LOGISTIC

The excursion will start and end at Rome's Fiumicino Airport. Monday June 3 rd will be dedicated to road transfer via motorway A1 (Roma-exit Orte), then superhighway E-45 until Perugia with exit Bosco-Gubbio. Then road n. SS-298 to Gubbio. Time of transfer is about 3 hours. To return time in Rome is planned for Friday 7 th according with the participant's fly schedules. The accommodation in Gubbio is in the medieval part of the town: HOTEL GATTAPONE -Via Ansidei 6 (100 m from Piazza 40 Martiri) Phone : 075-9272489 . www.hotelgattapone.net. Depending on the logistic constraints for each day, lunch will be either carry-on or in restaurants along the itinerary. The restaurants selected for dinner, mostly near the hotel, offer the characteristic regional cuisine.

In case of emergency contact one of the excursion leaders

Geology and stratigraphic framework of the Umbria-Marche Apennines

. The UMA form the southern sector of the Northern Apennines, part of the peri-Mediterranean system of Alpine chains formed as a result of differential movements between Africa andEurope plate. The area has been affected by at least three main tectonic phases: an extensional phase in the Mesozoic, compressional in the Neogene and, an extensional phase in the Umbria sector from Late Miocene and Pleistocene onward.

The Umbria-Marche sedimentary basin formed in the late Triassic in a passive continental margin of the southern Tethys Ocean. Its over 3000 m thick stratigraphic succession records the thermal and mechanical subsidence history from the Jurassic carbonate platforms to the pelagic realm of the Paleogene, while its upper part consists of Neogene terrigenous clastics that accumulated in a migratory foredeep system reflecting the encroachment of the Apenninic deformation and sedimentation patterns into the Adriatic Foreland.

The extensional regime triggered by the opening of the Tethys Ocean in the Late Triassic-Early Jurassic is recorded in the stratigraphic succession by a change in the facies type and thickness. The subsequent deposition of evaporites and dolomites in the Upper Triassic was followed by the formation of a carbonate platform in the Early Jurassic. Throughout the Early-Middle Jurassic, the opening of the Alpine Tethys Ocean led to the separation of the persistent carbonate platform (Central Apennines, Latium-Abruzzi region), where the sedimentation rates compensated for the syn-rift subsidence, from the pelagic domain (Northern Apennines, Umbro-Marchean region) by a slope-to-basin transitional domain. The UM pelagic basin was subdivided into structural highs and deeper basinal areas of varying thicknesses and facies bounded by Jurassic faults. The extensional phase ended during the Early Cretaceous when the deposition of the Maiolica Fm. homogenized the lithological facies while maintaining the differences in the bathymetry between the former structural highs and lows (Fig3).

Sedimentation in the area became homogeneous following the deposition of the Fucoid Marls Fm. in the early Aptian evolving towards hemipelagic lithotypes characterized by carbonates and marls with an abundance of chert during the Cretaceous and Paleogene. The Cretaceous UMA sequence is lithologically subdivided into several discrete formations and members on the basis of colour changes and carbonate content fluctuation along with the presence or absence of chert and black shales. The following sequence spanning a thickness of about 750 m can be recognized: Maiolica (late Tithonian -early Aptian), Fucoid Marls (early Aptian -latest Albian), Scaglia Bianca (latest Albian -earliest Turonian) and Scaglia Rossa (earliest Turonian -early Lutetian).

Although characterized by homogeneous sedimentation during the Cretaceous, the UM pelagic basin records several tectono-sedimentary events. Slumps are common, especially in correspondence to Jurassic faults reactivated in the Aptian and Turonian and in the Late Cretaceous. Carbonate turbidites composed exclusively of foraminifera are very common in the whole UM basin, but are particularly abundant in the Late Cretaceous.

Convergent orogenic activity in the Alps began in the Late Cretaceous (Fig. 4) while the Northern Apennines foreland fold-and-thrust belt developed since the Late Oligocene with the convergence and subsequent subduction of the Adriatic microplate under the Corsica-Sardinia block. The latter was controlled by the opening of the Liguro-Provencal ocean, which caused an ~30° rotation of the Corsica-Sardinia block and was accompanied by the development of the foredeep where proximal turbiditic sediments were deposited. Since this time, the tectonic and sedimentary activity has migrated eastward.

In the early Miocene (late Burdigalian-early Langhian), the back-arc extension shifted eastward with the spreading of the Tyrrhenian Sea. The orogenic front has also shifted eastward (possibly related to the subsequent roll-back and retreat of Adriatic lithosphere) with the progressive development of an arcuate thin-skinned fold-and-thrusts belt of NE convexity with the deformation of the Adriatic foreland against the foredeeps. The latter give good timing of the deformation, it's rate and the evolutional history of the tectonic-sedimentary events for all of the Northern Apennines.

The turbiditic deposits of the Miocene Umbro-Marchean and Romagnan foredeep are arranged in a typical tripartite suite, with basal prototurbiditic marls, a thick marly arenaceous orthoturbiditic sequence and capping cataturbiditic marls. The distribution of these intervals reflects the migration pattern of the foredeep system, which accompanied the migration of the orogenic paroxysm toward the Adriatic foreland characterized by propagating detachment tectonics in active foredeep segments. The synsedimentary character of this process is recorded by the distribution of key levels and slump zones. The depocenter migration of the foredeep system reconstructed for the early to middle Miocene amounts to about 10 km/Ma, increasing to 20 km/Ma during the late Miocene through Pleistocene.

The UMA tectonics since the middle-late Miocene and up to the Pleistocene, were characterized by coeval occurrence of shortening in the foreland and extension in the hinterland. This Tyrrhenian Sea related extension, continued through the Pleistocene-Holocene to the present day as recorded in the Umbria Preapennines by outcropping normal fault systems near Gubbio.

Geological framework of Gubbio area

In the Umbria Preappennines of central Italy, the structural geology near Gubbio is dominated by a rootless NE verging anticline formed in the late Miocene during the Neogene compressional phase of the Apenninic orogeny. The SW side of the anticline is downdrown by a normal fault forming the Gubbio Valley. The anticline was formed in the late Messinian to early Pliocene and thrust a few kilometers toward the NE, with the lower detachment plane located in the Triassic Burano Formation. The emplacement of the Gubbio anticline resulted in pervasive fore and back thrusting with associated retrovergent folding of the Schlier and Marnoso-Arenacea Formation terrains in front of it. The structural style of the shallow thrust sheets is characterized by asymmetric NE-vergent synclinal units separated by low angle reverse faults.

Starting from the late Pliocene, the Umbria area experienced an extensional tectonic phase. A system of SW dipping, NW-SE striking normal faults formed a set of intramountain valleys infilled by continental deposits with fluvio-palu-lacustrine facies of Plio-Pleistocene age. One of these extensional faults cuts the interior of the Gubbio anticline forming a trough of about 1000 m and generateing an asymmetric basin over a rollover anticline in the hanging wall. The basin is 20 km long and 6 km wide, oriented NW-SE and infilled by continental sediments of Pleistocene age. The depocenter of the 300 m deep basin is situated very close to the master fault plane. The fault trace, observable in the field for about 25 km, shows several oversteps and banding. It is concave southwestward, i.e. showing listric geometry. The inclination of the fault scarp ranges from 50° to 80° as a function of the carbonate content of the outcropping rocks. The fault surfaces display several geometric features that allow the identification of the displacement vector orientation as SW. Other normal faults, both synthetic and antithetic to the master fault plane, are observable in the Contessa Valley and in the Bottaccione Gorge.

In Contessa Valley and in its twin sister, Bottaccione Gorge (Figs. 5 and6), two of the most complete, both in a morphological and stratigraphic sense, Cretaceous-Paleogene pelagic sediment successions known from the Tethyan Realm, characterized by a remarkable record of many crucial aspects of the Earth history, are exposed (Fig. 2).

Owing to continuous deposition in a pelagic setting, a rather modest tectonic overprint, and the availability of excellent age control through magneto-, bio-, chemo-and tephrostratigraphy as well as direct radioisotopic dates from interbedded volcaniclastic layers, these sediments have played a prominent role in the establishment of the standard Cretaceous-Paleogene time scales. In particular, the numerous volcaniclastic layers within the Eocene to Miocene portion of this sequence present a rare opportunity for radioisotopic dating of magneto-, bio-, and chemostratigraphic events.

STOP 1.1

The Cretaceous stratigraphy of the Umbria-Marche basin and the Cretaceous pelagic succession of the Vispi Quarry While the exposure of the Cretaceous Scaglia Rossa is perhaps better in the classic Bottaccione section, and mostly covered by retention steel nets along the Contessa highway, the Maiolica (Late Tithonian to Early Aptian), Marne a Fucoidi (Early Aptian to Late Albian), and Scaglia Bianca (Late Albian to Early Turonian) Formations are nowhere in the region as well exposed as in the huge and spectacular quarry of the Vispi Company (Figs. 7 and8). The sediments belonging to these formations were deposited well above the calcite compensation depth at middle to lower bathyal depths (1000-1500 m) and at ~20°N paleolatitude over the southern margin of the western Tethys Ocean, An interval displaying synsedimentary disturbance within the uppermost Maiolica is recognizable, which corresponds to the interval visible at the base of the Bottaccione section. A thin ferruginous level, darker in color with reddish hues, approximately at half height on the quarry face, corresponds to the organic-rich Faraoni Level, rich in ammonites and Late Hauterivian in age. In the upper part of the quarry face, the Marne a Fucoidi Formation displaying synsedimentary folds and slumped masses is recognizable. Within the Cretaceous succession of the U-M basin, the Marne a Fucoidi represents a distinctive varicolored interlude with more shale. This formation consists of thinly interbedded pale reddish to dark reddish, pale olive to dark reddish brown and pale olive to grayish olive marlstones and calcareous marlstones together with dark gray to black organic carbon-rich shales, usually with a low carbonate content, and yellowish-gray to light gray marly limestones and limestones. The upper portion of the Marne a Fucoidi is cyclic, with well-developed light gray limestone/marlstone cyclothems. Several distinctive organic-rich black shale and marl marker beds occur within the Aptian-Albian interval, some of which have been identified as the regional sedimentary expression of Oceanic Anoxic Event (OAE) 1a (Selli Level) to OAE1d (Pialli Level). Marlstones progressively decrease in frequency upward leaving the predominant, thin-bedded whitish limestone with gray chert nodules of the Scaglia Bianca Formation. In the uppermost part of the Scaglia Bianca Formation, the organic-rich Bonarelli Level that is the sedimentary expression of the worldwide latest Cenomanian OAE2, stands out. Approximately 4 m above the Bonarelli Level, the Scaglia turns pale red, alternating with intervals of paler, whiter coloration and abundant chert ribbons, light gray, tan and reddish in color. Further up, the Scaglia Rossa Formation develops. Several Cretaceous Oceanic Red Beds are also well recognizable. (Coccioni, 1996, and unpublished data).

Meso-Cenozoic tectonic-sedimentary events in the Umbria-Marche basin

The tectonic activity in the basin since the Jurassic, when low angle normal faults shaped the carbonate platforms and drove the basin's subsidence formed, is well documented. Scarps with megabreccia, slumps and sedimentary dikes are distributed along the main fault systems. Several sediment deformation events are known in the Cretaceous stratigraphic succession of the northern UMA sector. In the Gubbio area, several slumps mobilizing Aptian layers at the boundary between the Maiolica Formation and the lower part of the Fucoid Marls Formation are documented (Fig. 9). These soft-sediment deformation events are associated with structures in lithified rocks within normal faults formed during the Pleistocene extensional tectonic phase. Different kinds of deformation structures cutting across the Gubbio anticline axes are observable in the outcrops along the main valley. The Fucoid Marls thickness increases from a few meters in the SE zone to tens of meters with a duplex in the NW zone, where compressive structures dominate over extensional ones. The main sediment deformation structures are slides with strain layers consisting of several folds of different deformation styles. Extensional zones are characterized by single, downslope-dipping normal faults, a few of which have listric geometries. Compressional zones are dominated by turnedup, rolled-in and recumbent folds with upslope-dipping reverse faults.

The basal detachment zone is characterized by imbricate faults, sigmoidal sheets and overfolds with local thinning of marl layers. The similarity in structural style between softsediment deformational structures and deformation structures in lithified rocks means that differentiating between these two groups of structures is difficult. Geometrical analysis of the fold axis trend has revealed a single large gravitational event along a paleoslope dipping toward the north. The estimated area involved in the deformation is about 60 km2 for a volume of 0.8 km3 of displaced sediments (Fig. 10). The strike of the slope corresponds to the main trend of the oldest Jurassic extensional lineaments and is likely linked to the transform faults of the westernmost Tethys rifting systems.

The inferred trigger mechanism for slump activation could be related both to the seismic input and to an overload of the sediments at the limestone/marl boundary. These two lithologies have very different rheological proprieties and permeabilities. The sealing behavior of the marl layers with respect to fluid migration in the sediment increases the hydrostatic pressure and produces mechanic instability of the sediments along a slope of a few degrees.

The Bonarelli Level

The Contessa Valley and the Bottaccione Gorge are to be considered the classic sites for the organic-rich Bonarelli Level (OAE2) (Figs. 11and 12). This event, which lasted for ~410 kyr, led to a severe environmental perturbation. Several events and biotic changes among calcareous and siliceous plankton, including the acme and crisis of different planktonic foraminiferal and radiolarian genera, are recognizable across the stratigraphical interval that includes the Bonarelli Level . They provide evidence of a progressive and rapid deterioration of paleoenvironmental conditions, from a general meso-eutrophic environment and a well-developed oxygen minimum zone (OMZ) to an increased surface productivity, enhanced OMZ, and marked rapid changes of ecological parameters (e.g., temperature, salinity, trace metals), reaching a climax coincident with the Bonarelli Event and of the subsequent, gradual recovery (Figs. 13 and14). Although no major mass extinction in planktonic foraminifera occurred across the Bonarelli Event, the extinction of the most specialized forms (i.e., the rotaliporids), is recorded just before its onset. Episodes of increased eutrophic conditions across the stratigraphical interval that includes Bonarelli Level are indicated by pulses in abundance of radiolarians. These marked planktonic foraminiferal changes culminate at the base of the Bonarelli Level with the temporary disappearance of all planktonic foraminifera and the concurrent radiolarian proliferation. A drastic radiolarian faunal change took place within the median part of the Bonarelli Level, associated with an interval of high organic matter preservation, but relatively low values of silica . Therefore, this part constitutes a critical period in the evolutionary history of Radiolaria. Diversity and density of trace fossils suggest fluctuations in pore water oxygenation from anoxic to oxic or dysoxic conditions during the deposition of the dark, pelagic sediments of the Bonarelli Level (Fig. 21). Figure 13 -Total organic carbon (TOC), δ 13 C TOC and δ 13 C Ph stratigraphic profiles across the Bonarelli Level, S4 core, Gubbio [START_REF] Tsikos | Carbon-isotope stratigraphy of the Cenomanian-Turonian Oceanic Anoxic Event (OAE): correlation and implications[END_REF]. The Cretaceous/Paleogene (K/Pg) boundary is well exposed on both sides of the highway, right after the northern exit of a short rock-fall protection tunnel (Fig. 22). A white limestone 60 cm-thick, with planktonic foraminifera of Maastrichtian age underlies the Iridium-clay layer, then overlain by the darker-red Scaglia Rossa of Paleocene age. The K/Pg boundary clay layer, 1.5 cm in thickness, is dark red, with a thin gray-green sole at the base. In comparison with its twin section at Bottaccione Gorge (see Stop 1.6), the K/Pg clay layer contains a more evolute glaucony, which would indicate that early diagenetic low-Eh conditions in this site lasted a bit longer than at Bottaccione. Moreover, strongly flattened, red hematite magnetic spheroids, which are absent in the Bottaccione and in other known K/Pg clay outcrops in the region, suggest that at Contessa the re-oxidation process following the initial low-Eh event was more intense than elsewhere in the U-M basin.

K

Pg

STOP 1.4 The Bottaccione Gorge and the C34n/C33r reverse boundary

The Bottaccione Gorge is the classic outcrop site for the Upper Cretaceous-Paleogene pelagic succession of the U-M Apennines (Figs. 24 and25). This nearly continuous and complete road exposure offers the rare opportunity to intercalibrate the calcareous plankton biostratigraphy and the isotope stratigraphy with the sequence of paleomagnetic polarity reversals through a span of 80 Myr (Figs. 26 and27).

In the mid 1970's, a renewed interest in the nearly continuous and complete Upper Cretaceous-Paleogene sequence of Gubbio by a group of interdisciplinary researchers led them to join into a perhaps unprecedented team effort for resolving the lithostratigraphy, sedimentology, planktonic foraminiferal biostratigraphy, and, above all, the magnetostratigraphy of this span of geologic time. The results of this coordinated research project were published in a series of papers in an issue of the Geological Society of America Bulletin (1977) along with the proposal of Gubbio as type section for the Late Cretaceous-Paleogene geomagnetic reversal time scale. For the first time it was possible to assign accurate magnetobiostratigraphic ages to the marine magnetic anomalies, and, thus, to date, with reliable geologic and biochronologic criteria, the expanding world's oceans.

A few years later, the discovery of an Iridium anomaly together with other trace elements in the clay layer marking the K/Pg boundary of the Bottaccione Gorge section suggested the hypothesis that the mass extinction at the end of the Mesozoic Era was triggered by the impact against the Earth's surface of a large extraterrestrial object (i.e., an asteroid or a comet) such as the one that led to the K/Pg Chicxulub structure, then opening the way to more than three decades of exciting scientific research and of extraordinary scientific debate within the world's Earth science community and the development of a new theory on the evolution of terrestrial life (Fig. 30).

The section extends along the state road SR298 from Gubbio to Scheggia, crossing the Bottaccione Gorge. The gorge dissects perpendicularly the Eugubini Mountains, separating the peaks of Monte (Mount) Ingino and Monte (Mount) Foce. Exiting the city of Gubbio from the medieval Metauro gate towards Bottaccione gorge and Scheggia, past the last houses the road crosses the river. Here the Bottaccione stream cuts its bed into the Upper Jurassic radiolarian cherty limestone (Calcari Diasprigni Formation). Shortly after the Calcari Diasprigni outcrop along the road, facies change into the light gray to white calpionellid limestone of the Maiolica Formation, forming the steep slopes of the gorge as far as the second watermill. The Maiolica is generally well-bedded and displays, as a distinctive feature in the Bottaccione Gorge, intraformational slump masses, with clasts and pebbles of the same reworked Maiolica and chert. In front of the second watermill, there is a faulted and slumped contact between the Maiolica and the overlying Marne a Fucoidi, which eliminates part of the upper Maiolica and the lower portion of the Marne a Fucoidi. The upper portion of the Marne a Fucoidi is cyclic, with well-developed light gray limestone/marlstone cyclothems. Marlstones progressively decrease in frequency upward leaving the predominant, thin-bedded whitish limestones with gray chert nodules of the Scaglia Bianca Formation. In the uppermost part of the Scaglia Bianca, the organic-rich Bonarelli Level occurs. The Scaglia Rossa outcrops for a long stretch along the road and in the side valley departing from the Bottaccione Restaurant from where it maintains a more constant reddish color. In the vicinity of an electric pole along the Bottaccione road is the top of the long normal-polarity magnetic zone and consequently the bottom of the subsequent reverse magnetic interval of the Cretaceous, corresponding to the oceanic Magnetic Anomaly 33 (basal Campanian). Above the Magnetic Anomaly 33, the Scaglia Rossa is devoid of any chert and its age is Campanian-Maastrichtian (Fig. 23). After the two subsequent bends in the road, there is a parking space on the right hand side, corresponding to the old Bottaccione road before it was rectified. In correspondence of this widening, the Scaglia Rossa facies change abruptly, in correspondence of the transition from the Cretaceous to the Paleogene. The K/Pg boundary is well-exposed at m 382.6, in the upper part of Chron 29r (Fig. 31). At the top of the monotonous reddish limestone, there is a 60 cm-thick bed of white pelagic limestone, Maastrichtian in age. Above, there is a thin interval of red and green clay; then again Scaglia Rossa facies resumes, with a darker reddish coloration and extending in age to the Paleocene and Eocene (after the Medieval aqueduct). The Paleogene Scaglia resumes its pale pink coloration and becomes again cherty, of a darker red brown hue. The transition to the Scaglia Variegata Formation consists of an intercalation of reddish and light gray beds, becoming gradually grayer (Scaglia Cinerea Formation). Strata become progressively lesser rich in chert, up to chert-free, upwards. The Scaglia Cinerea displaying its classical facies is exposed to the bridge crossing the Bottaccione Gorge.

With the definition and proposal of the Parvulorugoglobigerina eugubina (the former Globigerina eugubina) planktonic foraminiferal biozone as the base of the Paleogene in the type section of the Bottaccione Gorge it was described in detail a number of other K/Pg boundary sections throughout the U-M Apennines. In doing so, it was established a simple and precise criterion for recognizing the K/Pg boundary in any pelagic carbonate sequence in the world. The boundary is marked by a 1.5 cm-thick dark red clay layer with a thin graygreen sole at the base sandwiched between the last Cretaceous limestone containing large (up to 1 mm) planktonic foraminifera which are recognizable with a hand lens, and the first Paleogene limestone containing tiny (less than 0.1 mm) globigerinids not visible with a hand lens (Fig. 32). This constitutes a clear paleobiologic signature of the mass extinction event that took place in this deep marine environment at the K/Pg boundary. The white color of the top Cretaceous limestone has been attributed to iron reduction and leaching, and consequent bleaching of the oxidized, pink pelagic ooze, following a brief episode of anoxia at the watersediment interface. This low-Eh condition was probably caused by anoxic bottom waters, rich in organic matter, which formed on the abyssal sea floor immediately after the mass killing of the marine plankton. The K/Pg boundary clay is made of various clay minerals, including illite, smectite, kaolinite, and mixed layered illite-smectite clay. In addition, the K/Pg boundary clay contains variable amounts of secondary calcite crystals together with microspherules made of K-feldspar, glaucony, and iron oxide, shocked quartz grains, and benthic foraminiferal tests. Figure 26 -The Bottaccione section: Lithologic log, calcareous nannofossil and planktonic foraminiferal biostratigraphy correlated to magnetostratigraphy (after Premoli [START_REF] Silva | Cretaceous planktonic foraminiferal biostratigraphy and evolutionary trends from the Bottaccione section, Gubbio, Italy[END_REF].

STOP 1.5 The inoceramid extinction at Bottaccione

STOP 1.6 The K/Pg boundary at Bottaccione

After the two subsequent bends in the road, there is a parking space on the right hand side, corresponding to the old Bottaccione road before it was rectified. In correspondence of this widening, the Scaglia Rossa facies change abruptly, in correspondence of the transition from the Cretaceous to the Paleogene. The K/Pg boundary is well-exposed at m 372.6, in the upper part of Chron C29r (Fig. 31). At the top of the monotonous reddish limestone, there is a 60 cm-thick bed of white pelagic limestone, Maastrichtian in age. Above, there is a thin interval of red and green clay; then again Scaglia Rossa facies resumes, with a darker reddish coloration and extending in age to the Paleocene and Eocene (after the Medieval aqueduct). The Paleogene Scaglia resumes its pale pink coloration and becomes again cherty, of a darker red brown hue. The transition to the Scaglia Variegata Formation consists of an intercalation of reddish and light gray beds, becoming gradually grayer (Scaglia Cinerea Formation). Strata become progressively lesser rich in chert, up to chert-free, upwards. The Scaglia Cinerea displaying its classical facies is exposed to the bridge crossing the Bottaccione Gorge.

With the definition and proposal of the Parvulorugoglobigerina eugubina (the former Globigerina eugubina) planktonic foraminiferal biozone as the base of the Paleogene in the type section of the Bottaccione Gorge it was described in detail a number of other K/Pg boundary sections throughout the Umbria-Marche Apennines. In doing so, it was established a simple and precise criterion for recognizing the K/Pg boundary in any pelagic carbonate sequence in the world. The boundary is marked by a 1.5 cm-thick dark red clay layer with a thin gray-green sole at the base sandwiched between the last Cretaceous limestone containing large (up to 1 mm) planktonic foraminifera which are recognizable with a hand lens, and the first Paleogene limestone containing tiny (less than 0.1 mm) globigerinids not visible with a hand lens (Fig. 32). This constitutes a clear paleobiologic signature of the mass extinction event that took place in this deep marine environment at the K/Pg boundary. The white color of the top Cretaceous limestone has been attributed to iron reduction and leaching, and consequent bleaching of the oxidized, pink pelagic ooze, following a brief episode of anoxia at the water-sediment interface. This low-Eh condition was probably caused by anoxic bottom waters, rich in organic matter, which formed on the abyssal sea floor immediately after the mass killing of the marine plankton. The K/Pg boundary clay is made of various clay minerals, including illite, smectite, kaolinite, and mixed layered illite-smectite clay. In addition, the K/Pg boundary clay contains variable amounts of secondary calcite crystals together with microspherules made of K-feldspar, glaucony, and iron oxide, shocked quartz grains, and benthic foraminiferal tests.

Pg

marly intercalations that possibly; reactivated and inverted Jurassic synsedimentary extensional structures. Regional N-S right lateral and secondary E-W left lateral strike-slip faults dissect the entire chain and are interpreted as tear fault connected to the last stage of thrust sheet emplacement.

The crestal zone of the Mt. Nerone -Mt. Catria Anticline is complicated by prominent Jurassic faults, which define approximately N-S trending elongate highs of massive Jurassic carbonate platform, mantled by reduced pelagic deposits or condensed nodular carbonates. More or less complete basinal stratigraphic succession with middle-upper Jurassic to Cretaceous pelagic limestones characterize the basin's interposed lows.

STOP 2.1

The Jurassic/Cretaceous boundary at Bosso One of the best exposure of the Jurassic-Cretaceous (J/K) boundary in the Umbria-Marche Apennines is located along a road cut in the Bosso Gorge, near the town of Cagli. The boundary is found in the lowermost part of the Maiolica formation, which has a short, transitional lower contact with the underlying Calcari ad Aptici formation. The Calcari ad Aptici formation is characterized by thin bedded, pink-reddish cherty limestones, whereas the Maiolica formation is a typically white, medium-thick bedded, biomicritic limestone interbedded with, or containing, gray and whitish nodular cherts. The lithofacies contrast between the Calcari ad Aptici and Maiolica formations is sharp enough to suggest a major environmental change in this basin, which might correspond, indeed, to a significant explosion of the marine calcareous plankton.

Figura 34 -Outcrop view of the boundary between the Diaspri (D) and the Maiolica (M) formations at Bosso.

Figure 35 -Magnetostratigraphic profile across the J/K boundary at Bosso Gorge and summary results of magnetic, palaeomagnetic, lithostratigraphic and calpionellid data; 1, micritic limestone; 2, chert layers; 3, clayey limestone; 4, pink bioclastic limestone; 5, laminated bioclastic limestone (after Houša et al., 2004). The position of the boundary between the standard Crassicollaria and Calpionella zones is defined as the base of the first appearance of abundant minute, globular Calpionella alpina. At Bosso, the onset of Calpionella alpina is rather gradual, as is the disappearance of species of Crassicollaria and of Calpionella grandalpina. This significant event is located between Beds 76 and 79 of the section. The base of the standard C. alpina Subzone, hence also the J/K boundary, is therefore placed at the boundary between Beds 77 and 78. In relation to the magnetostratigraphic scale, the J/K boundary at Bosso lies approximately in the lower one-third of magnetozone M19n. This is in good agreement with the position of this boundary in other sections. The reason for the absence of calpionellids from the basal part of the section (Beds 1-45) is unknown, but this is a frequent phenomenon in basinal Maiolica successions of the Umbria-Marche Apennines. Calcareous sediments with abundant fragments of calcitic skeletal remains of Saccocoma and relatively well-preserved cysts of calcareous dinoflagellates indicate that the depositional environment was probably favourable for the preservation of microgranular tests of primitive calpionellids. The fact that calpionellids are not found suggests that they may not have been present during this period of deposition.

Figure 36 -Stratigraphic synthesis of the J/K boundary in the Bosso section. The biostratigraphy is based on calcareous nannofossils and calpionellids. Magnetostratigraphy is also available (after [START_REF] Montanari | Impact stratigraphy-The Italian record[END_REF].

STOP 2.2 The Aptian-Albian Fucoid Marls and the late Aptian-middle Albian organic-rich layers at Poggio le Guaine

STOP 2.3 The Maiolica-Fucoid Marls transition and the Selli Level (OAE 1a) at Gorgo a Cerbara

Figure 40 -The Selli Level (OAE 1a) at Gorgo a Cerbara. The Selli Level is a prominent, regional marker bed throughout the Umbria-Marche basin and the sedimentary expression of the OAE 1a. It is devoid of calcareous plankton and benthos and consists of olive-green to black mudstones and black, organic carbon-rich (up to about 10% of TOC), finely laminated shales, often rich in fish remains, pyrite nodules and/or radiolarians, alternated with radiolarian silty and sandy layers. The Selli Level can be subdivided into two lithological interval on the basis of colours. The dark, richest organic horizon characterizes its upper part. The Selli Level is sandwiched by silicified limestone beds, both of them some decimeters thick, which lack any of benthic life and a very depauperate planktonic foraminiferal assemblage extremely diluted by calcareous The distribution and composition of palaeocommunities lead to interpret these intervals" as periods of increased nutrient contents in the surface water and the Selli Level as a very high fertility event associated with depleted oxygenation at the sea bottom. Figure 44 -Stratigraphic profiles of Os and C isotope ratios and Re and Os concentrations in the Gorgo a Cerbara section. The Os isotope measurements across the Lower Aptian "Selli Level" black shale deposited during OAE 1a reveal two negative excursions in marine 187 Os/ 188 Os ratios within a period of 2 Ma starting above the Barremian-Aptian boundary and ending just above the Selli Level horizon, suggesting an order-of-magnitude increase in the global flux of unradiogenic Os. These results support the causative link between the emplacement of the Early Cretaceous Ontong Java Plateau and the marine biotic changes that culminated in the OAE 1a and are consistent with early and major phases of eruption of the Ontong Java Plateau. The latter phase is estimated to have been as short as ~1 Ma and may have induced widespread oceanic stratification that triggered OAE1a (after [START_REF] Tejada | Ontong Java Plateau eruption as a trigger for the early Aptian oceanic anoxic event[END_REF].

Geological framework of the Furlo area

The M.Pietralata -M. Paganuccio anticline -known as the Furlo structures after the gorge that crosses it -is located in the "Outer Ridge" of the UMA. The geology of the area has been well known since the XIX Century because of the very good exposure of a stratigraphic succession covering the period from the lower Jurassic to the Neogene along the Gorge. The stratigraphy is represented by lower Jurassic carbonate banks that underlie a middle-upper Jurassic condensed succession with slope facies indicating the presence of a structural high (known as Pelagic Carbonate Platform-PCP) located towards the SW with respect to the outcrops. The spatial geometry of the Jurassic slope and the reduced stratigraphic succession is observable in both sides of the anticline. In the lower quarry in the SW limb, Jurassic paleoslope stratigraphic and tectonic features dipping to NE are well preserved.

The Campanian-Maastrichtian Scaglia Rossa contains calcareous turbidites, mostly composed of planktonic foraminifera and ranging from some centimeters to some decimeters in thickness. These amalgamated turbidites have flute casts and cross bedding indicating a provenience from the SE. Important slumps, involving a few tens of meters of Cenomanian beds and including a triple Bonarelli level, are observable in the upper quarry. Other synsedimentary structures with soft-sediment deformation, detrital facies and several onlaps and truncations are present in the Turonian, Santonian and Campanian Scaglia Rossa.

The sedimentary facies and the paleomagnetic data suggest that these deformational events occurred during sediment consolidation in the early stages of diagenesis.

The anticline structure has regular continuity toward the SE and represents the internal boundary of the Pliocene Adriatic foredeep. The anticline is slightly vergent to the NE with the external limb is characterized by a progressively steeper dip and affected by blind thrusts that override the external structures for a few kilometers. The SW limb is affected by shallow thrusts rooted in the Paleocene Scaglia Rossa and by several N-S right lateral strike slip faults with offsets of hundreds of meters. A conjugate system of normal faults has downthrown the axial part of the anticline by a few hundred meters.

The upper Miocene sediments outcropping around the Furlo area postdate the upper Messinian when most of the anticline development took place. The regional marine Pliocene transgression is located a few tens of km to the East. Figure 51 -Rotated paleomagnetic declinations allow the recognition of otherwise obscure slides (from [START_REF] Montanari | Synsedimentary tectonics in the late Cretaceous-Early Tertiary pelagic basin of the Northern Apennines, Italy[END_REF].

June 6th The Monte Conero area

The Monte Cònero promontory is the eastermost anticline of the northern Apennine thrust-and-fold belt. It is located in the central part of the Pliocene foredeep. It is a highly asymmetric antiformal structure shaped by several strike slip faults. Here, the Umbria-marche carbonate sequence is exposed from the middle part of the Maiolica Formation all the way up to the Schlier Formation which reaches the very top of the Tortinian and is, therefore, laterally heteropic with the Marnoso-Arenacea and Laga flysch foramtions exposed elsewhere in the Umbria-Marche Apennines.

The sedimentary facies of the Scaglia Rossa at Monte Cònero is different from the equivalent unit of the classic Gubbio sequence. First, the Cretaceous portion of this foramtion exhibits a whitish-yellowish color instead of the typical pink of the Umbria-Marche facies. Second, the coccolith-foraminiferal biomicrites are interbedded with white calcarenitic and calciruditic tirbidites derived from a carbonate platform that was located a short distance to the east from the present day Cònero area. Thus, the Scaglia Rossa here represents a proximal facies characterized by lobate and strongly channelized carbonate turbidites and garin flows interfingering with the pelagic muds of the Umbria-marche deep-water basin at the toe of a carbonate apron.

Figure 1 -

 1 Figure 1 -Geological scheme of the Umbria -Marche Apennines.

Figure 2 -

 2 Figure 2-Stratigraphic and tectono-sedimentary synthesis of the Umbria-Marche succession (after Montanari & Koeberl, 2000).

Figure 3 -

 3 Figure 3 -Paleogeographic reconstruction at 150 MA (modified from Ron Blakey, NAU Geologyhttp://www2.nau.edu/rcb7).

Figure 4 -

 4 Figure 4 -Paleogeographic reconstruction at 75 MA (modified from Ron Blakey, NAU Geologyhttp://www2.nau.edu/rcb7).

Figure 6 -

 6 Figure 6 -Geological map of the Gubbio area (after Menichetti 1991).

Figure 7 -

 7 Figure 7 -Synoptic stratigraphic scheme of the Cretaceous of the Umbria-Marche basin(Coccioni, 1996, and unpublished data).

Figure 8 -

 8 Figure 8 -The Vispi Quarry in the Contessa Valley, near Gubbio, is the most spectacular outcrop of Cretaceous pelagic sediments in the Umbria-Marche Basin of Italy. Several organic-rich levels are recognizable: F = Faraoni Level (uppermost Hauterivian); S = Selli Level (OAE1a, early Aptian); MN = Monte Nerone Level and U = Urbino Level (OAE1b, early Albian); A = Amadeus Segment (OAE1c, late Albian); P = Pialli Level (OAE1d, latest Albian); B = Bonarelli Level (OAE2, latest Cenomanian).The position of the Cretaceous Oceanic Red Beds (ORBs) from 3 to 9 is also shown.

Figure 9 -

 9 Figure 9 -Detail of the upper part of Maiolica Fm in the Vispi Quarry . The main slump structures are highlight. Different levels of deformed synsedimentary structures can be recognize from thrust sheets, in the lower part, to folds, and to the chaotic levels. a -equal area stereonet with great circles of the detachment surfaces with the slip vectors; b -rose diagram of the groove direction; c -rose diagram of the fold axes; d -equal area stereonet with great circles of the calcite veins related to the fluid involved in the deformation. In the left the normal fault is related to the Pleistocene extensional tectonic phase affected the Gubbio structure.

Figure 10 -

 10 Figure 10 -Cartoon with the interpretation of the Aptian synsedimentary structures in the Gubbio area. (fromMenichetti, 2012)

Figure 11 -

 11 Figure 11 -The Bonarelli Level, about 1 m-thick, interbedded within the limestone beds of the Scaglia Bianca Formation in the Contessa Valley.

Figure 12 -

 12 Figure 12 -Carbonate carbon-and oxygen isotope stratigraphy and biostratigraphy of the Scaglia Bianca and Scaglia Rossa Formations in the Gubbio S2 core (after Tsikos et al., 2004).

Figure 14 -

 14 Figure 14 -Chemo-and biostratigraphic correlation between the Cenomanian-Turonian sections at Eastbourne (England), Tarfaya (Morocco) and Gubbio (Italy), and the proposed stratotype section in Pueblo, Colorado, USA. C-T boundary at Pueblo and Eastbourne fixed on the basis of ammonite stratigraphy. Pueblo data (except the first occurrence of Q. gartneri) from Kennedy et al. (2000) and references therein (after Tsikos et al., 2004):

Figure 16 -

 16 Figure16-Stratigraphy of the Bottaccione section interval including the Bonarelli Level plotted against the main events and the recognized phases (after[START_REF] Coccioni | Planktonic foraminifera and environmental changes across the Bonarelli Event (OAE 2, latest Cenomanian) in its type area: a high-resolution study from the Tethyan reference Bottaccione section (Gubbio, central Italy)[END_REF].

Figure 17 -

 17 Figure 17 -Lithologic log of the Contessa section plotted against samples location and the main radiolarian occurrences (after Bąk, 2011).

Figure 18 -

 18 Figure18-Part of the lithostratigraphic log of the Contessa section plotted against the carbon isotopic curves, Tu1-Tu6 carbon isotopic events and the main radiolarian first and last appearance data in the OAE2 and the Lower Turonian intervals (after[START_REF] Bąk | Tethyan radiolarians at the Cenomanian-Turonian Anoxic Event from the Apennines (Umbria-Marche) and the Outer Carpathians: Palaeoecological and Palaeoenvironmental implications[END_REF].

Figure 19 -

 19 Figure 19 -Stratigraphy of the Bottaccione section interval including the Bonarelli Level (BL) plotted against (A), radiolarian % abundance estimated on thin section (cross (x) corresponds to samples for which no thin section was produced); (B), radiolarian species diversity and (C), radiolarian preservation (after Musavu-Moussavou et al., 2007).

Figure 20 -

 20 Figure 20 -Lithostratigraphic detail of the Bonarelli level at Bottaccione, plotted against (A), radiolarian % abundance estimated on thin section (cross (x) corresponds to samples for which no thin section was produced); (B), radiolarian species diversity and (C), radiolarian preservation; (D), TOC values; (E), HI (mgHC/gTOC); (F), abundance of silica measured as quartz by infrared spectroscopy; (G), the curve of δ 13 C and (H), radiolarian events (after Musavu-Moussavou et al., 2007).

Figure 21 -

 21 Figure 21 -Ichnological features of the Bottaccione and Contessa sections, interpretation of oxygenation changes and their correlation. The gray shading in the ichnotaxa columns means reserved determinations, e.g., ?Thalassinoides sp. Total bioturbation means that 100% volume of sediment was bioturbated (after Monaco et al., 2012).

Figure 23 -

 23 Figure 23 -C33n/C34n boundary at Bottaccione Gorge

Figure 25 -

 25 Figure 25 -Location map of the Bottaccione section (after Premoli Silva & Sliter, 1995).

Figure 27 -

 27 Figure 27 -Virtual geomagnetic poles, magnetic declinations, inclinations, and resulting magnetostratigraphic interpretation from samples analyzed in the upper 35 m of Maastrichtian pelagic limestones in the Contessa section, and correlation with the restored magnetostratigraphic sequence of the classical Bottaccione section (after Chauris et al., 1998).A normal fault intersects the Bottaccione section at 328.5 m right within Chron C31n and shortens the Maastrichtian portion of this section of 10 m, which would correspond to a ~460 kyr stratigraphic gap. Due to the presence of this hiatus in the Bottaccione section, the Contessa Highway section constitutes a more complete late Campanian-Maastrichtian reference for magnetobiostratigraphy in the Tethyan realm (after[START_REF] Montanari | Impact stratigraphy-The Italian record[END_REF].

Figure 28 -

 28 Figure 28 -Stratigraphic synthesis of the mid-Maastrichtian environmental crisis in the Umbria-Marche pelagic basin (after Montanati & Koeberl, 2000).

Figure 29 -

 29 Figure 29 -'Inoceramid acme' (that is highest common occurrence) (HCO) and highest occurrence (HO) of inoceramid bivalves.

Figure 30 -

 30 Figure 30 -Stratigraphic synthesis and Iridium (Ir) abundance through a 10million-year long section across the Cretaceous/Paleogene boundary of the Bottaccione Gorge section (after Montanari and Koeberl, 2000).

Figure 31 -Figure 32 -

 3132 Figure 31 -The Cretaceous/Paleogene (K/Pg) boundary of the Bottaccione Gorge section.

Figure 37 -

 37 Figure 37 -Lower to Upper Albian Fucoidi Marls at poggio le Guaine M.Nerone.

Figure 38 -

 38 Figure38-Stratigraphic framework of the Poggio le Guaine core drilled on September 2010 with real stratigraphic depths according to bed dip measurements. Also shown are the occurrence and distribution of the organic-rich black shales including the marker beds resulting from Oceanic Anoxic Events (OAEs) and the discrete intervals where reddish colored beds become dominant (Cretaceous Oceanic Red Beds, CORBs) (after[START_REF] Coccioni | Umbria-Marche Basin, Central Italy: A Reference Section for the Aptian-Albian Interval at Low Latitudes[END_REF].

Figure 39 -

 39 Figure39-Stratigraphy of the Aptian-Albian Fucoidi Marls of the Poggio le Guaine/Bosso valley composite section. (after[START_REF] Coccioni | Stratigrafia, micropaleontologia e mineralogia delle Marne a Fucoidi delle sezioni di Poggio le Guaine e del Fiume Bosso (Appennino umbro-marchigiano). Atti 2° Convegno Internazionale "Fossili, Evoluzione, Ambiente[END_REF].

Figure 41 -

 41 Figure41-Detail of the Gorgo a Cerbara section across the Livello Selli with detailed lithology, sample position, and 'lower' and 'upper critical intervals' plotted against the estimated abundance of planktonic and benthonic foraminifera, nannoconids, and radiolarians. Note the distribution of Zygodiscus erectus. Legend: 1 -Marl, clayey marl, marly caly, bioturbated (a) and laminated (b) clay and/or claystone and marlstone; 2 -black shale; 3greenish-grey marly limestone; 4 -greyish-white limestone; 5 -whitish-grey limestone; 6radiolarian silty/sandy layer; 7 -chert nodules and layers (after[START_REF] Coccioni | Barremian-Aptian calcareous plankton biostratigraphy from the Gorgo a Cerbara section (Marche, Central Italy) and implications for plankton evolution[END_REF].

Figure 42 -

 42 Figure 42 -Virtual geomagnetic pole (VGP) latitudes at Gorgo a Cerbara, the proposed Barremian-Aptian boundary stratotype section. Open and closed symbols represent magnetization components defined by thermal and alternating field demagnetization, respectively. The Barremian-Aptian boundary has been designated to coincide with the base of polarity chron CM0 located about 3 m below the base of the Selli Level (after Channell et al., 2000).

Figure 43 -

 43 Figure 43 -Stratigraphic variations of inclination, declination, computed VGP latitude and magnetic polarity zones. In the stratigraphic column, the measured displacement of a normal fault at 57 m is restored. Magnetic polarity zones and subzones are progressively numbered from the section bottom (the correlative polarity chrons are in parentheses after the polarity zone labels). Uncertain polarity intervals are grey and cross hatched. The crosses indicate failed samples (after Speranza et al. 2005).

Figure 305 -

 305 Figure305-Stratigraphic variations in δ 13 Corg, initial isotopic ratios of Pb and Os for sediment samples ranging from the late Barremian through early Aptian at Gorgo a Cerbara. Pb isotopic ratios were calculated at 120 Ma. The Pb isotopic data, together with the prevously published Os isotopic record, provide new evidence for the eruptive history of OJP together with contemporaneous Pacific plateaus and its environmental consequences, starting from end-Barremian time and extending through early Aptian time (after[START_REF] Kuroda | Lead isotopic record of Barremian-Aptian marine sediments: Implications for large igneous provinces and the Aptian climatic crisis[END_REF].

Figure 316 -

 316 Figure 316 -Furlo lower quarry -The lithostratigraphic units : CoM -Corniola Massiccia ( Sinemurian p.p.-Lower Toarcian p.p.; Cg -Calcari stratificati Grigi (Lower Toarcian p.p.) ; RA -Rosso Ammonitico (Lower Toarcian p.p.-Upper Toarcian p.p.); B -Bugarone (Upper Toarcian pp -Lower Tithonian) ; M-Maiolica (Lower Tithonian -Lower Aptian); f -sedimentary dike -The red line indicate a N-S right lateral strike slip faults; dashed line indicates stratigraphic boundaries (after[START_REF] Cecca | Risultati preliminari del rilevamento nel settore sud-occidentale del foglio n. 280[END_REF]

Figure 48 -

 48 Figure 48 -The Upper quarry with the Scaglia Bianca and the Bonarelli level

Figure 49 -

 49 Figure 49 -Stratigraphic synthesis of the Scaglia Bianca-Scaglia Rossa transition at Furlo Upper Road (after Montanari & Koeberl, 2000).

Figure 50 -

 50 Figure 50 -Synsedimentary slides in Scaglia Bianca and Scaglia Rossa exposed along the road cut and in the upper quarry (from Alvarez & Lowrie, 1984).

Figure 5232

 5232 Figure 5232 --Itinerary of the day with the stops.

Figure 334 -

 334 Figure334-The K/Pg boundary at Fonte d'Olio Quarry. The K/Pg boundary is exposed in numerous localities in the Cònero area, but the best section can be found in this quarry located near the town of Sirolo. Here the K/Pg boundary is located about 80 cm below a 2-3 m thick calcirudite marker bed called "Mega T" and is marked by a 1.8 cm greenish clay layer sandwiched between pelagic limestones. Apart from their withish or creamy color, the texture and microfacies of the top Cretaceous limestone and the basal Paleogene, porcellanaceous limestone are identical to those seen in other Umbria-Marche sections. These light colors are due to a relatively more reduced state of the paleosea floor compared to the well-oxygenated environments expressed by the typically pink Scaglia Rossa. Higher plankton productivity and upwellin in this proximal environment may have been the main reasons for more reduced conditions on the sea floor in respect to other open sea, deeper areas of the paleobasin.

Figure 5735 -

 5735 Figure 5735 -Synoptic stratigraphic scheme of the Massignano global stratotype section and point (GSSP) for the Eocene-Oligocene boundary (after Coccioni et al., 2009).

Figure 368 -

 368 Figure 368 -Panoramic view of the "Pirolo" promontory and "due sorelle" rocks. The dip slope beddings are in Maiolica (M), while Fucoid Marls (MF), Scaglia Bianca (SB) and Scaglia Rossa (SR) outcrop in the eastern part on the sea cliff .

JUNE 5 th 2013 The Monte Nerone-Monte Catria and Furlo area

Geological framework of the Monte Nerone-Monte Petrano and Montiego area

The UMA, where the Meso-Cenozoic carbonate succession is exposed, consists of two main ridges separated by a hilly zone: the westernmost inner ridge of the UMA and the outer ridge are part of the eastern flank of the Marche Apennines. These ridges are composed of anticlinal structures that override, to various degrees, the adjoining synclinal zones to the NE. The "Inner Ridge" consists of juxtaposed en echelon brachyanticlines, while the "Outer Ridge" is characterized by a longitudinally more continuous anticlinal structure. To the NW the Inner Ridge is comprised of the Mt. Nerone -Mt.Catria and Montiego anticlines.

Typically, these 5 km-wide, asymmetric NE-vergent boxshaped anticlines have progressively vertical NE flanks that are affected by thrusts, override the intervening synclinal zones. Secondary detachment and disharmony levels are localized in correspondence with the


Salma Bergaoui
email: salma.bergaoui@cea.fr

Ivan Llopard
email: ivan.llopard@cea.fr

Nicolas Hili
email: nicolas.hili@imag.fr

Christian Fabre
email: christian.fabre1@cea.fr

Fayçal Benaziz
email: faycal.benaziz@cea.fr

Tool Support for a Method and a Language Integrating Model Refinements and Project Management

Keywords: Embedded Systems, Development Processes, Methods & Tools, Project Management, Model-Based System Engineering, Parallelism, Action Language

Complexity of Embedded System (ES) development is increasing due of several cumulative sources. Some of them are directly related to constraints on the ESs themselves, like computing power, resource constraints, and multi-or many-core programming, while other are related to the industrial context, like teamwork and parallelisation of concurrent development. In this paper we present CanHOE2, a Model-Driven Engineering (MDE) tool that addresses two issues of ES development: expression of parallelism by means of objects and Hierachical State Machines (HSMs), and teamwork synchronisation.

Introduction

Embedded System (ES) development teams have to cope with usual constraints of industrial organizations:

(1) End-to-End Engineering: the full development cycle goes from requirement formalization to the final integration and assessment of the application on its platform. [START_REF] Hili | A Model-Driven Approach for Embedded System Prototyping and Design[END_REF] Incremental & collaborative development: To organize efficiently the work of large teams, it is critical to regularly distribute and integrate work, and to measure progress towards the objectives. (3) Moreover, at any level, models should be executable and instrumented: executable to check them against requirements, and instrumented to get continuous qualitative and/or quantitative feedback to drive engineering decisions.

Another important factor of ES development efficiency is the set of modeling and programming languages used in a project. Ideally, we would rely on a single high-level modeling language that: (a) Can model hardware as well as software; (b) Is not tied to any hardware architecture like Field-Programmable Gate Array (FPGA), Digital Signal Processor (DSP) or General Purpose Processor (GPP); (c) Is parallelfriendly; (d) Provides a clear path to generate efficient code.

Lastly, the wide variety of modern platform patterns like manycore platforms with distributed memory based on Globally Asynchronous, Locally Synchronous (GALS) and Network-on-Chip (NoC) are increasingly heterogeneous and thus much more difficult to program than classical shared memory architectures. For these new architectures, parallelism has to be exposed; their distributed architecture requires strong partitioning of the code and calls for message-passing style of programming. At the same time, modern embedded applications cannot be divided between data/computational parts and control parts anymore. Instead, they are made of a number of layers that include both parallel computations on large data sets and data-dependent control as well.

In this context, we developped a Model-Driven Engineering (MDE) approach named "Highly Heterogeneous, Object-Oriented, Efficient Engineering" or HOE 2 for short. The approach is made of:

• A method that provides modeling concepts necessary to describe heterogeneous embedded systems. The HOE 2 method provides a set of related project management entities and metrics to organize, track and report on the development efforts [START_REF] Hili | Efficient Embedded System Development: A Workbench for an Integrated Methodology[END_REF][START_REF] Hili | A Model-Driven Approach for Embedded System Prototyping and Design[END_REF][START_REF] Hili | Model-Based Platform Composition for Embedded System Design[END_REF].

• An action language that seamlessly combines association-based data parallelism and operations on compound data [START_REF] Llopard | A Parallel Action Language for Embedded Applications and Its Compilation Flow[END_REF]. The HOE 2 language preserves the expressiveness of Statecharts [START_REF] Harel | Statecharts: a Visual Formalism for Complex Systems[END_REF], and captures a layout -and implementation -neutral description of data organization, extends message passing with an intuitive semantics for this additional parallelism and provides strong foundation for array-based optimization techniques. This paper is structured as follow. We review some related works in Section 2. Section 3 introduces the context of our approach. In Section 4, we present the CanHOE2 tool, its main features, design choices and implementation. Section 5 presents its application on a specific case study, and we conclude in Section 6 with perspectives and future work.

Related Work

Over the past years, many methods and tools were proposed in order to model embedded systems [START_REF] Gérard | Modélisation UML exécutable pour les systèmes embarqués de l'automobile[END_REF][START_REF] Aulagnier | SoC/SoPC development using MDD and MARTE profile[END_REF][START_REF] Basu | Rigorous Component-Based System Design Using the BIP Framework[END_REF].

ACCORD/UML is a model-based method proposed to model real-time application models in the automative area [START_REF] Gérard | Modélisation UML exécutable pour les systèmes embarqués de l'automobile[END_REF][START_REF] Aulagnier | SoC/SoPC development using MDD and MARTE profile[END_REF]. It is organized around waterfall lifecyles and implies several stakeholders such as car and parts manufacturers.

BIP (for Behavior, Interaction and Priority) is a framework for composing hierarchical systems [START_REF] Basu | Rigorous Component-Based System Design Using the BIP Framework[END_REF]. It permits to build composite systems by hierarchically assembling atomic components that are described in terms of behavior and interactions. BIP defines an activity-based process in which a few set of activities is defined, for designing application models, integrating platform's constraints, generating code and for verifying the system.

MopCom is a model-based development method for designing ESs [START_REF] Aulagnier | SoC/SoPC development using MDD and MARTE profile[END_REF]. It proposes a top-down process divided up into two flows for enhancing the development parallelism, and several iterations to refine an application model onto several abstraction layers of a platform.

In all these methods, processes are defined alongside generic or specific tools. Tools are used in order to support both the language used for modeling ESs, and the process with its different features (parallelism, multi-roles, etc.). However, there are several drawbacks. Tools are often generic and do not cover all the activities of an ES process. Coupling several tools can permit to cover the whole process, yet is inefficient for modeling ESs. Using non-dedicated tools hinders the development as they do not provide a global and coherent view of the developed system throughout the whole process. Hence, they allow designers to digress from the canonical process. In addition to that, they do not integrate any project management features a project manager could benefit from in order to have a global understanding of a current development and to monitor it. There is now a need of developing Integrated Development Environments (IDEs) that address all these issues in one go.

On the tool side, "IBM Rhapsody", from IBM/Rational, provides an IDE to develop UML or SysML models that is widely deployed in the industry [START_REF]Rhapsody[END_REF]. The dynamic behavior of an object is captured in a flavor of Finite-State Machine (FSM) where the transitions' actions are called by external libraries developed in a general-purpose language. The FSM can be translated into C++ code, compiled and executed. During development, this code calls back into the IDE for debug and animation of the execution, e.g. with sequence diagrams. Several Board-Support Packages (BSPs) are also available such that the generated code can be compiled, uploaded and executed on various embedded platforms. Other tools from IBM, such as "Rules Composer" permit to define specific code generators from Rhapsody models [START_REF]Rules Composer[END_REF]. The mixed semantics of these tools, with FSM and C++ libraries, do not allow for symbolic reasoning at the model level, be it for optimization, correctness analysis or model refinement. Although they do support MDE, they main target is executable code production.

"Papyrus MDT" [START_REF] Gérard | Papyrus: A UML2 tool for Domain-Specific Language Modeling[END_REF][START_REF] Gérard | On the Papyrus' USE: Usage, Specialization and Extension[END_REF] is a component of the Eclipse Model Development Tools (MDT) project. It is a complete solution for UML modeling and is fully compliant with the latest versions of the UML standard. It supports the definition of profiles, and their applications to tailor UML models to a particular domain. Papyrus provides some tools to customize the whole modeling environment of Eclipse (i.e. editors, palettes, the model explorer and the property panel) according to the definition of the profile. Thus, designers can design models in a dedicated environment using specific profiles. However, the customization is only performed regarding the dedicated language and disregarding any process that could be combined to the dedicated language. Hence, Papyrus could be tailored to a specific language, but not to a specific method. From the model execution side, Papyrus provides code generation engines for C++ and Java. However, it focuses on structural elements and only provides a limited support for code generation from behavior models through "Qompass Designer" [START_REF]Papyrus Qompass[END_REF]. That means, as the authors state [START_REF]Papyrus/Codegen/Cpp description[END_REF], Qompass Designer only supports simple FSM models and it is currently not possible to produce code from hierarchical FSM models.

Context

CanHOE2 supports and implements the HOE 2 method.

The HOE 2 Method

HOE 2 stands for Highly Heterogeneous Object Oriented Efficient Engineering. The HOE 2 method is organized around four models and three refinements, that defines a set of successive activities with clear inputs and outputs -See Fig. 1 In terms of associated process management, we define the following concepts:

• Task, Phase and Task Sheets: A task is an atomic modeling activity: one of the three refinements applied to a single objet. A phase is the set of tasks that captures all the refinements that build the phase's model. A task sheet is an instance of a task.

• Participant: A participant may be either a Project Manager (PM) or a Developer. A PM creates and drives the project by (a) defining and assigning tasks to Developers, and (b) by integrating, or rejecting, the models they produce. A Developer can modify models only according to a task sheets provided by the PM.

• Project: A project contains its task sheets and the four phases of the process. A project is led by a single PM and built by several Developers.

• Iteration: An iteration is a collection of tasks. It is the smallest entity of project management. Table 1 illustrates an example of a consistent planning using the iterations as a diagram similar to a Gantt where T i j denotes the i th task of iteration j. The same kind of planing can be declined for the development of the platform. As can be seen, the iterations form rectangles and squares in the table schedule: Each iteration starts from a consistant state and ends by a consistant state of the system. However, this kind of representation does not illustrate the refinements within a single iteration.

Table 1: Consistent Planning of developments RA SA SD SI U C 1 SN 1 1 T 1 1 T 2 1 T 6 3 T 8 4 U C 2 SN 1 2 U C 3 SN 2 3 T 3 2 T 4 2 T 7 3 SN 3 3 U C 4 SN 1 4 U C 5 SN 1 5 T 5 2 SE 2 5 SE 3 5 U C 6 SN 1 6

HOE 2 -A New Action Language for HSM

The HOE 2 language build on a number of concepts from Unified Modeling Language (UML) such as objects and associations [START_REF] Llopard | A Parallel Action Language for Embedded Applications and Its Compilation Flow[END_REF][START_REF]OMG Systems Modeling Language (OMG SysML)[END_REF]. HOE 2 Objects communicate through exchange of messages. Their behavior is captured by Harel's Statecharts [START_REF] Harel | Statecharts: a Visual Formalism for Complex Systems[END_REF][START_REF]OMG Systems Modeling Language (OMG SysML)[END_REF]. The HOE 2 language proposes a number of extensions to UML:

• A new Action language. The HOE 2 action language separates actions into two sequentially ordered parts: First the parallel updates of associations, followed by a parallel sending of messages -See Fig. 2.

• Using associations to define Iteration domains and Indexes. HOE 2 introduces a syntax for the specification of parallel iteration domains for associations updates and sending actions.

• Indexed regions: Iteration domains can also be used to enumerate parallel regions. Each region is identified by its own index.

• Transaction: The concept of interface is extended with the ordering and direction of messages exchanged.

These extensions are detailled by Llopard et al. [START_REF] Llopard | A Parallel Action Language for Embedded Applications and Its Compilation Flow[END_REF].

The CanHOE2 Tool

As we explained previously, CanHOE2 serves to support the HOE 2 process and language. We choose to develop our tool with the several Eclipse technologies [START_REF]The Eclipse Foundation[END_REF][START_REF]Xtext: a Framework for Development of Programming Languages and Domain Specific Languages[END_REF][START_REF]Sirius: an Eclipse Project which Allows the Creation of Graphical Modeling Workbench by Leveraging the Eclipse Modeling Technologies[END_REF] It is suitable for metamodels and model exchanges. CanHOE2 also offers a textual editor for the HOE 2 language. In this section, we detail the implementation choices, interface design and contributions of our tool.

Tool Design

CanHOE2 provides four editors corresponding to the four models described in the HOE 2 method (see Fig. 1). Navigation in the models is based on the logical ordering of refinements within models. The project management tool supports consistent planning and definition of iterations obeying the model refinement dependencies. The iteration history is navigable. The user interface is split into three areas at a minimum (see Fig. 3):

• The Navigator Area, that allows the designer to intuitively navigate inside a streamlined hierarchy of HOE 2 artefacts.

• The Editor Area: where the developer can write program using graphical elements or textual coding.

• The View Area, dedicated to project management and teamwork tools. It implements dedicated views to update information about the entities selected in the active editor.

As illustrated in Fig. 4, the developer may either write its program directly in HOE 2 textual language or describe it graphically, assisted by a palette and a property panel: a palette is displayed and the developer is able to drag and drop entities from it. Information about graphical entities can be modified in the graphical editor, or in a property panel. Graphic and textual development can be complementary. Indeed, the developer can mix user friendly textual and graphics solutions, they will be automatically synchronized to each backup (see Fig. 4). By double-clicking on any graphical element, an embedded HOE 2 language editor open up and let the programmer modify the actual code (see Fig. 5).

Tool Implementation

The first step is to derive a well-formatted Ecore metamodel from our canonical one. This step is fundamental since we need to consider the Ecore and its associated tool specificities. Once we have produced our Ecore metamodel, we defined the HOE 2 language syntax using Xtext/Xtend technology from the above defined Ecore model [START_REF]Xtext: a Framework for Development of Programming Languages and Domain Specific Languages[END_REF]. Xtext provides a set of tools for the implementation of domain-specific languages.

From the HOE 2 metamodel, we derived a full concrete implementation of it. The compiler components of our language are independent of Eclipse or OSGi and can be used in any Java compliant environment. Xtext automatically generates the parser, a type-safe builder of our Abstract Syntax Tree (AST), the serializer and code formatter, the scoping framework and the text editor. The editor integrates syntax highlighting and error checking, among many other things. To achieve graphical models, we rely on the Sirius framework [START_REF]Sirius: an Eclipse Project which Allows the Creation of Graphical Modeling Workbench by Leveraging the Eclipse Modeling Technologies[END_REF]. Sirius enables the visual design of complex systems (software, business activities, physics, etc.) and guarantees the consistency of the corresponding data (architecture, component properties, etc.).

Support Tools for Project Management in CanHOE2

CanHOE2 offers several tools to support project management. Indeed, it can manage the authentification and collaborative work providing a global view on the progress of the project.

Authentication. In a regular work environment, an employee can only access the projects to which he has been assigned. In CanHOE2, once authenticated, the user accesses a personal dashboard that lists the projects in which he is involved. From this dashboard, he can also create new projects as a PM. According to his role in the project, one of two perspectives is opened: "Project Manager" or "Developer" perspective. A perspective is a window with adapted views to the user. Eclipse RCP can easily manage these perspectives and allow us to show a proper layout of the available views. The views in CanHOE2 are based on Java SWT [START_REF]SWT : an open source widget toolkit for Java designed to provide efficient[END_REF].

The user authentication process goes through Lightweight Directory Access Protocol (LDAP). LDAP is a network protocol for accessing an electronic directory where you can reference the users (name, login, phone ...), machines or applications. Access to LDAP server is done via Java Naming and Directory Interface (JNDI) [START_REF]Java Naming and Directory Interface[END_REF].

Collaborative development. Such a collaborative environment needs a database to capture all the artifacts manipulated and their evolution over time. CanHOE2 uses centralized Git repositories to this end that are accessed by CanHOE2 on behalf of each participant [START_REF]Git: a Free and Open Source Distributed Version Control System[END_REF]. CanHOE2 uses two types of repositories:

• A configuration Git repository contains the infor- • Several project-specific Git repositories, where we store additional information about the project (task sheets) and resulting patterns of the Can-HOE2 application (model use cases, scenarios).

Project monitoring. In order to help the project manager to monitor the project development and to plan different iterations on it, we implement traditional diagrams for project management such as GANTT and PERT diagrams. Internalized project management reduces development time and provides a monitoring interface to better manage the development team.

Case Study

In this section, we introduce a Face Tracker system. The face tracker system consists of application for face detection, which is hosted by an Oriented Camera platform. This platform includes a general purpose processing unit, a Passive InfraRed (PIR) sensor and a bracket on which the camera is attached. Two servomotors orientate the bracket for pan and tilt.

Fig. 3 illustrates use cases diagram of the Face Tracker application . Tables 2 and3 show multiple use cases and scenarios, respectively, that formalizes the requirements. From these use cases and scenarios, we can now define a task list and its corresponding order of execution. We present hereafter a non-exhaustive list of tasks that have to be performed:

• T 1 : Refinement of UC 1 & 2 • T 2 : Initiation of the system analysis • T 3 : Refinement of UC 3, 4, 5 & 6
• T 4 : Refinement of the system analyis for UC 3 & 4

• T 5 : Refinement of the system analyis for UC 5 & 6

• T 6 : Initiation of the system design • T 7 : Refinement of the system design • T 8 : System implementation Once this list is completed, we can define the execution priority of tasks and hence the list of our different iterations.

• I 1 = T 1 + T 2 : Refinement of the use cases 1 & 2 and system analysis initiation In what follows, we will focus on I 1 and I 3 iterations. However, before the beginning of the design phase (i.e. iteration I 3 ), the platform development team have to start to work on it. We will call that iteration I 1 . We named our platform, "The Oriented Camera platform".

Conclusion & Perspectives

The HOE 2 method defines a single process used to develop both applications and platforms. It defines precisely what information is sent from the platform model to the application model during development. Its companion language suports parallelism and is amendable to polyhedral analyses. It is made of (1) a new action language limited to association updates and sending of messages, (2) domains, iterators and indexes based on associations.

In this paper, we presented CanHOE2, a modelling and process management tool for the HOE 2 method and its language. Its main contribution is that not only does it supports the HOE 2 language, as any modelling tool, but also the associated process. The In future work, we want to extend CanHOE2 with more support for the method, in particular towards the models simulation and HOE 2 model-to-model transformations.

  [START_REF] Hili | Efficient Embedded System Development: A Workbench for an Integrated Methodology[END_REF][START_REF] Hili | A Model-Driven Approach for Embedded System Prototyping and Design[END_REF][START_REF] Hili | Model-Based Platform Composition for Embedded System Design[END_REF]. These models are built as follows: (A) The informal requirements are formalized in the Requirement Model by means of System, Actors, Use Cases and Scenarios; (B) This requiement model is then refined into an executable, platform independent, Analysis Model. This is done by means of Hierarchical Opening of objects: replachttps://hal-cea.archives-ouvertes.fr/cea-01236474 ing an object viewed as black box with several object that represent a more detailed version of the orginal object while collectively exhibiting the same apparent behavior. This transformation can be applied recursively to new objects. (C) The Platform is partially introduced by declaring its Worlds -See (1) in Fig.1. A world is an abstraction of an execution domain that can Hosts objects -like a set of processors and their shared memory, a FPGA, or a dedicated hardware Intellectual Property (IP). Once the platforms's worlds are known, the Design Model is built. For this, each object from the analysis model is split in smaller objects that are Distributed over the platform's worlds. (D) Further platform details are introduced into the application: for each world, its Containers are provided. Each container embodies a set of coding rules, with a trade-off, to implement an object semantics on the target world. The Implementation Model is built by Injecting each object of the design model into a container.

Figure 2 :

 2 Figure 2: HOE 2 Action Language

Figure 1 :

 1 Figure 1: HOE 2 a Collaborative Top-Down Dev. Process for Embedded System Design: Application and Platform Tracks

Figure 5 :

 5 Figure 5: Embedded Editor for Transition

Figure 3 :

 3 Figure 3: The CanHOE2 Interface Dedicated to the HOE 2 Method and Language

Figure 4 :

 4 Figure 4: CanHOE2 Synchronized Text and Graphical Editors

• I 2 = T 3 + T 4 + T 5 :

 2345 Refinement of requirements and system analysis• I 3 = T 6 + T 7 : System design • I 4 = T 8 : System implementation

Figure 8 :

 8 Figure 8: Oriented Camera Platform Analysis

Figure 9 :

 9 Figure 9: Oriented Camera Platform Composition

Figure 10 :

 10 Figure 10: Face Tracker system design

  principles of HOE 2 for efficient management of projects. It is canonical in the sense that it aims at illustrating the main points of the method.

	January 27-29, 2016	ERTS 2 2016	Toulouse, France
			c 2015, CEA

• A canonical tool named CanHOE2 that combines textual and visual programming while enforcing https://hal-cea.archives-ouvertes.fr/cea-01236474 1/9 the

Table 2 :

 2 Usecases of the Face Detection Application

	Id	Causality	Name
			Description
	1	Primary	Detect presence
	The actor wants to know when somebody enter the monitored
	zone.
	2	Primary	Track faces
	The actor wants to track faces of people entering the moni-
	tored zone.
	3	Secondary	Toggle camera control
	The actor wants to switch between manual and automatic
	tracking modes
	4	Secondary	Query camera control mode
	The actor wants to know the current tracking mode
	5	Secondary	Orientate camera
	The actor set the camera's orientation.
	6	Secondary	Query camera orientation
	The actor wants to know the camera's curent orientation.

Table 1

 1

illustrates our iterations planning.

https://hal-cea.archives-ouvertes.fr/cea-01236474 6/9 c 2015, CEA

The I 3 iteration initializes and starts the system design phase satisfying the separation of objects, into the two worlds of the platform (See Fig.10).

Aknowledgements: This work was partially funded by the Artemis-JU and the French "Ministère de l'économie, de l'industrie et du numérique" for the Artemis project COPCAMS, GA 332 913, http://copcams.eu.

January 27-29, 2016

ERTS 2 2016 Toulouse, France Nominal Presence detected notification The actor subscribes for updates of presence in the monitored zone. The application notifies to the user when somebody enters or exit the monitored zone. The actor unsubscribes when he does not want updates anymore.

2-1

Nominal Face tracking notification The actor subscribe to people's faces and the position in the monitored zone. The application notifies to the user with the position of a face in the monitored zone every 2 s. The actor unsubscribes when he does not want to track people faces anymore.

3-1

Nominal Switching to automatic mode The system is in manual mode. The user toggles it to automatic mode.

3-2

Nominal Switching to manual mode The system is in automatic mode. The user toggles it to manual mode.

4-1

Nominal Querying control mode The actor asks for the camera's control mode. The system answers wether the camera is in automatic or manual mode.

5-1

Nominal Manually orienting the camera The system is in manual mode. The user wants to move the camera relative to the curent position. The camera is moved by the requested pan and tilt angles.

5-2

Error Manually orienting while in auto. mode The system is in automatic mode. The user wants to move the camera relative to the curent position. The system refuses because the camera is in automatic mode.

5-3

Error Manually orienting the cam. hits a stop The system is in manual mode. The user wants to move the camera relative to the curent position. The camera is moved by less than the requested pan and tilt angles as it hits a hard stop.

6-1

Nominal Camera position query The actor asks the system about the camera position. The system answers with the position.

Iteration I 1 : Refinement of the use cases 1&2 and system analysis initiation

During this iteration, we can detail the use cases identified but also initiate the analysis phase. Fig. 6 illustrates an analysis model of the Face Tracker system : the system is composed by three objects (1) a presence detector for detecting a presence in a specific area, (2) a face detector for detecting a face and its position from a video stream and (3) a turret controller for controlling the orientation of a camera a controllable turret two angles.

In this iteration we have also to model the behavior of our application, and its response to exchanged messages (See Fig. 7).

Iteration I 1 : Requirements and system analysis of the platform Tables 4 and5 gives a list of use cases and scenarios of the platform. These lists can be completed and refined with theirs corresponding diagrams.

To model the platform, we use the same diagram for • The Raspberry PI platform: It is adapted to the field of image processing and allows installing and uninstalling Python programs running one program at a time. It allows also the update of time and date settings.

• The turret control platform: This platform provides the use cases (1) subscribtion to presence detection, and (2) turret orientation. The turret can be used to support the sensors or actuators, such as a camera, an ultrasonic radar, a projector, etc.

• The Arduino UNO platform: It is a prototyping platform for the control of sensors and, digital or analog actuators.

From these three platforms we have designed the composition diagram (see Fig. 9). From this level of modeling we can start the system design.

1-2

Error Firmware installation error A firmware is already installed on the platform. The actor wants to install the same version or an older version of the firmware. The firmware cannot be installed.

2-1

Nominal Toggle the application on/off The actor turn on the application. The application runs till the actor decides to turn off the application. The application is switched off.

5-1

Nominal Firmware version query The actor asks the system about the firmware. The system answers with the firmware version.