MlOcene). "Piano Racollo" for the older glaciation and "Coppe The study area generally follows a monoclme dl SalJto Stefano" for the younger (Fig. 5), whIch dips gently to the northeast, even though the ovcrdll Structure IS the result ofthe tectonic superim­ pOSItion ofseveral UOllS (following a NE trend), which The Piano Racollo glaciation took placf' durmg an Upper Miocene - Lower Pliocene compressional phase (Parotlo & Praturlon. 1975: The Piano Racollo glaciation IS the oldest and most Ghlsem & Vezzani, 1990: Bigi et al.. 1991). extensive glacial phase recognised ID the Campo Durmg the Quaternary. the area was subjected to Imperatore basin. It affected nearly the whole study extensIOnal tectoDlcs (Carraro & Giardino, 1992; area. from Mt. AqUlla to the base of Mt. Bolza and Jaurand. 1992; Giraudi, 1994) which produced sys­ Mt. MutTl. Most of the glaCial clrques produced dur­ tems ofnonnal faults. most ofwhIch trend ENE-WSW 109 thiS phase have substantially been reworked by the and whIch border the Gran Sasso Massifon its south­ glaCIers of the most recent glaCiation. But on the ern margins. This tectonic phase, which has contrnued wanner southern slopes and west-facmg slopes ofMt up to the present, has resulted in a progressive low­ Prena, an old glacial cirque IS present which was not ering of the central portion of the basin with respect reacuvated during the last glaclallon and which was to the surrounding ridges. strongly affected by both linear erosion. and. subordi­ On the slopes. present-day tectomc activity is in­ nately, by debris flows. During thiS ancient glaCiation. dll.:31Cd by the presence ofspectacular triangular fac­ the maximum length of the glacier was at least 12.5 ets, fresh scarplets and intense badland-like erosional km and its Width at the deposiuonal zone was c. 3 km. Fig. 2. The uppcnnosl reach of Campo Impcrlltorc, lllndforms lypical of glacial ero~ion below Ml. Aquila. Wllhin phenomena. the last of which affect brecciated dolo­ The glacial advance that produced the most extended glacial cirquc karstificd bedrock lopography \\ Ilh Ihin drift deposits_ mites. Locally, these faults also cut Late Quaternary glaCial limit was reconstructed mainly on the basis of deposits (stratified slope-waste deposits and alluvial the distribution oferratic boulders and small moraine fans) (Fig. 4). remnants. 38 ~ ~ ~ ~: ~ -,n~. ~ -:::I:rgb" - ~ • - g i ~ ~~ a. ~ , < • " ~.~. ~ c ':: ~ , a = ~ ;>:::'1~ f ·• •=~ --;:. $l " ,~ g. ~.. ·8.~~ ~ ;:; iJ ~ :::: a.~ I od .. - 0 ~ =. ~• • 3 .-c -§ Ho s -:;t>2.- r) ~ =c "g ~ :!! ~ <l '• • ·~ ~ .. ~, ,'" 3e: ~ . ~ e ~ •", ·~ -~ ~ l;- ~[. ~. ~o ·9 [~.- Legend 1 _2 _3 _4 Mt. della _5 Sclndarella _6 2233 _7 Vldo dl Corno, 1924 _8 Mt. Brlncastetlo 2386 _9 _10 s N _11 _12 Mt. Prenl, 2561 _13 _14 _15 _16 _17 Mt. Bolza, 1899 "'11;. ~. Inlerpn.:lali~e Ihree-dimcn~l(1Il:11 block dlagmm of lhc arca. Legend: I - congllltllemrc~: 2 slope debris: J alluvial fan: 4 .I!laCIOnUVHII deposlls; 5 _ lal:U~lrine depo~it~: 6 Ouvio·I;lclIslrinc deposits: 7 - della. K glllcmflllvia] elongared hill; 9 rock glacier: 10 PlIlllO Racollo moraine: 11 _ 14.COllPC dl SlInlo SIc/hno temlinal tllllflllllCS (MICl:CS~IVC sHlges): 15 -lalcralll1omlnc: 16 ancien I ermlcu moraine; 17 - glacial dnn. LJ'- Lago Pielranzoni (lake). The extent of Pfeistocene gJaciations in the western part of the Campo Imperatore..
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