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 ~ :!! ~ 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... The southwestern maximum lateral extension of The Coppe di Santo Stefano glaciation the Piano Racollo glaciation is denoted by erratics deposited on the glacially-polished limestone hills of The more recent Coppe di Santo Stefano glaCia the Maniere valley. These boulders are mainly com· tion is characterised by extensive and well-preserved posed ofwell-cemented conglomerate (breccia), sim terminal (and. subordinately, lateral) moraines. which ilar to that constituting the glaciated valley noor in show a distinctive morphology. These glacial features the upper section of the depression (at altitudes rang differ significantly from those of the Piano Racollo 109 between 1,660 and 1,900 m a.s.I.). The less glaciation, especially in respect oftheir freshness. The common red limestone erratics are also good indica maximum extent of the glacier is clearly marked by tors of long glacial transportation, since this litho the sharp morphological contrast between ItS moram type crops oul only close to the western end of the ic system and its outwash plain (Fig. 6). main watershed. The most conspicllous features in the main valley A rather well-preserved lateral moraine system, depression are landforms of glacial deposition. In which has locally dammed minor side valleys (there altitude, these range from 1,640 to 1,590 m a.s.1. A by causlllg lacustrine deposItion) is a further feature stagnant ice deglaciation pattem is dominatand. This ofthc southemwest margin ofthe Campo Imperatore. has the form of a c. 2.5 km wide lobate moraine A small glaciofluvial delta produced by water flow system, rises 25-30 m above the surrounding plain. mg from the ice mass, which still eXists in one ofthese Within this widespread outwash plain, formed by small basms. provides evidence for this. glaciofluvial water, braided paleochannels show a well In Piano Racollo, only small patches of moraines preserved braided river pattem. (often strongly remodeled) are still recogmzable within The morpholob'Y ofthe area affected by the Coppe the ounvash plain. di Santo Stefano glaciation suggests that most of the Along the southern side of the valley, at the base ice entered the central depression from the north-west of the Cima di Mt. 801za. remnants of the older gla (glacial cirques of Mc Aquila, Mc della Scindarella Ciation are represented by narrow shelves of glacio and Mc S. Gregorio di Paganica) and then flowed Ouvial scdm1ents, formed as ice-contact deposits. The southeastwards, along a relatively narrow (ca. 1 km Fig. 6. Aerial phologmph Gcntred 011 the Coppe di Santo Slcfano area where typical stagnant ice dcglaci glacial/glaciofluvial ongin of these deposits is con wide) valley section between Mc S. Gregono di Pa alion patterns are clearly visible. fioned by both the abundanl.:C ofwarser scdimcnts and ganica and Mt. Brancastello. Minor lateral glaCIal the presence WIthin these terrace-like features ofbad valleys and cirques generally show bedrock topogra Iy preserved dead-ice hollows. phy, only locally being covered by poorly developed In the same area, a small hill composed of non recessional moraines. soned, sharp-edged boulders and cobbles with The glacial erosion scarps present on the slopes of a sandy-silly matrix protrudes about 10 m above the Mc S. Gregorio di Paganica suggest that the ice body nearly flat valley bonom (outwash plain). The very was at least 250 m thick. On reaching the Coppe di gently undulating or planar crest of the hill. which is Santo Stefano area, the valley glaciers coalesced to Interpreted as a remnant ofa moraine, shows evidence form a 2.5 km widc piedmont-like glacier. of creep and solltluction processes. Supraglacial sediments (10-20 m thick) deposit To the northwest. the limit ofglacial deposition has ed during the more recent glaciation have been affect not clearly been defined, since glacial deposits have ed by differential ice melting. This has resulted 111 been buned by very large coalescent alluvial fans, spectacular topographic irregularities, well visible both which have probably been active during the whole in the field and on aIr photographs (Fig. 6). This mor· tltnespan from the end of this glacial period 10 the phology is similar to tbe so-called "karst topography present. Only a very small morainic hill protrudes on stagnant glaciers" described by Clayton (1964) and Immediately to the west of the huge fan which bor Clayton and Moran (1974). ders the western slope of ColJe Paradiso. In the area immediately behind this terminal mo The Piano Racollo glaciation also produced gla raine system, comprising of partially coalescent mo clOOuvlal and glaclOlacustrine sedimell1s. These de rainic arcs which were deposited during successive posits form an elongated hill (1,567 m ao5.l.) which stadial periods, older glacial sediments have been found IS elevated a few meters above the valley noor and to be partially covered by younger ones. Close to the consists of well-rounded cobbles and pebbles In Lago di Pietranzoni, there IS a small patch of ancient a sandy-silly malnx. ThiS land form (interpreted as till, which has been overridden by the younger ice body an esker) still shows a weJl-defined morphology with and fossilised by supraglacial deposition. In the same relatively steep sides. and trends parallel with the area, moderately thick fluviolacustrine deposits have Fig. 11. SOlllh-facing ,lopes of /1.11. I:3runeastdlu and Ml. Pn:na st~ongly modified by water erosion and periglacial pro reconstructed ice now dlTection. cesses. BdWeen Ill()raine topography of Sa1110 Stefano GlacIatIOn (frontal part of the phOIO) and rocky slopes, co infilled older depressions in the previous topography, al~,dng alluvial fans constitule Ihc Illo-t ,peetacular landfofllls at Campo llllp~ratorc. so producing a flat plain. Distinct recesSional moraines are also present at various altitudes. At least four main 39 Carlo Bisci, Sirio Ciccacci, Francesco Dramis, Bemardino Gentili, Adam Kotarba The extent of Pleistocene glaciations in the western part of the Campo Imperatore ... stadials are recognizable in the valley (i.e. close to well preserved at an altitude of about 1,900 m a.s.1. cia. Loose erratics, either of limestone or conglomer· oldest glaciation extended down to about 1,550 m a.s.1. 2,250: 2.180; 2,000 and 1,740 m a.s.I.). on the western side ofthe valley. According (0 Girau ate. are locally present. but a continuous ground By contrast. the limits ofthe less-extensive glaciation As indicated by the small delta constructed by a di & Frezzotti (1997) there are at least three gener moraine IS absent; lateral moraine is discontinuous, it have been very well defined by its distinct morame stream which fed a minor depression dammed by the ations ofrock glaciers in the Campo Imperatore. They IS mostly present on the right-hand (southern) side of pattern, typical of a supraglacial morphology, which main moraine, the mort recent glaciation also pro were distinguished by both absolute and relative dat the main valley. reached c. 1,589 m a.S.I. (i.e. it extended for about 1.5 duced minor Lacustrine basins. ing and pedogenetic condition of these features. Unit 3 - Flat-floored valley bottom: this is filled km less than the older one). Because deposits correLated to the "Tufo Giallo Coalescent alluvial fans and composite debris flow with generally non-cemented fluviolacustTine sedi Taking into account the geomorphological position Napoletano" volcanic episode rest on the glacial drift cones are the most spectacular landfonns in the Cam+ ments (locally covenng older glacial deposits) and is and freshness ofthe Coppe di Santo Stefano terminal (Frezzoltl & Narcisi, 1989; Carraro & Giardino, po Imperatore; they cover large areas between the present in the internal pan of a distinct moraine sys· moraine, the glacial phase responsible for its deposi· 1992). the Coppe di Sanlo Stefano glaciation must steep, mainly south·facing slopes and t:le drift-filled tern (UnJl 4) at an altitude of c. 1.640 m a.s.l. tion might reasonably be correlated to the Wurm III have culminated before 13,000 yr. B.P. valley floor. thereby fossilizing the glacial depositional Unit 4 - The moraine system of the Coppe di stage (pleniglacial) which occurred in the Apennines. Periglacial processes (more common along the landfonns (Fig. 8). The alluvial fans were fonned Santa Stc-fano: this well·preserved arcuate and corn· as elsewhere in continental Europe (Wi.inn). from northern slopes of the valley) were partially simulta during the Late Pleistocene, possibly during the sec plex moraine system, deposited during the more recent 21,000 to 18,000 years B.P. (Federici, 1979a). In fact. neous with the glaciation and strongly affected the area ond glacial phase, as testified by 14C dating of pa glaciation. dominates in the intcnnediate portion ofthe these glacial deposits are partly covered by the "Tufo after the Ice retreat. In fact, since the broad valley leosoils included within an alluvial fan located in the valley floor and features a spectacular stagnant ice Giallo Napoletano" which is dated c. 13.000 years RP. depression ofthe Carnpo Imperatore was never com eastern pan of the Campo Imperatore (Frezzoni & deglaciation pattern. (Frezzotti & Narcisi. 1989). By contrast. according to pletely filled by the Pleistocene ice body, the surround Giraudi. 1990). Unit 5 ~ The foreland of the moraine system of paleoclimatic reconstruction elaborated by Giraudi ing mountain slopes. mainly comprising lectonically Geomorphological studies by Giraudi (1994) show Coppe di Santo Stefano: this is characterized by an (1989) for the neighbour Fucino Lake area (some 30 fragmented calcareous and dolomitic rocks, were that alluvial fans have been developed in five phases. outwash plain correlated with the younger moraine km to the south. at an aJtitude ofabout 650 m a.s.I.). widely affccted by geomorphic processes typical ofthe the last related to the present day alluviation ofthe area. system. Within the latter, small hills protruding from the last period with a damp-cold climate in the Ap periglacial environment. In such an environment, on the surface have been interpreted as the remnants of enmnes was between 24,000 and 20.000 years B.P. south-facing slopes, huge amounts of frost-shattered the moraine system created during the older glaciation. Thus, the receSSional moraines recognized in the area matenals were produced. The presence ofan abundant Geomorphologic units recognized The lauer was strongly eroded and reduced during the may reasonably be referred to the Late Wunn degla amount of water shifted the freshly-produced debris more recent cold phase. The maximum extent of the ciation, since it is probable that only at higher altitudes and converted it into stratified slope·waste deposits Links between the two glacial phases (and related Plano Racollo glaciation is marked both by erratics did a few small cirque glaciers (such as the still ac (grezes Iitees). More ancient stratified slope·waste landforms) described here can be observed within the and small moraine remnants, the latter being located tive Calderone glacier) survived during the Holocene depoSits, well cemented by pedologic processes in their framework ofseveral geomorphologic units (Fig. 7). at a distance of about 2 km from the slopes of Mt. (Federici, 1979a). uppernlOst pan, are present at the base of the nonh Unit I- Glacial erosion landscape with hanging Bolza. The most recent results of studies by Giraudl and eastern slope of the valley. These deposits, which valleys: this is frequent at altitudes higher than ca. Frezzotti (1997) in these areas have dated the max locally show evidence of having been affected by 1,800 m a.s.l., where the floors of glacial cirques are imum extent and Late Glacial stadial phases. In the recent tectonic activity (Carraro & Giardino, 1992), characterized by the presence ofeither poorly devel Discussion and conclusions Campo Imperatore, the last maximum advance was are tentallvely attributed to the Middle Pleistocene. oped recessional moraine systems or occasional gla probably reached c. 22,680±530 yr B.P., and the major After the retreat of the last ice body, the upper cial erratics on a karslified bedrock topography. Geomorphologic field works recently carried out glacier retreat began c. 21,000 yr S.P. According to portion of the main valley was strongly affected by Unit 2 - Erosional morphology ofglacial valleys: In Campo Imperatore. have demonstrated that the these authors, the glaciers (with the exception of periglacaal morphogenesis. A relict rock glacier (Ghi· this may be recognized at an altitude ranging from glacial landfonns there are related to two separate Calderone Glacier) had disappeared at the beginning seui er aI., 1990; Dramis & Kotarba, 1994) is fairly 1,850 to 1.660 m a.s.l., mainly on outcrops of brec- glaciations (Bisci Cl 01.,1993; Giraudi, 1994) and not of the Holocene. to the single phase recognised by Demangeot (1965). No chronological data are available on the age of The relative sharpness and freshness ofthe landfonns the older glacial deposits. Immediately adjacent 10 the w'- aSSOCiated with the more recent glacial period, the study area, volcanic ash dated at 460.000 years RP. -- E distance ~f different terminal deposits from glacial underlies deposits which have bcen interpreted as cirques. Ihe degree of soil development and the glacial by Carraro & Giardino (1992). Since the gla hthological composition of sediments, are all insis· cial expansion occurring during Wiirm TT! (Le. the tent that the area has been affected by at least [WO glaciation responsible for the emplacement of the "" major glaciations. Funherrnore. it is clear that the Coppe di Santo Stefano moraine system) was the J"OO more recent one was significantly less extensive than largest ever recorded for the Late Pleistocene (80ul Its predecessor. too et al., 1985: Dawson, 1992), it seems reasonable Okm1 23 5 6 7 • • • " The maximum extent of the first glacial phase to correlate the glacial deposits present in Piano IL---,I__ ~2 -'---=---'-3 __---"------''-----_5 I I • (Piano Racollo glaciation) is not clearly defined ow Racollo to the last cold stages of the Middle Plc IS -_-_c :.:':, , -:-=-" """-. Ing to tbe scarcity of related moraines. Glacial dep tocene ("Riss" Auct.) (Federici, 1979b). This chrono --. to -- ositional features relating this have effectively been logical reference is consistent with the recognition of Fig. 7. SchematIC cross section along the main valley. showing the principal geomorphologic units (numbers I to 5 in the bar below removed by the proglacial waters of the second gla· pre-Wiirm glacial landfonns and sediments in other the: section indicate the approximate extension of each unit: for their description refer to the text). SG and RG resp<:ctively indicate ciation and have often been concealed by the large parts of the Abruzzi Apennine (Demangeot, 1965; the maximum extension of the Coppe di Santo Stefano and the Piano Racollo Glaciation. Legend: a - moraine (Piano Racollo glaCiation); b ~ moraine (COPflC di Santo Stefano glaciation); c - gllldofluvial deposits (Coppe di Santo Stefano glaciation); d alluvial fans which are widespread at the base of the Pfeffer, 1967; Cassoli et al., 1986; Societa Geologica nuviolucustrine deposits (Coppe di Santo Slefano glaciation); e - glacial erntics on bedrock topography (Coppe di Santo Stefano mountains bordering the depression. On the basis of ltaliana, 1989) and, further north, in the Umbro glaciafion); f - well cemented conglomerate (breed.), eroded by glaciers; g - recessional moraine (Late Glacial): h -lateral moraine the distribution of erratics and small remnants of Marchean and Tuscan·Emilian Apennines (Dramis et (Coppe di Santo Stefano glaciation); i - outwash plain (Coppe di Santo Stefano glaciation). moraine deposits, it has been determined that the aI., 1980; Federici & Tellini, 1983). 40 41 Carlo Bisei, Sirio Ciecacci, Francesco Dramis, Bemardino Gentili, Adam Kotarba The extent of Pleistocene glaciations in the western part of the Campo Jmperatore ... Italy) - A review. Palaeogeography, Palaeoclima~ Pfeffer, KH., 1967: Bcitriige zur Geomorphologie der Acknowledgements Clayton, L. & Morao, R.S., 1974: A glacial process form model. In: Glacial Geomorphology, Bingham wlogy. Palaeoecology 70: 249-260. Karstbechen in Bereiche des Monte Velino (Zentral ton Symposia Series. 89-119. Glfaudi, c., 1994: Elementi di geologia del Quater apennin). Frankfllrter Geogr. Hefle 42: 85 pp. The authors wish to thank C. Di Nisio, C. Ginni Co.Ge.Far., 1979: Gran Sasso; il traforo autosrradalc. nano della piana di Campo Imperatore (Gran Sas Postpischl. D. (ed.), 1985: Catalogo dei terremoti Cl. C. Maineri, L. Papini, E. PetrilJi. A. Pettini. R. A.N.A.S., Roma, 463 pp. so d'ltaha). Aui Tlcinesi di Scienze della Terra, italiani dall'anno 1000 al 1980. C.N.R.. Pmgetlo Rlghetti. C. Romagnoli. A. Smisi and S. Tatoni for Dawson, A.G., 1992: Ice age earth. Routledge. Lon serie speciale 2: 137-143. Finalizzato "Geodinamica", 239 pp. their fundamental help in the field surveys. don and New York, 293 pp. Giraudi. C. & Frezzotti, M., 1997: Lale Pleistocene Smiraglia, C. & Veggeui, 0., 1992: Recenti osservazi· The present work has been carried out within the Demangcot. J., 1965: Geomorphologie des Abruzzes Glacial Events m the Central Appennines, Italy, oni sui ghiacciaio del Calderone (Gran Sasso framework of a research programme on glacial and Adriatiques. Memoires et DOCllments, CNRS, 403 Quaternary Research 48: 280-290. d'Italia, Abruzzo). Holletino Societa Geografia periglacial geomorphology ofthe Central Apennines, pp. Jaurand, E.. 1992: Les moraines failles du Gran Sas Iraliana, serie Xl, 9: 269-302. 1Ovolving the Department of Geomorphology and Dramis, F.. Coltorti, M. & Gcntili, B., 1980: Glacial so d'ltalia (Apennin Abruzzais): interct geomor Societa Geologica Italiana, 1989: Elem-;nti di tenon· Hydrology of the Polish Academy of Sciences and pcriglacial morphogenesis in :he Umbria phologique Cl neotcctonique. Ceogr: Phis. Enl'iron. ica pliocenico-quatemaria cd indizi di sismiciui 010 (Krak6w) and the Departments of Earth Sciences of Marche Apennines. Abstracts, 24th International 44, 10-29. cenica nel1'Appcnnino laziale abruzzese. Guida both the University ofCamerino, and the First and thc Geographical Congress, Tokyo, 1: 114---115. Klebelsberg von R., 1930-31: Die eiszeitliche all"escursione, 31 maggio - 2 giugno 1989, eN.R., Tlmd University of Roma. Dramis, F. & Kotarba, A .. 1994: Geomorphological Vergletscherung der Apennines. I Gran Sasso Centro di Studio per la Gcologia Tecnica evidences of high mountain permafrost in Central Maiella. Zeirschriftf Gletscherkunde Glazialgeol E.N.E.A.-P.A.S., Laboratorio di Geologia Applicata Apennines. Geografia Fisica Dinamica Quaterna ogie 18: 141-169. alla Sismoteuonica, 129 pp. References ria 17: 29-36. Parouo, M. & Praturlon, A" 1975: Geological sum Suter, K., 1939: Die eiszeitliche Vergletscherung des Dufaure, J.• Bossuyt, D. & Rasse, M., 1989: Criteres mary of the Central Apennines. QlIaderni della Zemralapennins. Vierteljahrsschrift de,. Nalllrfor Ambrosetti. P., Carraro, F., Deiana, G. & Dramis, F., geomorphologiques de neotectonique verticale dans Ricerca Scientifica 90: 257-311. schenden Gesel. Zurich, 140 pp. 1982: 11 sollevamento dell'ltalia centrale Ira il Pleis I'Apennin Central Adriatiques. Ass. BIIII. Franc. £1. toccne inferiore e il Pleistocene medio. C.N.R. Quat. 2: 151-160. Proget!o Finalizzato "Geodinamica", Contributi Federiei, P.R., 1979a: Una ipotesi di cronologia gla Concluslvi per la Realizzazione della Carta Neotet ciale wiirmiana, tardo e post-wiirmiana nell'Appcn tonica d'Italia 2: 219~223. nino Centrale. Geografia Fisica Dinamica Qualer Bigi, S., Calamita, F., Centamore, E., Deiana, G., naria 2: 196-202. Ridolfi. M. & Salvucci, R. t 1991: Asseno struttur Federici, P.R., 1979b: On the Riss Glaciation of the ale e cronologia della deformazione della "zona Apennines. Zeilschriftf Geomorphologie, N.F., 23: d'IDcontro" tra le aree umbro-marchigiana e laziale 106-111. abruzzese (Marche meridionali e Lazio-Abruzzo Federici. P.R. & Tellini, c., 1983: La geomorfologia seucntrionali). StlIdi Geologici Camerti, special dell'alta Val Parma (Appennino Senentrionale). RiI'. Issue 1991/2, CROP 11: 21-26. Geografica ltaliana 80(3-4): 393-428. B1SCI, C., Ciccacci, S., Dramis, F., Gentili, B. & Frezzoui, M. & Giraudi, C, 1990: Sedimenti calici Kotarba, A., 1993: Glaciated valley land system of tardopleistocenici ed olocenici nell'Appennino Ccn Campo Imperatore, Gran Sasso (Central Italy). Pro tralc. Memoire Societa Geologica ltaliana 45(2): gramme with Abstracts, Third International Geo 836-883. morphology Conference, August 1993, Hamilton Frezzotri, M. & Narcisi, B., 1989: Identificazione cll (Canada): 103. un andosuolo, possibile livello guida per la crono Bisci, c.. Dramis, F.. Fazzini. M. & Guglielmin, M. (in stratigrnfia olocenica dell'Appennino centrale. Mem press): Climatic conditions and sporadic permafTost orie SocietQ Geologica Ilaliana 42: 351~358. ID the Maiella massif (Cemral Apennines, Italy). Ghisetti, F. & Vezzani. L.. 1986: Carta geologica del Geografia Fisica e Dinamica Quatemaria. vn Con Gruppo M. Sella - M. Camicia - M. Prena - M. vegno Glaciologico Italiano. Bonnio, sept. 1999. Brancastello (Gran Sasso d'!talia, Abruzzo). Boulton, G.S., Smith, G.D.. Jones, A.S. & Newsome, S.EI.Ca., Firenze. J.. 1985: Glacial geology and glaciology ofthe last Ghiselti, F. & Vezzani, L., 1990: Stili strunurali nei mid-latitude ice sheets. Journal Geological Soci sistemi di sovrascommento della cat-:na del Gran ery, London. 142: 447-474. Sasso (Appennino Centrale). Studi Geologici Cam Camro, F. & Giardino, M., 1992: Geological evidence erri, special volume 1990: 37-50. of recent fault evolution. Examples from Campo Ghiscni, F., Vezzani. L., Blumetti, A.M., Cellini, M.. Imperatore (L'Aquila - Central Apennines). 11 Centamore, E., Pinori, C. Ridolfi, M., Frezzoni, M.. Quaternario 5: 181-200. Giraudi, C., Clari, P., Bruzzone. B., De La Pierre, Cassoli, A., Carda, L., Lodoli, C, Malatesta, A., F. & Bigozzi, A., 1990: Carta Geologica del Gran Malaroni, MV & Ruggeri, A., 1986: Il glacialismo Sasso d'ltalia da Vado di Como al Passo delle Ca quatemario del gruppo Velino-Ocre-Sirente. Mem panncHe. S.EL.CA., Firenze, Studi Geologici Cam· one Sociera Geologica IlaUana 35(2): 855-867. erti, special issue 1990. Clayton, L., 1964: Karst topography on stagnant gla Giraudi, C, 1989: Lake levels and climate for the laSi ciers. .Journal of Glaciology 5(37): 107-112. 30000 years in the Fucino area (Abruzzo ~ Central 42 •• 43