D07_copertina_R_OK C August 20-28,2004 Florence -

Field Trip Guide Book - D07 During-Congress L. Ferreli,Guerrieri,Serva Associate Leaders: C. Carrara Leader: S. FRANCESCOD’ASSISI BASIN AND THE RIETIINTERMOUNTAIN 32 Volume n°3-fromD01toP13 GEOLOGICAL CONGRESS nd INTERNATIONAL D07 24-05-2004, 14:02:32 The scientific content of this guide is under the total responsibility of the Authors

Published by: APAT – Italian Agency for the Environmental Protection and Technical Services - Via Vitaliano Brancati, 48 - 00144 Roma - Italy

Series Editors: Luca Guerrieri, Irene Rischia and Leonello Serva (APAT, Roma)

English Desk-copy Editors: Paul Mazza (Università di Firenze), Jessica Ann Thonn (Università di Firenze), Nathalie Marléne Adams (Università di Firenze), Miriam Friedman (Università di Firenze), Kate Eadie (Freelance indipendent professional)

Field Trip Committee: Leonello Serva (APAT, Roma), Alessandro Michetti (Università dell’Insubria, Como), Giulio Pavia (Università di Torino), Raffaele Pignone (Servizio Geologico Regione Emilia-Romagna, Bologna) and Riccardo Polino (CNR, Torino)

Acknowledgments: The 32nd IGC Organizing Committee is grateful to Roberto Pompili and Elisa Brustia (APAT, Roma) for their collaboration in editing.

Graphic project: Full snc - Firenze

Layout and press: Lito Terrazzi srl - Firenze

D07_copertina_R_OK D 24-05-2004, 14:04:14 Volume n° 3 - from D01 to P13

32nd INTERNATIONAL GEOLOGICAL CONGRESS

THE INTERMOUNTAIN BASIN AND S. FRANCESCO D’ASSISI

AUTHORS: C. Carrara1, L. Ferreli2, L. Guerrieri2, L. Serva2 1 c/o IGAG - CNR, Roma - Italy 2 APAT - Italian Agency for Environmental Protection and Technical Services, Roma - Italy

Florence - Italy August 20-28, 2004

During-Congress D07

D07_R_OK A 24-05-2004, 13:46:12 Front Cover: Geological landscapes and Franciscan sanctuaries in the Rieti basin

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Leader: C. Carrara Associate Leaders: L. Ferreli, L. Guerrieri, L. Serva

Introduction Field map references This fi eld trip is aimed at showing the Quaternary In this guidebook we will refer to the following evolution of the intermountain Rieti basin (Central geological maps: Apennines) under extensional tectonics, climatic - Carta Geologica d’Italia (scale 1:100,000) variations and human activities. The interaction Sheet 138 “” , Servizio Geologico among these factors during the Quaternary triggered d’Italia, 1970; continuous and fast landscape modifi cations, such - Carta Geologica d’Italia (scale 1:100,000) as the Holocene fi lling of the Rieti basin (up to 50 Sheet 139 “L’Aquila”, Servizio Geologico meters) or the almost complete receding of the Lacus d’Italia, 1955; Velinus (a lake larger than 90 km2) under the Roman - Cavinato G.P.: Geological map of the draining work. Southern Area of the Rieti Basin (Central The singularity of the natural landscape, Apennines), scale 1:50,000, CNR, Centro di characterised by Le Marmore Falls and other Studio per la Geologia dell’Italia Centrale, geomorphic features (fl uvial terraces) shaped by , 1991; travertine deposition, attracted human settlements - Cosentino D., Parotto M., Scrocca D. & since at least the Bronze Age. Moreover, the Vecchia P.: Carta geologica della media presence of the places where S. Francesco d’Assisi valnerina (), scale 1:25,000 Università lived and prayed enhances the magnifi cence di Roma Tre, Dipartimento di Scienze (spirituality) of the area. Geologiche, Rome, 2000; The itinerary will provide the basic elements for - Guerrieri L., Comerci V., Ferreli L., Pompili comprehending the role played by natural and human R., Brunamonte F., Michetti A.M. & Serva L.: factors in the geomorphological evolution of the Rieti Geological mapping of continental deposits in Basin, a special area for its spirituality as witnessed the Rieti Basin and surrounding areas (Central by the presence of four important Franciscan Apennines, Italy): a tool to compare past, sanctuaries. present and future evolution of intermountain basins, in press, Atlante di Cartografi a The trip will start at the base of Le Marmore Falls Geologica - 32nd IGC Florence 2004. where the river fl ows into the river (stop 1). We will focus on the climatically-controlled Regional geologic setting growing and downcutting of the travertine dam during Regional geologic framework the Holocene and the role of reclamation work and (see fi eld map references) other human activities regulating water discharge at The Rieti basin (fi g. 1) is a typical intramontane Le Marmore in historical times. depression of the Apenninic chain (Accordi and Then the itinerary will go upstream in the Velino Carbone, 1988; Cosentino et al., 1992). It is fi lled valley and enter the Rieti Basin. After a quick look with continental Plio-Quaternary sediments made up at the geomorphological (Piediluco and Ventina of conglomerates, sands, silts and travertine deposits ancient shorelines) and Upper Pleistocene-Holocene that reach a thickness of 400-500 m (Manfredini, stratigraphic records (Lago Lungo and Ripa Sottile 1972). high-resolution record) of Lacus Velinus, we will The origin and evolution of the Rieti basin is related visit the Franciscan Sanctuary of to the post-collisional extensional tectonics that have (stop 2). strongly affected this sector of the Apenninic orogenic DO1 to P13 n° 3 - from Volume After lunch, the trip will move SE in the middle belt since the Pliocene (Patacca et al., 1990; Doglioni, Velino valley, between and Rieti (stop 1993; D’Agostino et al., 2002). 3), where Middle Pleistocene travertine barriers and During the Late Pliocene-Early Pleistocene period lacustrine and fl uvial terraces are preserved. (“Villafranchian” age Auct., according to the The trip will end at Greccio, on the western slope of historical name of the typical Upper Pliocene-Lower the Rieti basin where, during Christmas Eve of 1223, Pleistocene continental facies in Italy), the Rieti basin S. Francesco set up the fi rst representation of the Holy developed in the hangingwall of the SW-dipping, crib. NW-trending, Rieti fault segment (Cavinato et al.,

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Volume n° 3 - from DO1 to P13 D07 - D07 Leader: C.Carrara Age); 10.LocationofRipasottileandLagoLungoboreholes faults; 6.Normal7.Normal-oblique8.Shore-lines(fi (Late Pliocene-MiddlePleistocene).4.Mainlycarbonaticunitsofthe“ sequenze”(Meso-Cenozoic);5.Thrust deposits (UpperPleistocene-Holocene);2.Travertines (Middle Pleistocene-Holocene);3.Fluvio-lacustrinesediments Figure 1-Geologicalsketch oftheRietiBasin(fromRicci Lucchi etal.,2001).Legenda:1.Fluvio-lacustrineandfan rst-Iron Age); 9.lacustrinebeach deposits(fi 24-05-2004, 13:49:10 rst Iron THE RIETI INTERMOUNTAIN BASIN AND S. FRANCESCO D’ASSISI D07 Volume n° 3 - from DO1 to P13 n° 3 - from Volume

Figure 2 - Landscape evolution of the Rieti basin in four scenarios (a, b, c and d) since the Late Pliocene.

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Volume n° 3 - from DO1 to P13 D07 - D07 Leader: C.Carrara thresholds grew up,controlledbyalternating erosional the courseof Velino river numeroustravertine Since theMiddlePleistocenetoPresentalong 2b). divided theancientbasininhorst andgraben(fi Rieti basinnew normalfaults trending N-SandE-W Stoppa & Villa, 1991;Laurenzietal.,1994).Inthe local volcanic districts(Cupaello,Gragnani,1972; north. Ultrabasicvolcanic activity occurredinsmall Michetti etal.,1995)andthe Velino river diverted in the Terni andRietiareasrejuvenated (Raffy, 1983; environment, the“Villafranchian” drainagenetwork were activated. As aconsequenceofthisextensional 1993), includingtheRietibasin,andnew normalfaults uplift affected awidesectorofCentralItaly(Dramis, At theendofEarlyPleistocene,aregional tectonic Velino systemwas stilldrainingSSE. the paleo-Nerariver migrated WSW whilethepaleo- SSE (paleo-Nera-Velino rivers). Intheyoungerone one (fi of two different stagesinthisperiod.Intheolder surfaces, windgaps)clearlysupportsthehypothesis Geomorphic andstratigraphicevidence (erosional al., 1989;BarberiandCavinato, 1993). fan-delta andfl the basinandconsistofconglomeratessandstones crop outinthesouthern,easternandnorthernpartsof Late Pliocene-Lower Pleistocenecontinentaldeposits Landscape evolution oftheRietibasin successions intheLeonessabasin(GEMINA, 1963). 1995; Basilici,1997),andbylacustrinemarshy (“Lago Tiberino” basin, Auct., Ambrosetti etal., lacustrine andfl of thickbasinfi 1991). These normalfaults forcedthesedimentation basin(Leonessafault, Michetti&Serva, NW-trending segment causedtheformationof the easternslopeofMt. Terminillo, aNE-dipping, fault segment, Brozzetti&Lavecchia, 1995). Along trending segment generatedthe Terni basin(Martani Some kmtoNWoftheRietibasin,aS-dipping,E- 6.5) occurredbetween5000and6400BP. capable ofproducingsurface faulting (magnitude> 1995). According tothesestudies,thelastearthquake (Piedicolle, LaCasettaandCaporio,Michettietal., shown bypaleoseismologicalanalysesinthreesites in Middle-LatePleistocenetoHolocenetimeas about 100kmlong. The Rietifault hasbeenactive normal fault systemintheCentral Apennines, north-western extension ofaprimarysegmented 1989; Michettietal.,1995). This segment isthe g. 2a)asingledrainagenetwork was directed uvio-lacustrine sediments(Cavinato et uvial sequencesinthe Terni basin lling successions,characterizedby g.

1938; Lorenzetti,1989;Leggio andServa, 1991). acquired itspresent-daycondition(Duprè-Thesedier, last century, theplainwas completelydrainedand the wholealluvialplain.Finally, inthethirties ofthe 1990; Ferrelietal.,1992),thatoccasionallycovered of theso-called works causedchangesinthelevel andextension control ofthemainstreamswater regime. These cutting ofLeMarmorethresholdandthepartial processes. The mainevidence ofthisistheartifi a signifi Moreover, fromatleasttheRomanagetoPresent, alluvial plain(sixthterraceorder, fi travertine barrierandupstreamthepresentRieti of climatecausedthegrowing oftheLeMarmore the Rietibasin(fi and deepvalleys andcanyons formedupstreamin (LGM) theMarmoretravertine barrierhasbeencut 70÷30 kyrs inage.DuringtheLastGlacialMaximum the fourthoneisabout400kyrs old,whilethefi three ordersofterracesareolderthan400kyrs B.P.; Six ordersofterraceshave beenrecognized. The fi 1993). and ages(Brunamonteetal.,1992;Ferreli the determinationoftheirdepositionenvironment these terracesandtheirradiometricanalysesallowed 1993). Detailedstudiesofthesedimentsforming present aretestifi lacustrine basinsalongthe Velino valley thatat thresholds upstreamcausedtheformationoffl The evolution oftheabove-mentioned travertine the erosionoftravertine barriers. circulation ofCa-richwaters andconsequentlycaused cooler climaticphases,onthecontrary, reducedthe during humidandtemperateclimates.Drier and sedimentaryphases. Travertine depositedmainly round himthe12discipleswhobecameoriginal restoration ofdilapidatedchurches.Hegathered charity amongthelepersandbegan working onthe Back in Assisi in1205,heperformedactsof he resolved toalter hisway oflife. imprisoned, hesuffered asevere illnessduringwhich he was heldcaptive inPerugiaforover ayear. While life. Following abattlebetween Assisi andPerugia, a youngman,S.Francescoledworldly, carefree even thoughhisfather was awealthymerchant. As He appearstohave received littleformaleducation, S. Francesco(1182-1226)was bornin Assisi (Umbria). S. Francescod’Assisi A shortbiography of cant anthropicactivity superimposednatural ed byrelictterraces(Carraraetal., g. 2c). The Holoceneamelioration Lacus Velinus (Verri, 1883;Segre, g. 2d). 24-05-2004, 13:48:41 uvio- fth is cial rst THE RIETI INTERMOUNTAIN BASIN AND S. FRANCESCO D’ASSISI D07

brothers of his order, later called the First Order; they connected to the geomorphic evolution of the elected Francesco superior. river, and by the E-W trending Martani normal fault, In September 1224, after 40 days of fasting, Francesco that borders the northern slope of the Terni basin. was praying upon Monte Alverno when he felt pain mingled with joy, and the marks of the crucifi xion of Stop 1: Christ, the stigmata, appeared on his body. Francesco Le Marmore Falls was carried back to Assisi, where his remaining Le Marmore Falls (fi g. 3) are located at the point years were marked by physical pain and almost where the Velino river falls into the Nera river. The total blindness. He was canonized in 1228. In 1980, top of the scarp is at 380 m a.s.l. and its height is Pope John Paul II proclaimed him the patron saint of about 165 m. ecologists. In art, the emblems of S. Francesco are the Three paths, departing from the Information Point, wolf, the lamb, the fi sh, birds, and the stigmata. His allow to reach the upper view point (“Belvedere feast day is October 4. Superiore”) in about 30 minutes. The spectacular waterfalls are opened only on Sundays, Saturdays San Francesco spent a lot of time in the Rieti area and holidays. During working days the waterfall is (for this reason called “Valle Santa” – Holy Valley): not visible because the waters are captured in order he most likely arrived in Rieti in 1209 and stayed to produce hydroelectric energy for the steel-works for a long period in 1223 and 1225-1226. The Rieti in Terni. atmosphere suggested to San Francesco the holy crib, the defi nitive Rule of the Franciscan Order and Late Quaternary evolution of probably the Canticle of the Creatures. Nowadays, Le Marmore travertine four sanctuaries (Poggio Bustone, Greccio, Fonte The Nera Valley has probably a tectonic origin related Colombo and La Foresta) testify to his staying in the to a Middle-Upper Pleistocene NE-SW trending Holy Valley. normal fault. The Velino river, tributary of the Nera river, has been cut by the above-mentioned fault. As a Field itinerary consequence a deep scarp took place. Road logs from Florence to Le Marmore Falls Along this escarpment, at least in Late Quaternary, the rich in Ca-salts waters of the Velino river 0 - 200 km: Highway A1 “Autostrada del Sole” have deposited huge amounts of travertine, which from Florence to Orte. has dammed the Velino valley. The growing and downcutting of the barrier was strictly connected During this two-hour trip we move from the Northern to climatic variations: during periods of warm and to Central Apennines, crossing three regions: in humid conditions the travertine barrier grew up, Tuscany we pass through the Arno River valley and causing a rise of base level with consequent fl ooding near Mt. Amiata, which was an important Pleistocene of the Rieti plain and the development of lakes and volcanic district, then in Umbria we follow the Tiber swamps. On the contrary, during drier and fresher River valley until entering , in the and periods, the deposition of travertine diminished or Cimini Pleistocene volcanic districts within the so- ended and erosional phases occurred, which cut the called Roman Magmatic Province. barrier and left terraces and abrasion platforms. The uppermost part of Le Marmore barrier (fi g. 3b), 200 – 235 km: From Orte to Le Marmore Falls at Cuor delle Fosse locality, consists of a 20 m thick Holocene sequence of superimposed autochthonous This part of the transfer moves from West to East and clastic travertine bodies, rich in fresh-water and

passing through the Amerini Mts (Mesozoic pelagic terrestrial molluscs (Carrara et al., 1995). DO1 to P13 n° 3 - from Volume limestones and marls of “Umbria-Marche” facies) and An anthropic colluvial horizon, containing the Terni basin. archaeological remains attributed to the Late Bronze In the Pliocene-Early Pleistocene, this basin was Age (about 3,000 years BP), occurs within the the south-western branch of the “Lago Tiberino” travertine sequence. On the basis of sedimentological basin and fi lled with lacustrine and alluvial fan and malacological features and of isotopic composition deposits (Ambrosetti et al., 1995; Basilici, 1997). The of studied sediments, together with aminostratigraphic following evolution of the Terni basin was basically analyses and radiometric age determination it has controlled by the Nera river fl uvial activity, strictly been possible to reconstruct the environmental and

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Volume n° 3 - from DO1 to P13 D07 - D07 Leader: C.Carrara In the13 from GrecciotoPoggioBustone. descriptions ofS.Francescowhotravelled byboat channels. These conditionsarealsowitnessedbythe and theprogressive obstructionoftheartifi because ofthecontinuousgrowth ofthebarrier plain wereoccupiedbyshallow lakes andponds, In theMiddle Age, againlarge areas oftheRieti sources (Cicero). between Rietiand Terni aredocumentedinclassical Terni area.For thisreason,numerous legal disputes promoted catastrophicfl increased water discharge intheNerariver actually to cultivate large areaspreviously underwater. The 2200 mlong,thatdrainedthe funded theexcavation ofanartifi In 271B.C.theromanconsulManiusCuriusDentatus Le Marmore Human impactonnaturalprocesses at Velinus occupied large part oftheRietiplain,known as as aconsequence,upstream,wideandshallow lake barrier causedalake-level increaseupto375ma.s.l.; In thefi climatic evolution ofthissequence. area (fromCarraraetal.,1995) Figure 3Left-Geomorphologicalsketch ofLeMarmore the drainedareasfromnew fl following centuries,several attemptstopreserve areas. This was onlyatemporaryeffect as, inthe channel network thatallowed to recover large wet deviated the Velino river inordertoexcavate adense . rst Iron Age afast growing ofthetravertine th century, moreover, Cistercianmonks oods downstream, inthe Lacus Velinus oods werepromoted cial channelabout , allowing Lacus cial (15 calcareous tufa (sandsandsilts)richinfresh-water lacustrine andmarshenvironment facies madeupof The innerpartofthebarrierismainlycomposed deposited partoftravertine. stripes hangingandsuperimposedonthepreviously form vertical orsubvertical festoons,drapesand that aretypicalof“water fall” environment. They deposition ofstromatoliticandphytohermalfacies of travertine. The outerpartischaracterizedbythe The Marmorebarrieriscomposedofdifferent facies Travertine facies inundations. the groundwater preserve theRietiplainfromnew of the Velino river andtheartifi dams alongtheSaltoand Turano rivers, tributaries Clementina Colluvial anthropichorizon(BUnit);5.Calcareoussand of the A Unit.6. Archeological remains;7U/Thages(ka th the CUnit;3.Pool-gradine andwaterfall travertine; 4. Figure 3Right-panoramicviewofLeMarmoreFalls and silt(calcareoustufa)rich infresh-water mollusks century et al.,1995).1.Soil;2.terrigenouscalcareoustufaof Figure 4-“CuordelleFosse” section(fromCarrara , 18 Cava Gregoriana th century Canale Pio from theNeraRiver Valley , 17 cial pumpingfrom ). At present, two present, ). At th century 24-05-2004, 13:50:25 Cava B.P.)

THE RIETI INTERMOUNTAIN BASIN AND S. FRANCESCO D’ASSISI D07

and terrestrial fauna. 22 km Paleo-environmental studies at Lago Lungo Similar facies are present also at Cuor delle Fosse and Lago di Ripasottile from High-resolution locality, where it is possible to observe spectacular stratigraphies examples of perched large structures of phytohermal and stromatolithic facies that cover lacustrine facies Two high-resolution boreholes were drilled in Lago (fi g. 4). Lungo (Calderoni et al., 1995, depth 81.5 m) and Lago di Ripasottile (Ricci Lucchi et al. 2001, depth Road log from Le Marmore to Poggio Bustone 60 m), that are the only remnants of the ancient Lacus Velinus. 8 km Piediluco and Ventina Lakes: Ancient The cores (simplifi ed stratigraphy in fi g. 5) shore-lines of Lacus Velinus after descriptions were sampled for various and multidisciplinary analyses: sedimentology (bedding, Strips of wave-cut terraced surfaces have been found structures and textures), mineralogy, isotope along the coastlines of the Piediluco and Ventina geochemistry, magnetic properties, paleontology lakes, at the border of the Montisola and Colle San (molluscs, ostracods, pollen). Balduino hills and, fi nally, in the north-eastern part The results of this multidisciplinary approach have of the plain. These features, several meters wide, provided the Late Quaternary paleo-environmental and show a variable development in length up to a few paleo-climatic evolution of the Rieti alluvial plain. hundreds meters. Silty limestone beach deposits, with gastropods and lamellibranches of a lacustrine environment are present above these surfaces. In some cases, charcoals and reworked archeological material were found inside these sediments. Locally (Case Mazzelvetta, Piediluco) the wave cut terrace is covered by travertine deposits in stromatolithic facies. The elevation of these features shows a general coherence between 372 and 376 m a.s.l., higher than the present-day alluvial plain (about 369-371 m a.s.l.). Numerous archeological sites (Carancini et al., 1985) constrained the age of this Lacus Velinus high level during the recent Bronze Age-beginning of the early Iron Age.

18 km Remnants of a Paleo-Velino-Nera drainage network at Colle Valentino ( ) and Polino

Near the village of Polino, at about 950 m a.s.l. several erosional surfaces and paleo-valleys have been interpreted as the remnant of an ancient Figure 5 - Schematic stratigraphies at Lago (Pliocene?) fl uvial system (paleo-Nera) draining to di Ripasottile and Lago Lungo SW in the paleo-Velino. Thus, these features are the DO1 to P13 n° 3 - from Volume geomorphic evidence of a single paleo-Nera-Velino Moreover, the variable Holocene thickness in fl uvial landscape. these sites (27.5 m at Lungo Lake and >60 m at Late Pliocene fl uvial deposits, located on the top of Ripasottile Lake) confi rm that Holocene fl uvial and Colle Valentino (about 900 m a.s.l) and surrounding lacustrine deposits fi lled a previous paleotopography hills (Morro Reatino), on the present divide between characterized by deep valleys and canyons connected the Velino and Nera drainage networks, are the to the last low-stand of Le Marmore travertine stratigraphic record of this fi rst stage of the drainage occurring about 18,000 yrs ago (Last Glacial network evolution. Maximum).

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Volume n° 3 - from DO1 to P13 D07 - D07 Leader: C.Carrara for thelocalinhabitantsandhasundergone several Giacono Maggiore,was foundedasacemeterychurch The SanctuaryofPoggioBustone,dedicatedtoS. (from Leggio,2000) The FranciscanSanctuaryofPoggio Bustone northern terminationofthisfault (LaCasettasite). have documentedLatePleistocenedeformationsatthe Recent seismotectonicstudies(Michettietal.,1995) this tectonicelementsincetheLatePliocene. 1989) have evidenced thefundamentalroleplayedby geological studiesofthissegment (seeCavinato etal., the WNW-ESE trendingRietinormalfault. Detailed The SanctuaryofPoggioBustoneisvery closeto age, cover thecarbonaticbedrock(Meso-Cenozoic). conglomerates, LatePliocenetoEarlyPleistocenein this slope,tenstohundredsmetersof“Villafranchian” eastern slopeoftheRietibasin.Onlower partof The villageofPoggioBustoneislocatedonthe Geological overview Poggio Bustone Stop 2: Figure 6-ThecloisteroftheSanctuaryPoggio Bustone restored notlongago,andafi in 1951. The singlenave churchhasatrussroof, reached andadmiredbymeansofarecentportalbuilt restorations over time. The wholestructurecanbe which preserved S.Francesco’s breviary fromthe tradition attributes tohim,wecanincludeastone life ofS.Francesco. Amongst themiraclesthatlocal which representsupposedmiraculousevents inthe shrines built bythe localreligiouscommunityand this naturalpathway wecanseeseveral small arrived forthefi saint passedhis“working” dayswhen,in1208,he mountain thatsoarsabove themonasterywhere A 600mlongsteepcountrypathleadstothe story ofS.Francesco. cloister therearefourteenlunettes,whichnarratethe fi partially conserved andischaracterizedbyelegantly admired. Unfortunatelythecloister(fi castle, sidedbyS.Francescoand Antonio, canbe a seventeenth centuryrepresentationofthetown’s painting depictingthe“HolyFamily”. Underthis nished smalloctagonalcolumns.Overlooking the rst timeintheHoly Valley. Along fteenth centurywood g. 6)isonly 24-05-2004, 13:50:36 THE RIETI INTERMOUNTAIN BASIN AND S. FRANCESCO D’ASSISI D07

Figure 7 - The and Papena Canyons pouring water, the imprint of the Saint’s hood, knee, most likely occurred in the Middle Pleistocene during elbow and foot on the rock, together with the sign an important erosional phase of the Northern Rieti left by the supposed presence of a terrible tempter Basin. The Papena Valley, S of Cantalice, is now a demon. At the far end of the climb the visitor fi nds relict valley recording the ancient N-S trending of the himself in front of a small church which conceals Cantalice Canyon. the “Sacro Speco” (Holy Cavern), a rocky shelter that gave protection to S. Francesco during his 19 Km Cupaello

pilgrimages. DO1 to P13 n° 3 - from Volume In the Middle Pleistocene small volcanic districts Road log from Poggio Bustone to Cittaducale (Cupaello and Polino) had been active along the eastern border of the Rieti basin. 10 km The diversion of Cantalice Canyon Near Cupaello village, a melilite and diopside The Cantalice Canyon (fi g. 7) is one of the major N-S ultrabasic lava fl ow (Gragnani, 1972), some trending valleys draining the Reatini Mountains. Near hectares wide, is embedded in Lower Pleistocene the medieval village of Cantalice, it suddenly turns “Villafranchian” fl uvial sediments.). in an E-W direction. This diversion of the canyon, According to radiometric dating (Stoppa & Villa,

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Volume n° 3 - from DO1 to P13 D07 - D07 Leader: C.Carrara (Casale Giannantoni)covered bytravertines (slope is representedbyfl The secondorder, outcroppingatabout440ma.s.l., where facies ofcascadearewellpreserved. these depositsandarepresentonthetopsurface, Volcanic Districts. Travertine horizonsintercalate tephra material,likely connectedtothe Tyrrhenian of colluvialandalluvialsedimentsrichinreworked (Canetra, SanRoccoandCittaducale),ismadeup The fi at leastthreedifferent orders. At present,thesedepositsareterraced,distributed in connected upstreamlacustrineandfl Middle-Upper Pleistocenetravertine depositsand at themiddlecourseof Velino River, is toobserve The aimofthisstop,locatedafew kmEastofRieti Cittaducale Stop 3: Pleistocene. that reacheditsacmeinthissectorduringtheMiddle agreement withtheextensional tectonicenvironment 1991) theeruptionoccurred640kyrs BP, in terraced travertine barrieratCittaducale. Giannantoni) isabout480kyrsinageaccordingto Ar/Ar datingonvolcanoclastic materials.Inthebackground, the Figure 8-MiddlePleistoceneterracesalongthe Velino Valley. Intheforeground, alacustrineterrace(Casale rst order, outcroppingat480÷500m a.s.l. uvial andlacustrinesediments uvial sediments. uvial of theRietibasin. The Rietiurbanarealiesatthesouth-easternborder Urban GeologyandSeismicResponse 10 kmRieti: Road logfrom CittaducaletoGreccio this ordertotheUpperPleistocene. and alluvialhorizons.U/Thdatingoftravertines refer Strade, revealed travertines intercalatedwithcolluvial A 62mstratigraphyfromcontinuousborehole,at Tre order arestillpreserved alsoatCaporioand Tre Strade. Cittaducale and Villa Roselli.Remnantsofthesame is encasedintheprevious ordersatSanRocco, The thirdorder, outcroppingat390÷430ma.s.l., Pleistocene. et al.,1985)constrainsthisordertotheMiddle within lacustrinedeposits(480kyrs, Capaldi related tothisorder. Ar/Ar datingoftephramaterial Rieti), partiallyreshapedtravertines areprobably from thisstop(Colarieti,Granaro,CampoMoroand and cascadefacies, Villa Roselli). Downstream 24-05-2004, 13:50:48

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Figure 9 - Simplifi ed geological map of historical downtown Rieti Geological surveys distinguish three main sectors Stop 4: (fi g. 9): the southern sector is founded on Holocene Greccio alluvial deposits of the Velino river; the central one Geological overview lies on travertines which are often covered in the The village of Greccio is located on the western slope most elevated portion of the town by thick mounds of the Rieti basin, characterized by at least three main of rubble; the northern sector is built on alluvial fans NNE-SSW trending Neogene thrust units made up from the eastern margin of the Rieti basin (Reatini of Meso-Cenozoic pelagic limestones and marls mountains). (Umbria-Marche facies). During the Quaternary, a N-S trending normal fault system, partially buried By comparing the distribution of damage induced beneath the recent alluvial deposits of the Rieti plain,

by the June 27, 1898 earthquake (Me=5.3, I0=VII- cut the Neogene thrusts. This normal fault system Volume n° 3 - from DO1 to P13 n° 3 - from Volume VIII MCS) and the different outcropping lithologies represents the western border of the Rieti basin (Comerci et al., 2003) it has been possible to point graben. out that the mostly damaged areas are founded on It is important to outline that the Greccio slope post-glacial alluvial deposits and on anthropic fi ll is affected by important gravitational phenomena deposits. In contrast, the least damaged areas are (rock-falls in the calcareous upper sector and distributed around the most elevated portion of the rotational landslides in the marly and clayey lower central sector of the town, where houses were built on sector). solid travertine deposits.

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Volume n° 3 - from DO1 to P13 D07 - D07 Leader: C.Carrara near theHolycave. the secondhalfofthirteenthcenturyongrounds S. Francescototheextent ofbuilding a sanctuary in then Grecciointimatelytieditsdestiny tothecloakof crib was setupandadmiredbythepilgrims.Since Christmas Eve, the fi Fame reachedthe walls of Greccioin1223whenon kilometres away. of thevalley, touching therock-wall situatedover two young boy threw thefi landed, therehewould build hisdwellingplace. The the hill,promisingthatwherever theburning stick the town andtoldhimtothrow afi of thelocalpeople,hepicked outasmallboy from was soontocome.Infact complyingtotherequests was immediatelygoodandproofofthis“feeling” between S.FrancescoandtheinhabitantsofGreccio throughout thesurroundingarea. The relationship since 1217,whenhestartedhisevangelical work Lacerone, overlooking Greccio,as hisdwellingplace According tothelegend, S.FrancescohadchosenMt. (Leggio, 2000) The FranciscanSanctuaryofGreccio rst representationoftheHoly re-brand ontheoppositeside Figure 10-TheFranciscan Sanctuary ofGreccio re-brand towards re-brand friars oncecelebratedthesacredfunctions. of tiedchairstallsonwhichthesmallcommunity double structureandwhoseinteriorreveals aseries Close bythereisasmallchapelwhichpresents separated bymeansofreedsandwooden barriers. The structureissubdivided intotiny independentcells dormitory known asthedormitoryofS.Bonaventura. are abletoseethesmallthirteenthcenturywooden from therock.Inupperpartofmonasterywe slept, restingplaceswhichwereobviously carved out to show theexact placeswhereS.Francescoateand Greccio andthatofBethlehem. The itineraryproceeds the cave representtwo very importantcribs;thecribof unknown Umbrianartist. The fi of thefi between theendoffourteenthandbeginning where touristscanadmiretwo frescoespainted A visittothemonasterydepartsfromHolycave ANPA andItalianGeologicalSurvey (now APAT), study conductedintheRietibasinareafundedby This fi Aknowledgments eld tripguidebookisthe result ofalong-term fteenth centuriesbytheskilledhandsofan gures onthewalls of 24-05-2004, 13:51:10 THE RIETI INTERMOUNTAIN BASIN AND S. FRANCESCO D’ASSISI D07

and CNR-GNDT. M. and Serva L. (1993). I terrazzi della medio-bassa The Authors are very grateful to all the people valle del F. Velino. Studi Geol. Camerti, Spec. Vol. involved in this research and in particular to A.M. (1992/1), 97-102. Blumetti, V. Comerci, T. Leggio, P. Lorenzoni, A. M. Carrara C., Esu D. and Ferreli L. (1995). Lo Michetti, M. Raglione and E. Vittori. sbarramento di travertino delle Marmore (bacino di Rieti, Italia Centrale): aspetti geomorfologici, Reference cited faunistici ed ambientali. Il Quaternario, 8(1): 111- Accordi B and Carbone F. (1988). Lithofacies map of 118. Latium-Abruzzi and neighbouring areas, scale 1: Cavinato G.P., Chiaretti F., Cosentino D. and Serva L. 250.000. CNR – Prog. Fin. Geodinamica, Quaderni (1989). Caratteri geologico-strutturali del margine de “La Ricerca Scientifi ca”, n° 114, vol. 5. orientale della conca di Rieti. Boll. Soc. Geol. It., Ambrosetti P., Basilici G., Papasso Barbato L., 108(2), 207-218. Carboni M.G., Di Stefano G., Esu D., Gliozzi E., Comerci V., Molin D., Pasquarè F.A. and Serva L. Petronio C., Sardella R. and Squazzini E. (1995). (2003). Risposta sismica dell’area urbana di Rieti Il Pleistocene inferiore nel ramo sudoccidentale del in occasione del terremoto del 27 giugno 1898 nel Bacino Tiberino (Umbria): aspetti litostratigrafi ci e bacino di Vazia (RI). Boll. Soc. Geol. It., 122, 147- biostratigrafi ci. Il Quaternario, 8(1): 19-36. 156. Barberi R. and Cavinato G.P. (1993). Analisi Cosentino D., Scoppola C., Scrocca D. and Vecchia sedimentologiche ed evoluzione paleogeografi ca P. (1992). Stile strutturale dei Monti Reatini e dei del settore meridionale del bacino di Rieti settentrionali (Appennino centrale) a (Appennino centrale). Studi Geologici Camerti, confronto. Studi Geol. Camerti, Vol. Spec. (1991/2), Spec. Vol. (1992/1): 39-54. CROP 11, 55-61, Camerino. Basilici G. (1997). Sedimentary facies in an D’Agostino N., Jackson J.A., Dramis F. and extensional and deep lacustrine depositional Funiciello R. (2002). Interactions between mantel system: the Pliocene Tiberino Basin, Central Italy. upwelling, drainage evolution and active normal Sedim. Geology, 109, 73-94. faulting: an example from the central Apennines Brozzetti F. and Lavecchia G. (1995). Evoluzione del (Italy). Geophysical Journal International. campo degli sforzi e storia deformativa nell’area dei Doglioni C. (1993). Some remarks on the origin of the Monti Martani (Umbria). Boll. Soc. Geol. It., 114, foredeeps. Tectonophysics, 228, 1-20. 155-176. Dramis F. (1993). Il ruolo dei sollevamenti tettonici Brunamonte F., Gaeta M. Michetti A.M., Mottana a largo raggio nella genesi del rilievo appenninico. A. and Palladino D.M. (1992): Caratterizzazione Studi Geologici Camerti, Spec. Vol. (1992/1), 97- mineralogico-petrografi ca ed inquadramento 102. stratigrafi co preliminare di alcune depositi Duprè Theseider E. (1938). Il lago Velino. Saggio vulcanoclastici dell’area reatina. Studi Geologici storico-geografi co. Rieti, Arte grafi che Nobili, 108 Camerti, vol. spec., (1992/1), 65-72. pp. Calderoni G., Carrara C., Ferreli L., Follieri M., Ferreli L., Brunamonte F., Filippi G. Margheriti L. Gliozzi E., Magri D., Narcisi B., Parotto M., Sadori and Michetti A.M. (1995). The formation of the L., and Serva L. (1995). Palaeoenvironmental, Lacus Velinus and the settlement of the Iron Age in palaeoclimatic and chronological interpretations of the Rieti Basin. Proc. “Egyptian–Italian Seminar on a late Quaternary sediment core from Piana di Rieti Geosciences and Archeology in the Mediterranean (Central Apennines, Italy). Giornale di Geologia, countries”, Cairo, November 28-30 1993, 51-66. 56(2): 43-72. Ferreli L., Brunamonte F., Margheriti L. & Michetti

Capaldi G., Civetta L. and Gillot P.Y. (1985). A.M. (1993) - Riconoscimento di un livello DO1 to P13 n° 3 - from Volume Geochronology of Plio-Pleistocene rocks from lacustre della prima eta del ferro nel bacino di southern Italy. Rend. Soc. It. Min. Petr., 40, 25-44. Rieti e possibili implicazioni neotettoniche. Studi Carancini G.L., Massetti S. and Poli F. (1985). L’area Geologici Camerti, volume speciale 1992/1, 127- tra Umbria meridionale e Sabina alla fi ne della 135. Protostoria. Dialoghi di Archeologia. Terza Serie, GEMINA. (1963). Il bacino di Leonessa. In: GEMINA Anno 3, numero 2, 37-56. (Editor) “Ligniti e torbe dell’Italia continentale”: Carrara C., Brunamonte F., Ferreli L., Lorenzoni P., pp. 107-114. Margheriti L., Michetti A.M., Raglione M., Rosati Gragnani R. (1972). Le vulcaniti melilitiche di

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Volume n° 3 - from DO1 to P13 D07 - D07 Leader: C.Carrara Michetti A.M. andServa L.(1991).New dataon Michetti A.M., BrunamonteF., Serva L.and Whitney Manfredini M.(1972).Studioidrogeologicodella Lorenzetti (1989).Storiasocialeeeconomicadella Leggio T. (2000). Andar persantiantiche Leggio T. andServa L.(1991).Labonifi Laurenzi M.,StoppaF. and Villa I.(1994).Eventi 37-46. area (Rieti,CentralItaly).Rend.Soc.Geol.It.,13, the seismotectonicpotentialofLeonessafault Seattle, WA, USA,pp.63-82 Assoc. Eng.Geol.,SpecialPublicationn°6(1994), (Editors) “Perspectives inPaleoseismology”, Bull. (Central Italy).In:Serva L.&SlemmonsD.B. paleosismological evidence intheRietiregion R.A. (1995).Seismichazardassessmentfrom 122, Rome. piana diRieti.CNRQuad.Ist.Ric. Acque, 6,87- Sabina. IstitutoE.Cinese.Rieti,637pp. Provincia diRieti,169pp. in provincia diRieti. Assessorato allaCultura, strade….Itinerari traipaesaggieglispazidelsacro Protezione, 25,1-10. di Rietidall’etàromanaalmedioevo. Sicurezzae Summer Meeting,Plinius12:61-65. Abstracts Volume, 77°ItalianGeologicalSociety aggiornamento ecomparazionedeidaticronologici. ultra-alcalino umbro-laziale(ULUD):revisione, ignei monogeniciedepositipiroclasticineldistretto Cupaello (Rieti).Rend.Soc.Min.It.,28,165-189. ca dellapiana Verri A. (1883).Studigeologicisulleconchedi Terni Stoppa F. and Villa I.M.(1991).Primidaticronologici Segre A.G. (1990).BacinoquaternariodiRieti- Ricci LucchiM..CalderoniG.,CarraraC.,Cipriani Raffy J.(1983).Leversant tyrrhéniendel’Appennin Patacca E.,SartoriR.andScandoneP. (1990). 4-82. e Rieti.R. Acc. Naz.Lincei,Mem.,serie3,15(4), June 1991,54. Quaternario nell’area Tosco-Laziale”, Pisa12-13 Neogenici elororapporticonilmagmatismoPlio- Volume, Workshop “Evoluzione deibacini del distrettoultra-alcalinoumbro-laziale. Abstracts Perusina, V.6,177-185. nell’alveo dell’anticoLacus Velinus, Archeologia sulle nuove ricerchedisuperfi Curci P. &DionisiP., 1990–Secondarelazione Piediluco. In:CaranciniG.L.,MassettiS.,PosiF., Giornale diGeologia,ser3°,62,105-136. paleoenvironmental andpaleoclimaticevolution. Quaternary recordoftheRietibasin,centralItaly: M., RicciLucchiF. and Vigliotti L.,(2001).Late Lombardo M.,Longinelli A., MagriD.,Nebbiai N., EsuD.,FerreliL.GirottiO.,GhiozziE., (1979) 705pp. Central: étudegéomorphologique.CNRS,Paris Geol. It.,45,425-451. relations sincelate Tortonian times.Mem.Soc. Tyrrhenian Basinand Apennines Arcs: kinematic ce eseguite cie 24-05-2004, 13:47:17 Back Cover: Field Trip Itinerary

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