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Considerations geological, geomorphological and tectonic Tremiti

Balocchi P. (1) & De Luca G. (2)

Summary: The Tremiti recall every year thousands of tourists from around the world. The wonders seen, admired and photographed every day are nothing more than the effect of the course of nature over millions of years. Tourist experience comes a detailed study of the formation and history of the archipelago from a geological point of view and lithology. A tourist route with a high scientific content.

(1) Geologist GeoResearch Center of Italy - geoblog (website: http://www.geobalocchi.blogspot.com/ ) (2) Survey e collaboratore del GeoResearch Center Italy - GeoBlog (sito internet: http://www.ricercasperimentale.blogspot.com/ ).

Introduzione
L'Arcipelago delle Tremiti è costituito da tre isole più grandi (San Domino, San Nicola, Caprara), da un isolotto più piccolo (Cretaccio) e da un'ulteriore small island moved eastward about 10 miles (20 kilometers), called Pianosa. The archipelago is located north of the Gargano Peninsula and 12 miles (22 kilometers) off the coast of Molise.
It is therefore small islands (two square kilometers the largest island of San Domino) easily walkable and circumnavigation in two hours using small boats.

aspects
lithological succession is characterized by outcrops of marine sedimentary lithologies ranging in age from the Paleocene and the Pliocene followed on average, in angular unconformity (Unconformity angular), a succession of continental clastic Pleistocene Upper-Middle (Fig. 1).

The marine succession is mainly represented by a series limestone, dolomitic limestone and limestone-marl passing up a series of lists and the open sea with flint nodules, to close with neritic environment of the calcarenites . From bottom to top, are the following distinct lithological units (SELL, 1971, Channell, 1979; Brozzetti, 2006): Formation of the Bue Marino (dolomite and limestone and calcarenites bioconstructions organogenic neritic environment; Paleocene upper), Training Caprara (compact dolomite with chert nodules and lists of the pelagic environment; Eocene) Formation of San Domino (including a number of lithofacies Low water: organogenic limestones and calcarenites in nummulites bioconstructions; lower-middle Eocene) Formation of Cretaccio (dolomitic limestone and marl glauconitiche yellow, yellow-whitish, the environment variable from coast to open sea; Langhian-Messinian pp), Training San Nicola (dolomitic limestone in the formation of angular unconformity Cretaccio organogenic limestone and the roof of sea bass and richly bioclastic, pp Messinian, middle Pliocene) (Fig. 2).

The continental deposits (Ram, 1989; Brozzetti, 2006), rarely surfacing in complete sequence, are characterized by underlying calcareous conglomerates (Middle Pleistocene), followed by a few meters of limestone Marly (Middle Pleistocene), and a succession of sandy-silty deposits of wind (Loess and Loess Red Yellow Middle Pleistocene-sup., of the Upper Pleistocene Loess Bruno.) sporadic intercalations containing gravel. Finally, resulting from the decalcification of the typical loess "croutons" interleaved at several levels within the continental succession.

aspects
Islands tectonic quakes occur with a dipping stratigraphy to the SE (south coast of San Domino in fig. 3) NE-SW direction and defining an emphasis on monoclonal (Fig. 4), which represents the southern flank of a loose fold with vertical axial plane and hinge line with direction N60 (p-diagram greek fig. 1) (SELL, 1971, Ram, 1989; Brozzetti, 2006).

This structural setting is clearly visible on the island of Caprara (Fig. 4) showing the planar surface topography and slightly tilted to the south plunging into the Adriatic Sea, while to the north the coast is steeper and shows irregular .

NO Along the coast of the island of San Nicola is visible in the contact between the formation of angular unconformity and the overlying formation Cretaccio San Nicola (Fig. 5). Note the large fold that deforms the Formation of Cretaccio and normal faults that cut both formations.

Other structures are visible at the Grotta del Bue Marino (fig. 6 and 7) where you can see both the stratigraphic dip SE, has many faults.

An interesting structure is the "presumed fault probably active" localized outcropping in the upper part of the island of San Nicola (Fig. 8). Rejection (moving two blocks) and probably represents a transcurrent movement left, highlighted by the step that has formed between the two blocs. In fact, in the non-activity of the fault (fault stops and not moving), the erosion would have even without the two blocks show the step (Panizzi, 1995; Panizzi, 1988).

From a geomorphological point of view of geography and morphology of coastal tourism is the one that attracts the visitor, becoming the predominant element of the landscape.
This morphology may be contained in three main morphotypes:

• a high cliff coast : characterized by the presence of a vertical slope (above the sea) generally rocky and formed by the erosive action of waves on rocks (fig . 5 and 9);
• low rocky shore slopes gently into the sea : often the shoreline is jagged and broken into large bays (Fig. 3, 4 and 10);
• low sandy coast: the only presence is in Arenas set the island of San Domino.
  
  

may be separated if the escarpment cliffs lives is in direct contact with the sea and subject to the processes of marine erosion (Fig. 5 and 9). When the foot of the slope sediments accumulate (of different nature: sandy shoreline, slope debris, landslides) that separate from the sea and thus the erosion of the waves does not change its shape, it is called dead cliff (Fig. 11).
The process of formation of a cliff can be outlined below (Panizzi, 1995) (Fig. 12):

• Escarpment in direct contact with the sea, where the processes of chemical weathering and physical disintegration accentuate the cracks in the rocks the top of the cliff;
• actions marine erosion dig a furrow of the hinged base of the cliff (Fig. 13);
• collapse of a portion of the escarpment;
• accumulation of debris at the foot of the cliff that can be removed from the waves and then the process continues (cliff alive), or if the deposits persist without being removed, protect the base of the slope, resulting in an erosion of the sea cliff died.

Other characteristic forms of the islands are represented by numerous coves along the coast to form small coves called "set" (Cala del Bue Marino, fig. 6 and 7, Cala of Moray fig. 13, the English Cala, Cala of the Swallows, etc.).. Associated with them are the numerous caves of karst coasts located mostly along the coasts of the island of San Domino.
La Grotta del Bue Marino (fig. 6 and 7) is a hollow dome-shaped rounded and slightly elongated in the direction NE-SW. The entrance to the sea is narrow and low. La Grotta delle Viole (Fig. 14) appears as a round shape with a cavity opening to the sea and of rectangular shape (the shape of the opening is influenced by stratification), while the terminal portion of the cave opens up , showing the sky (well, cave, fig. 14 and 15).
The genesis of the caves (Castiglione, 1978; Panizzi, 1995) of San Domino is related to the dissolution of carbonate rocks by rain water that alter the lithologies on the surface topography and the sea water attacks from below. As a result loosely formed cavities within the rock si allargano formando, inizialmente, una piccola grotta generalmente a forma di cupola e invasa dalle acque marine (a testimonianza che il carsismo procede dal basso, per maggiore alterazione chimica da parte dell’acqua del mare). L’assottigliamento della volta, in tempi successivi, provoca il suo collasso per gravità formando un’apertura verso l’alto. I detriti che si depositano all’interno del piccolo bacino possono essere successivamente allontanati per effetto del trasporto da parte del moto ondoso.

La diversità tra le grotte lungo la costa NO e quelle lungo la costa SE di San Domino è legata alla struttura monoclinalica dell’isola (rilievo a cuesta; PANIZZA, 1995). Infatti a SE le coste sono basse e i processi di dissoluzione con maggiore facilità possono formare delle grotte a pozzo con la volta collassata, mentre lungo le coste alte a NO, la successiole stratigrafica presenta uno spessore maggiore e quindi più resistente ai processi di alterazione permettendo il formarsi di grotte a cupola (in prossimità del mare) e non a pozzo con il succesivo collasso della volta.
Con molta probabilità le piccole baie dell’isola di San Domino, possono essersi formate a causa dei processi carsici che inizialmente hanno generato una grotta a forma di pozzo con la volta collassata. I processi erosivi del moto ondoso insieme ai processi di alterazione chimica, put in the small inner basin connected with the sea forming a small bay, which with the passage of time has been extended until the present structure (Fig. 15).
Other forms of dissolution of carbonates are represented by pyramids and grooves due to stagnation of water along fractures and on the surface of the rock that the chemical alteration. After the removal of stagnant water are brought to light forms of dissolution (Fig. 10).

number of slope deposits cover the costs or NO on the island of San Nicola. A landslide of considerable rotational sliding scale and probably active, is located along the NE (Fig. 16) with the detachment of some blocks highlighted by the opening of fractures and their respect for lowering the ground level, while at the bottom of the scree slope is visible at different grain sizes. A landslide along the coast to overturn NO (Fig. 11) shows a block rotated slightly to the north and the base of the slope you see a thick blanket of debris.

Geological History Tremiti
Initial investigation and first came to attention in the late nineteenth century and the early years of the twentieth century. Tremiti islands were in fact subject of research aimed at identifying the age and nature of the soil.
was a period very active studies, during which the foundations of knowledge Tremiti. From the beginning it was thought seriously to steer them in the broader science of geological relationships between the Italian peninsula to the west and the Balkan Peninsula to the east.

The islands were in fact a large limestone bridge that would have combined the Gargano promontory with Dalmatia and that it would split into two basins of the Adriatic Sea, leaving the southern Adriatic and Ionian-depression in the North Adriatic pit, reaching the depth of 200 meters off the coast of Ancona.
The geological events that led first to the formation of the rocks that make up the archipelago and subsequently to the genesis of that, we are place in a period that lasted about 200 million years. At the beginning of this period, geologists trace the split of Pangea, the supercontinent that is believed would include all land. At the beginning of removal of the plates (or plates) so determinatisi ensuing open expanses of ocean. The space gradually formed between the African and Eurasian plate was occupied by the Tethys Sea, a vast ocean whose depth were formed on the thick carbonate platforms (which includes also the rocks of the Tremiti) due to sedimentation, which lasted for about 120 million years, the carbonate remains of countless marine organisms.
Subsequently, the tectonic movements led to il ravvicinamento della zolla africana e di quella euroasiatica, causando la frattura, l'accavallamento e l'emersione di parte delle piattaforme carbonatiche.
Gli eventi geologici che hanno interessato il Mediterraneo ed in particolare il bacino Adriatico negli ultimi 65 milioni di anni (durante il Cenozoico e il Quaternario), hanno portato alla configurazione attuale dell'arcipelago delle Tremiti.

Durante il Quaternario, le isole Tremiti, già emerse, sono state interessate da processi di erosione e modellamento, principalmente a causa delle variazioni del livello marino dovute alle glaciazioni.
E’ proprio a questo ultimo periodo che si fa risalire la formazione dei sedimenti continentali (löess, crostoni calcarenitici, conglomerates and gravels) that cover the most ancient carbonate rocks of marine origin, consisted primarily of dolomite, limestone and doloareniti.

The testimony of a geological evolution of the Tremiti turns out to be long and difficult. This is testified by the morphology, geologic structures (planes of stratification, tilt and bending of the same, the fault plane) and the presence of fossilized remains of unquestionably related to marine organisms such as shells, corals, skeletal remains of fish.

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Bibliography
AA.VV; Tremiti, geology. Available at Internet: http://tremiti.planetek.it/6g/6g.htm .
AA.VV; Tremiti, geomorphology . Available at Internet: http://tremiti.planetek.it/6g/6g_m.htm .
AA.VV; portal Tremiti . viewed on the internet: http://www.lecinqueisole.it/ .
Brozzetti F., D. D'AMATO, PEACE B. (2006); complex structures Neogene nell'avampaese Adriatic: new structural data from Tremiti. Rend. Geol Soc lt, 2, New Series, pp., 94-97.
CASATI P. (1985); Sciences of the earth. Elements of Geology General . Clued Publishing.
CASTIGLIONI GB (1978); Geomorphology. UTET Edizioni, Torino.
Channell JET, D'Argenio B., HORVATH F. (1979); Adria, the African promontory, in Mesozoic Mediterranean paleogeography . Earth. Rev. Sci, 15.
MONTONE P., R. Funiciello (1971); elements tectonics Tremiti Islands (Puglia). Rend. Lt Geol Soc, 12, pp. 7-12.
PANIZZA M. (1995); Geomorphology. Pitagora Editrice, Bologna.
PANIZZA M. (1988): Applied Geomorphology . Italy Nuova Editrice Scientifica, Rome. SADDLE
R. (1971); Islands Quakes and Pianosa . Notes to the Geological Map of Italy, F. 156 S. Marco in Lamis, pp. 49-65.

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Geological Survey-structural study of the altitude morfostruttura pyramidal Vesallo considerations and morphogenesis (App. reggiano)

Paul
Toys

Summary: Through the collection and processing of the elevation of the micro-card natural the exposure of the slope Charter, the Charter the inclination of the slope and DEM (Digital Elevation Model) has been possible to define the structure and elevation of morfostrutura recognize some forms due to the natural pattern of the slopes. The detection geological and structural correspondence of some outcrops near the pyramid morfostruttura showed how the morphology is controlled by both faults, and folds (stratigraphic structures plicate), as is found by two outcrops, the first placed on the side in north and the other on top of which houses the morfostruttura stratification.

Introduction
morfostruttura The pyramidal Vesallo (Carpiteti, Reggio Emilia) is described by some authors ( ROMANO, 2009a; Corrado, 2009) as a form of man-made due to the remodeling of the slope from Part of populations old and lived in surrounding areas prior to the Etruscans. A previous study, describing them instead as a phenomenon linked to natural processes of erosion and selective chemical alteration along the main tectonic ( TOYS, 2010th ). More Italian pyramid morfostrutture southern Apennines are also described as a phenomenon of anthropogenic origin (ROMANO , 2009b; Barbadoro ), have been the subject of a recent study macroscopic, where they analyzed the morphology and geological structures through the analysis Photo satellite Google map ( TOYS, 2010b). The study proposes a "model denudazionale" straight for recession con variazione dell’inclinazione del versante ( BRANCACCIO e al., 1978; ) come modello genetico delle morfostrutture piramidali, che con tutta probabilità può essere esteso anche ad altri siti.

Tale studio ha come obiettivo quello di valutare il modello morfogenetico precedentemente descritto da BALOCCHI (2010a; 2010b ) e completarlo con i dati di campagna relativi allo studio dell’assetto altimetrico e delle principali strutture tettoniche.
Il rilevamento dell’assetto altimetrico con la realizzazione di carte tematiche ( Carta del microrilievo naturale , Carta dell’esposizione del versante , Carta dell’inclinazione del side, DEM) in order to describe the surface Circulation space topography and the main forms of the landscape.
The geological survey of the main structural-tectonic structures describe the structural setting of the area and any correspondence with the morfostruttura, confirming the hypothesis on the morphology control by tectonic structures.

Geological
The area under study from the geological point of view falls within the syncline Vetto-Carpineti ( Papania et al., 1987, De Nardi and al. 1991) and is characterized lithologically formations belonging to the Succession Epiligure (Bettelli and al. 1987) described below:
Ranzano formation (Fig. 1 and 2) is characterized by turbiditic origin of sedimentary bodies with lenticular to tabular geometry and depositional facies vary widely, from conglomerate to sandstone, arenaceous-pelitic and pelitic ( MARTELLI et al., 1998, and Papania al. 2002).
The lower contact of the training is mostly with the formation of the Marne di Monte Plan and is marked by the emergence of well-Arenac net levels, which are absent in the upper part of the formation underlying the formation of locally Ranzano can also support the underlying Ligurian units deformed. Often the contact with the Monte Piano Marl is discordant with a clear gap erosion ( Papania et al., 2002 ).
The contact with the perforation of the overlying marl Antognola is sharp and angular unconformity with a gap in biostratigraphy ( Fornaciari, 1982; Fregni & SANDWICHES, 1987, De Nardi and al. 1991).
The origin of the training environment of turbidite slope and basin with intercalations of submarine landslides. Age: Upper Eocene. - Lower Oligocene. (Priamboniano sup. - Rupel sup.). Formation of
Ranzano was divided into different States ( HAMMER et al., 1998; Papania et al., 2002 ) among which describes those represented in the study area (Fig. 1 and fig. 2):

• member Varano dé Melegari (RAN3): Contact with the net, sometimes discordant, the Member Val Pessola, is covered in apparent continuity of sedimentation from the overlying formation Antonioli. The lithofacies are those pelitic-arenaceous and arenaceous-pelitic The layers range from thin to thick, sometimes very thick, with a geometry that can be both tabular and lenticular.
• Member of Val Pessola (RAN2): lithofacies varies from arenaceous to pelitic-arenaceous-conglomerate, the layers are ranging from medium to very thick and is generally tabular geometry, while in the coarse-grained layers are present in lenticular form.

Training Plan of Marne di Monte (Fig. 1 and 2) consists of clayey marls and marly clays in thin layers and thin, bearing thin and lenticular whitish feldspathic sandstones of graded and rolled, lithologically similar to those that constitute the formation Loiano. The environment is attributable to the continental slope and deep basin, with sedimentation emipelagica order interspersed with turbidite deposits under distal. Age: Middle Eocene - Eocene sup. (Lutetian - Priamboniano) ( Papania et al., 2002 ).

Loiano Formation (Fig. 1 and 2) consists of siliciclastic sandstone bodies of quartz and feldspar-white, just cemented that are interbedded within the Monte Piano Marl (Bettelli and al., 1987; Papanice et al., 2002 ).

macroscopic analysis ( TOYS, 2010th ) were found two main systems of faults and a subbordinato:

• System NE-SO: with an orientation di circa N50°/60° e denominato in letteratura scientifica come “sistema antiappenninico” perché taglia l’asse della catena appenninica in senso trasversale (fig. 2);
• Sistema NO-SE: con una orientazione di circa N300° e denominato in letteratura scientifica come “sistema appenninico” perché è parallelo all’asse della catena appenninica (longitudinale; fig. 2);
• Un ulteriore sistema di faglie (fig.2) subverticale e con direzione N30° con spiccate evidenze geomorfologiche che alla scala macroscopica rappresentano faglie secondarie subbordinate a quelle appenniniche è stata cartografata lungo il Fosso delle Coste ubicato morfostruttura west of the pyramid ( TOYS, 2010th ).
  

Suspension Height
morfostruttura The pyramid is located on a hill of height 587 m above mean sea level, and has a strong pyramid shape with a square base. Morfostruttura of the four sides of the pyramid, three (hips West, North and the East) are occupied by a dense forest cover, while the south side is used for agricultural crops and probably its morphology can be influenced by human practices. The elevation of
morfostruttura pyramidal structure under consideration is represented in C arta del microrilievo naturale (fig. 3), con equidistanza delle isoipse di 5 m. La carta è stata ricavata elaborando i dati provenienti da due fonti differenti. I primi sono stati ricavati dalla topografia alla scala 1:25000 ( GEOMEDIA, 2009 ), mentre i secondi sono stati acquisiti in campagna attraverso GPS portatile (waypoint in cordinate xyz), utilizzando i parametri geodetici descritti in Tab. 1. I dati ottenuti sono stati elaborati con procedura software mediante calcoli di interpolazione lineare.

Rielaborando la Carta del microrilievo naturale è stato possibile produrre diverse carte tematiche different depending on the characteristics that you wanted to describe.

Charter exposure of the slope (Fig. 4, superimposed on the Charter of the micro- natural ) describes the orientation of the slope through the contours and colors of the same exposure. This feature is the azimuthal angle between true north and the direction perpendicular to the contours of the surface topography represented in the Charter of the micro- natural , measured clockwise. The azimuthal angles are referred to the four main compass points as shown in Table 2 and further divided into classes of 20 ° each color (fig. 4).

Carta dell’inclinazione del versante (fig. 5; sovrapposta alla Carta del microrilievo naturale ): descrive l’inclinazione del versante attraverso delle isolinee e colori di uguale inclinazione. Tale caratteristica del versante viene espressa in gradi da 0° per indicare il versante orizzontale e 90° per indicare quello verticale, ed opportunamente suddiviso in classi di colore di 10° ciascuna (fig. 5). DEM o modello digitale delle altezze (dall’inglese: Digital Elevatin Model): rappresenta la distribuzione spaziale delle altezze del soil (Fig. 6). To better highlight the lay of the land has introduced a light source that simulates the sun's light on Earth's surface, creating an effect of three-dimensional view of the relief ( REICHENBACH et al., 1993; GIUSTI, 2001; CASTALDINI & TOYS, 2006).

Analyzing the elevation data of the natural Charter of the micro-data can be retrieved morfostruttura on the shape of a pyramid. As described by TOYS (2010) morfostruttura the pyramid has a base shaped like a square with sides facing north and west straight e ben definiti (lati certi), mentre il lato a est è in parte definito e tracciabile e in parte mal definito. Il lato a sud è mal definito e non tracciabile a causa delle pratiche agricole che condizionano la morfologia del versante. La quota altimetrica della base della morfostruttura di Vesallo è pressappoco coincidente con la curva di livello dei 555 m, e i lati sono quasi tutti ortogonali tra loro, ad eccezione del vertice posto a SE il quale non conserva l’ortogonalità a causa della presenza di un dosso con direzione NO-SE e ben visibile nella Carta del microrilievo naturale (fig. 3). Inoltre si può notare come al procedere dalla base verso la vetta (quota di 587 m), la morfostruttura non conservi un perimetro a forma square, but since dall'isoipsa of 570 m assumes a triangular shape with one hand extended in NW-SE off coincides with the previously described (Fig. 3).
Two creeks in the watershed areas marked by contour lines, one on the west side and one on the east, show how water runoff concentration were affected by the surface topography across the contour lines. The shape of
morfostruttura is well marked also in the exposure of the Charter side (Fig. 4), which shows the different places in four areas of morfostruttura pyramidal

• Northern Exposure: on the field with color reddish-orange with azimuth angle 30 °.
• position east: on the field with color-orange hue Rorro azimuthal angles 60 ° / 90 °.
• position south: the field with the color green color with azimuth angle 180 ° / 210 °.
• position west: the field with the colors blue colors with 300 ° azimuth angles.

The two areas north and east seem to belong to one sector can be interpreted as the same NE-facing slope (azimuth angle around 30 ° / 60 °) and cut in half by a bump to NE-SW direction. This surely must be off genesis linked to water runoff concentrated at the watershed areas that previously described for selective erosion has affected the side bringing out the bumps in NW-SE (main) and SW-NE (subject to above). The sides of the pyramid
morfostruttura rake varies from point to point from 20 ° to 40 ° tilt (Fig. 4).
The slope located on the west side shows a smooth surface and planar geometry as evidenced by the exposure of the slope Charter (Fig. 4) and a variable slope and distributed in groups according to height as shown the Charter of the inclination of the slope (Fig. 5):

• lower range of tilt 10 ° / 20 °
• midrange angle 30 °;
• high-end angle 10 ° / 20 °.

The regularity of the middle class with azimuth angle of 300 degrees and inclination of 30 ° is classified as a "triangular space" ( TOYS, 2010th ) at a sub-vertical tectonic structure in the direction of N30 ° and remarkable geomorphological features to macroscopic scale ( TOYS, 2010th ) and then back to selective erosion ( Panizzi, 1995; BRANCACCIO et al., 1977, 1978; TOYS, 2010th; 2010b). In the low-end (at the base of the slope) there is an adjustment of the slope at an angle of 20 ° (Fig. 5) due to the deposition of sediments that come from high-end carried by runoff water (affecting the slope across the contour lines as shown by the two watershed areas) or by gravitational processes (falling debris from the side).

Spatial mesostrutturale
It 'campaign was conducted by the writer mesostrutturale detection structures tectonic in three outcrops (Fig. 7). Were measured with the attitude geological compass (direction and inclination) and the stratification of the main faults and fractures in order to describe the structural setting of the area and assess the relationship with the sides of the pyramid morfostruttura Vesallo.

Outcrop 1

This outcrop is found along the north side of the pyramid morfostruttura. Lithologically consists of the formation Ranzano (Member of Val Pessola described by Papania et al., 2002 ) characterized by alternating sandstones and mudstones divided into layers of varying thickness from centimeters to decimetre and report Sandstone / pelite much less than 1.

Structurally, it can be described as a multilayer (lithological alternations with competence and different thickness) ( JOHNSON, 1977, DAVIS & REYNOLDS, 1996; BETTELLA & Vannucci, 2003 ) consists of alternating sandstones with high competence and depth of expertise and mudstones and thinner. These are intensely deformed by two multilayer mesopieghe size metrics are classified as parallel (Class 1B) ( Ramsay & Huber, 1987 ). Of these folds can be describe the geometric structure in the direction and angle of the hinge (N226 ° -8 °) and the direction and angle of the axial plane (N250 ° -18 °), as anticlines lying horizontal (Fig. 8 and 9).

Outcrop 2

This outcrop is located at the top of the pyramid morfostruttura. Lithologically, it is also made by alternating sandstones and mudstones divided into layers of varying thickness (A / P much less than 1) belonging Formation of the Ranzano (Member of Val Pessola).

Even in this case can be described as structurally surfacing multilayer (see description outcrop 1) which has a LOCATION reversed direction and angle of N190 ° -60 ° (Fig. 10).

In both outcrops described above, were also measured respectively with two fault plane and direction of N260 ° -50 ° angle to the outcrop and a N160 ° -50 ° the outcrop 2 (Fig. 11). As far as regards the kinematics, the system in the direction N260 ° Exhibition separation of strata that indicates a relative motion of two blocks of normal fault, and you do not know kinematics of the system N160 °. In stereographic projection shows the two systems is married and likely belong to the same event is also relaxing described in other areas of the Northern Apennines ( TOYS, 2003).

Surfacing 3

This outcrop is located within walking distance of the pyramidal morfostruttura. Lithologically consists of the formation Loiano consists of a small bank of coarse-grained siliciclastic sandstone, very friable and fractured two major systems (kinematic indicators are not visible on the fault plane indicates the relative movement of the blocks): the first oriented with the direction and angle of 190 ° -40 ° N (parallel to the fault system Antiappennino) and the second oriented with direction and inclination of N120 ° -60 ° (parallel to the Apennine fault system, Fig. 12, 13).

mesostrutturali Comparing the data measured in outcrop can be seen as the main structures plicate (horizontal fold anticline - lying down) show the direction of the hinge line and stratification direction almost parallel to the west and east of morfostruttura (Fig. 8). Although this structure plicate should not have had a direct impact on the morphology, most likely the stratigraphic slightly affected the current shape of the hill. The two faults
dell'affioramento 1 and 2 are parallel to the north and south sides of morfostruttura. Even fractures measured nell'affioramento 3 (which saw the parallel with the fault systems could be Antiappennino Apennines and of the faults were found, although not on the surface kinematic indicators) show directions very close to the direction of the sides of the pyramid morfostruttura. In the Formation of Loiano you can see two main systems (as described above, fig. 12, 13) but only one of the two systems can be found in the Formation of Ranzano. In fact, the fracture system in the direction N120 century was also measured in the Formation of Ranzano and parallel to the north and south sides of morfostruttura. As for the system to the direction N190 °, no structures have been found in the same direction in the Formation of Ranzano, probably because the macro-structures with distinct geomorphological described by TOYS (2010th) mesostrutturali no evidence (at the scale dell'affioramento ) or such macrostructures represented by mesoscale fractures are also macroscopic fractures (For the principle of pumpellyite and al. 1894).

Conclusions The finding of a small outcrop on the summit of the hill (Fig. 10) which has a well-preserved stratification and in agreement with the data collected nell'affioramento 1, means that the phenomenon Vesallo pyramidal structure in the Province of Reggio Emilia is of natural origin ( TOYS, 2010th ). The altimeter data show evidence of ongoing processes of runoff likely to be accompanied by gravitational processes that regularize the low end of the slope with varying inclinations around 20 °. Thus, the genesis of morfostruttura pyramid is attributed to erosion and chemical weathering selective along the main tectonic structures ( TOYS, 2010th )

The regularity of the west slope (azimuth angle constant at about 300 ° and tilt 30 degrees throughout its length) is actually the result of the fault scarp retreat due to erosion and chemical weathering. Fault that does not present evidence to the mesoscopic scale geological and structural features but marked morphological characteristics to the macroscopic scale ( TOYS, 2010th ) presenting with sub-vertical structure of the plan and the direction of N30 ° (Fig. 2).
The model that describes the morphogenetic genesi di tale versante è rappresentato dal “modello denudazionale” per recessione rettilinea con variazione dell’inclinazione del versante ( BRANCACCIO e al., 1978; ripreso da BALOCCHI, 2010b ). Il versante è stato modellato da una serie di processi di alterazione chimica ed erosione fisica, in corrispondenza della principale struttura tettonica (con direzione N30°) portando all’arretramento del versante e alla sua riduzione di pendenza (impostandolo ad una inclinazione di 30°; BRANCACCIO e al., 1977; 1978; BALOCCHI, 2010b ). Successivamente alla base del versante è avvenuta una regolarizzazione del profilo con una inclinazione di 20° per l’accumulo di detrito from the upper part of the same side and transported by surface runoff or by gravitational processes (Fig. 14).

The two slopes north and south are the result of weathering processes and erosion along the two conjugate fault systems in the direction N260 ° and N160 ° -50 ° -50 ° (fig . 11) who find themselves in a persistent way in the formation Ranzano ( TOYS, 2010th ). The inclination of the fault plane along the NS direction is parallel to the slope (Fig. 15). Subsequently, the south side has been further shaped by the man through the practices agricole ha ulteriormente variato il profilo del versante.

Il fianco est sembra non essere interessato da faglie che condizionano la morfologia (ad eccezione dei sistemi di frattura nella formazione di Loiano a direzione N190°, che non si presentano all’interno della Formazione di Ranzano e pertanto non vengono considerate). Per questo fianco il modello morfogenetico, è da imputare alle acque di scorrimento superficiale che hano modellato il versante, attraverso la sua erosione della parte alta e sucessivamente alla deposizione nella parte bassa. La giacitura stratigrafica (le pieghe presentano una giacitura pressoché parallele al fianco est della morfostruttura; fig. 8) ha condizionando marginalmente la morfogenesi della collina (fig. 14).

Pertanto sia le strutture tettoniche fragili (faglie e fratture) sia le strutture plicative (pieghe) hanno influenzato il modellamento dei versanti da parte dei processi di erosione e alterazione chimica. Tale modello genetico può essere riportato anche ad altre morfostrutture piramidali essendo che il confronto dei dati macroscopici e mesoscopici fa presumere la sua validità ( BALOCCHI, 2010a; 2010b ).

Bibliografia

• BALOCCHI P. (2003); Analisi mesostrutturale e macrostrutturale delle strutture fragili presenti nelle unità del Gruppo di Bismantova affioranti between Zocca and Castel D'Aiano (Appennino Modena and Bologna). Unpublished Thesis, Dept. of Earth Sc University of Modena and Reggio Emilia.
  
• TOYS P. (2010th), Birth of a pyramidal structure Vesallo. Macrostructural analysis. GeoR.C.It, pub. No 1, available at website: http://georcit.blogspot.com/2010/05/piramide-di-vesallo.html .
  
• TOYS P. (2010b) Genesis of Sant'Agata dei Goti morfostrutture pyramid and surrounding areas. GeoR.C.It, pub. No 3, available at: http://georcit.blogspot.com/2010/05/genesi-delle-morfostrutture-piramidali.html .
  
• Barbadoro G. (Unknown) The pyramids of Benevento (Campania Italy). Available at Internet: http://www.eco-spirituality.org/tdgr-prmdbnv.htm .
  
• BERTELLI V., Cerrina A. FERRONE, PLESE G., G. FONTANESI (1984); Deformation semiduttile Ranzano Sandstones in the middle Val d'Enza (Reggio Emilia Apennines), an attempt to analyze the billing associated with the concentric bending. Bull Soc Geol It., 103, pp. 601-614.
  
• BETTELLA G., BONAZZI U., Fazzini P., F. PANINI (1987); Scheme introductory geology of the Modena Apennines and Epiliguridi limitrofe.Mem areas. Geol Soc It., 39, pp. 215-244.
  
• BETTELLI G., VANNUCCHI P. (2003); Structural style of the offscraped Ligurian oceanic sequences of the Northern Apennines: new hypothesis concerning the development of mélange block-in-matrix fabic. Journal of Structural Geology, 25, pp. 371-388.
  
• BRANCACCIO L., CINQUE A., SGROSSO I. (1977); Forma e genesi di alcuni versanti di faglia in rocce carbonatiche: il riscontro naturale di un modello teorico. Rend. Acc. Sc. F.M.S.N.S.L.A. Napoli, ser. 4, 46.
  
• BRANCACCIO L., CINQUE A., SGROSSO I (1978); L’analisi morfologica dei versanti come strumento per la ricostruzione degli eventi neotettonici. Mem Soc Geol lt, 19, pp. 621-626.
  
• CASTALDINI D., P. TOYS (2006), geomorphological study of the territory of the plains south of Modena. In: A. Lodovisi "Reclaiming the High Plains in the territories." Land Reclamation Consortium Burana-Leo-Scoltenna-Panaro Modena.
  
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• DAVIS GH, Reynolds SJ (1996), Structural geology of rocks and regions. JOHN WILEY & SONS.
  
• FORNACIARI M. (1982); lithostratigraphic observations on the southeast margin of the syncline Vetto - Carpiteti (RE). Rend. Geol Soc lt, 5, pp. 117-118.
  
• Fregni P. PANINI F. (1987); Lacuna between stratigraphic formations and Ranzano Antognola areas and Roteglia Montebaranzone (Appennino Modena and Reggio Emilia). Riv. Lt Paleont. Start., 93, pp. 261-280.
  
• GEOmedia (2009); Hiking Map No 2: The Appennino Reggiano to the scale 1:25000. Graphic Arts Castle - Viadana (MN)
  
• GIUSTI C. (2001), The Digital Terrain Model (DTM) to support the mapping geomorphology: the example of the plain of Modena (Po Valley, Northern Italy). Proceedings of the National Conference on "Culture and cultural map of the territory", Sassari, 12-13 December 2000. Bull Ass It. Cartography, 111, 112, 113, pp. 409-417.
  
• JHONSON AM (1977), Styles of folding: mechanics and Mechanisms of folding of natural alastic material. Elsevier Scientific Publishing Company, Amsterdam, p. 406.
  
• DE NARDO MT, Iaccarino S., MARTELLI L., G. Papania, TELLINI C., TORELLI L., Verne L. (1991), Observations on the evolution of the basin-satellite epiligure Vetto Carpineti-Canossa (Northern Apennines). Mem Descr. Charter of Geol It., XLVI, pp. 209-220, Rome.
  
• MARTELLI L., G. CIBIN, Giulio A., Catanzaro R. (1998); lithostratigraphy of the formation Ranzano (Priamboniano-Rupel, Northern Apennines and the Tertiary Piedmont Basin). Bull Soc Geol It., 117 pp. 151-185.
  
• PANIZZA M. (1995), Geomorphology. Pitagora Editrice, Bologna.
  


• Papanice G., TELLINI C., TORELLI L., Iaccarino S. (1987), New data on stratigraphic and structural formation in Bismantova "syncline" Vetto-Carpineti (Appennino Reggiano - Parmesan). Mem Soc Geol lt, 39, pp. 245-275.
  
• Papanice G., DE NARDO MT, BETTELLA G., D. RIO, TELLINI C., Verne L. (2002), Geological Map of Italy at the scale 1:50000, F ° 218 - Neither Castelnuovo Monti. S.EL.CA Florence.
  
• Papanice G., DE NARDO MT, BETTELLA G., D. RIO, TELLINI C., Verne L. (2002), Notes to the Geological Map of Italy at the scale 1:50000, F ° 218 - Neither Castelnuovo Monti. S.EL.CA Florence.
  
• pumpellyite, R., WOLFF, JE, AND DALE, TN, (1894), Geology of the Green Mountains in Massachusetts. U.S. Geological Survey, Monographs, v. 23, 206 p.
  
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• ROMANO LB (2009a) discovered a further ... Vesallo borer in Italy in Reggio Emilia. Available at Internet: http://piramidiinitalia.myblog.it/archive/2009/06/19/scoperta-una-ulteriore-piramide-in-italia-vesallo-reggio-emi.html .
  
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Visual Pokemon Ruby Cheats

stratigraphic succession of paleogeographic Corniano and assumptions (Trentino). Genesis of

di Paolo Balocchi

Introduzione
Scopo dello studio è quello di misurare una successione stratigrafica analizzando le diverse facies presenti e descriverne le caratteristiche macroscopiche e microscopiche.
Si vogliono ricavare le caratteristiche stratigrafiche, sedimentologiche e paleontologiche della serie, per definire un modello paleogeografico inerente alle aree dove affiorane le medesime facies.
La successione è costituita da tre principali formazioni: Scaglia Variegata (membro superiore della Formazione del Biancone); Scaglia Rossa; Calcare di Torbole. La formazione al tetto della successione è ben differenziabile in affioramento grazie alla presenza di un hard – ground che mette a contatto la Scaglia Rossa e il Calcare di Torbole, mentre più difficile è stato definire il limite tra Scaglia Variegata e Scaglia Rossa, causa le loro similitudini litologiche e sedimentologiche. Lo studio delle sezioni sottili ha consentito di ricavare il contenuto paleontologico e di definire il limite biostratigrafico tra le due formazioni.

Inquadramento geografico
La successione è affiorante a nord del paese di Corniano lungo the trail across the road passing through the country and continues to the outside.
The country is geographically situated in the region of Trentino - Alto Adige, between Mori (south of Rovereto) and Torbole. To reach the estate is able to traverse the road that leads to Loppio Mori and Torbole, where you go in Agriculture Directorate Manzano; Nomesino and finally Corniano (Fig. 1).

Geological
The general stratigraphic framework of the Adige Valley consists of several formations characteristics of different depositional environments. The area is part of the Alpine chain, formed from the Late Cretaceous as a result of the collision between the African plate and Eurasian plate, causing the closure of the Tethys Sea. These tectonic movements, also associated with subsidence and rising relative sea-level in ancient times (pre-collisional), have led to different conformations Paleogeographic.

As for the series of coin, is represented by a stratigraphic succession outcropping and prominently includes the following formations (Fig. 2; Castellarin, 1971):

• Scaglia Variegata: The base is composed of calcilutiti layered ivory white or gray (rarely pink) with the presence of bioturbation and intercalated with marly gray levels - blackish (BOSELLINI Et al., 1978) with thicknesses ranging from a few cm to 20-30cm. Are visible nodules or beds of flint with red or gray. There are radiolaria and foraminifera (BOSELLINI et al., 1978) and at the base by tintinnidi (Castellarin, 1971). In the geological map of the latter, the Scaglia Variegata is a member of the higher education of Biancone. Age: Neocomiano - Albian.
• Scaglia Rossa : more or less marly micritic limestones (BOSELLINI et al., 1978) or laminated limestones (Castellarin, 1971) red or white. Are visible layers or nodules of flint and marl intrastrati. Planktonic foraminifera ( Rotallipore, Globiotruncane ) are abundant. The limonite this paste in the fund is responsible for the reddish color (BOSELLINI et al., 1978). The roof is a hard - ground with a temporal hiatus variable from location to location (Eocene - Paleocene). Age: Albian - Maastrichtian.
• Limestone Torbole : it consists of massive stone blocks and poorly stratified calcarenitic with a high content of fossil type macroforaminiferi, coralline algae neritic environment (Luciana, 1989). Age: Lutetian.

facies analysis of the sequence of Corniano

Corniano series (see end of article) shows, the macroscopic scale, as a concordant succession from the base to the roof, and a discontinuity of type paraconformity (BOSELLINI et al., 1997) is marked in outcrop by a hard-ground structure, is the study of thin sections showing a discontinuity paleontological .
The methods used during the in situ detection, are classic geology of the country. During the measurement sequence with dipstick, have addressed issues primarily due to intense tectonic deformation in the area, which has produced a succession of tiltaggio west, and in the central part of the series is a sporadic tree cover in patches that in some cases prevented detection. It has adopted a system of discontinuous sampling, collecting those samples of the different facies to perform microscopic investigations are more detailed than the simple macroscopic description. For the microscopic study of carbonate rocks have been referred to the classification of DUNHAM (1962).

The study carried out in the country macroscopic and microscopic study, have the following distinct facies within the lithological formations outcropping:

1. Scaglia Variegata Formation

This training has a measured thickness of 4.2 m of age Turroni - Santonian. The contact to the roof is not visible, but microscopic investigations it was possible to put a limit whereas the loss from the radiolaria which determine the transition to the overlying formation.

Facies of Limestone - Limestone marl a Radiolaria
marly to fine texture (wakestone) from gray to red, the color that lightens the base to the roof. The tabular facies is divided into layers, the thickness varies from 10 cm to 15 cm, sometimes due to the deposition of laminated shells of planktonic foraminifera in thin layers. Are contained within tabular layers and layers of black flint nodules or red, and rare type structures mineralized manganese dendrites. Interlayers levels thin (from millimeters to centimeters) of Marne for gray (Fig. 3).

microfossils: radiolaria, planktonic foraminifera (type Dicarinella Turonian - Santonian, Whiterinella Turonian - Santonian) which appear to be silicified. Washed from the interlayers was found a fossil content consists of poorly preserved and silicified foraminifera planton classification unclear.

2. Formation of the Scaglia Rossa
The Scaglia Rossa has a thickness of 59.0 m and a stratigraphic distribution from the Turonian to Maastrichtian. This formation is characterized by non-cyclic alternations of three main facies described below. The transition to the roof with overhanging formation appears to be clearly visible through a clear and hard - ground (hardened crust more compact) of Maastrichtian age. The microscopic analysis shows an increase in fossil content to the roof and a sudden change of faunal associations between the Scaglia Rossa Formation of Limestone Torbole. The facies are:

facies of limestones -
marly marly limestones (Fig. 4) layers divided into tabular mostly regular, the thickness varies from 5 cm to 15 cm. They have variable color from white to red, to red and pale gray, depending on stratigraphic position. The roof of the training in the last meters There is a hardened crust coarser texture where the stratification is lost (hard - ground).

E 'possible to further differentiate them according to texture:

• facies of limestones - marly fine texture : mudstone to fine texture at the base of the formation, with nodules and layers of red chert horizons tabular .
• facies of limestone - marl woven medium - fine : wakestone woven medium - fine and sometimes coarse, placed in the roof of the training, with poor or nearly absent levels of flint nodules.

These two divisions are quite recognizable even in the country, being one of them separated by a thickness of 18.2 m of nodular limestone facies. The contact to the roof and the base of this facies is always unclear and poorly identifiable, through a gradual transition.

microfossils: a second you can find the stratigraphic position of planktonic foraminifera (type Marginotruncana Turonian - Santonian in the basal part; Globotruncane Campanian - Maastrichtian at the summit).

nodular limestone facies of nodular limestones
coarse texture (packstone - wackestone), divided in piccoli straterelli composti da matrice fangosa fine di colore rosso – grigio e talune volte assume delle sfumature di colore bianco. Nelle facies alla base della formazione assumono colorazioni più rossastre, mentre al tetto si hanno colorazioni più biancastre.

Microfossili: foraminiferi planctonici tipo Marginotruncana Turoniano – Santoniano).

3. Formazione del Calcare di Torbole
Tale formazione si presenta con uno spessore di 5.20 m di età Eocenica e caratterizzata da una sola facies:

Facies dei Calcari Massicci
Calcari (pakstone) grigi talvolta anche giallastri mal stratificati con tessitura medio – fine. Risulta essere compatto e resistente.

Microfossili: Macroforaminiferi (tipo Nummulites Eocene, Discocicline Eocene), piccoli foraminiferi planctonici, rodoliti, alghe.

Analisi Stratigrafica deposizionale della serie di Corniano
Nelle facies appena descritte non si è rilevata alcuna ciclicità nel processo di sedimentazione; le caratteristiche più salienti sono la tessitura e la colorazione che variano procedendo dalla base al tetto. Anche il contenuto paleontologico risulta differente, con morfologie più antiche alla base della serie e più recenti verso il tetto, questo a indicare un’assenza di disturbi tettonici fragili (Faults or diaclasi) to displace the stratigraphic sequence.
stratigraphically the series appears to be consistent from base to roof, with visible layering formed by banks of more competent material ( facies of limestones - marl, marly limestone of Facies in radiolarians, the nodular limestone facies ).
analysis of facies and microfacies have been able to set limits and determine the various formational environments, in order to obtain the evolution - stratigraphic depositional series Corniano. The presence of
Dicarinella , Whiterinella Marginotruncana and put the first number in the range of 32.0 m Turonian - Santonian. In this interval are present, in continuity of sedimentation, the two formations of the Scaglia Variegata and the Scaglia Rossa above. To determine the boundary between the two formations is considered the disappearance of the forms in place radiolarians to 4.2 m (Fig. 6). In the first few meters of the Scaglia Variegata, there is a deposition of a marly limestone of Facies radiolarian characteristics of a closed environment of the deep sea, little oxygen (BOSELLINI et al., 1978). Just the appearance of
Marginotruncana for the start of sedimentation of the Scaglia Rossa (fig.10) with marly limestone facies of fine texture and nodular limestones . In this case there is a deposition of facies, sometimes with a pinkish red hue, due to the presence of limonite (2Fe 2 O 3 • 3H 2 O), a mineral of iron oxide hydrate which indicates a oxygen-rich environment. The texture varies from one end of the marly limestone facies that grossly nodular limestones, may indicate different environments. While the first facies is a not confined to the open sea, deep and rich in oxygen, the second seems facies deposited in a similar environment but with a hydrodynamic higher than the previous.

Above the Campanian - Maastrichtian, determined by the appearance of the genus
Globotruncana (34.0 m; fig.7), we have the marly limestone facies of a medium texture - fine. Again the red color and the texture variable reveal a non-secure environment of shallow sea oxygenated. The variability of textural changes from medium - an end to 34.00 m remains nearly unchanged up to 54.00 m, where he began a coarser sediment. Up to shade the roof in a very compact hard crust which is lost in the last meters layering and texture is more coarse, very similar to the nodular limestones of Facies . This hard - ground (fig.7, fig.8) is in Upper Maastrichtian (disappearance of Heterohelidae ) and represents an erosional surface that shows a hiatus around the Paleocene. The similarity of facies between hard - and ground nodular limestones may indicate the same origin and same environment. In fact, several authors (FUGANTI, 1964; Castellarin, 1971, 1972; BOSELLINI & Luciana, 1985) have suggested tectonic rhythmic pulse that led to the emergence of the area with the deposition of the Scaglia Rossa conglomeratic levels, demonstrating that these events are gaps produced by stripping and underwater portions conglomerate deposits are the result of gravitation.

Eocene (appearance of Nummulites and Discocicline ) is a marine carbonate platform sedimentation (shallow sea) facies represented by a massive Limestone (Limestone Formation of Torbole). These new conditions are due to tectonic processes of collision between the Eurasian and African plate that led to the lifting of the Trento Plateau (with deposition of deep sea), and the formation of a new configuration represented by paleogeographic Lessini - Shelf (BOSELLINI, 1989 ).

paleogeographic model air coin
The area surrounding the succession of Corniano where I found the same lithological formations, from the Cretaceous can be considered an environment of deep sea open place below the minimum oxygen (from-700m to -100/-1500m now, but in the Cretaceous was extended to -2000 /-3000m depth) where it was the deposition of the Scaglia Variegata, under anoxic conditions and protected environment, confinement, still below the low oxygen, were deposited in the Black - Shale. Above the minimum oxygen was an increasingly deep and oxygenated but this time not limited where you filed the Scaglia Rossa (Fig. 9).
According to the model proposed the Black - Shale and the Scaglia Deporsi were varied in sheltered conditions, with limited amounts of oxygen. These conditions could be possible if there were ups and downs of the structural support the diversity statement. If we consider now the active tectonics in that particular moment in geological history (BOSELLINI et al. 1978; Cassinis & Castellarin, 1988; DOGLIONE & BOSELLINI, 1987), it is possible to envisage a more complete model than the previous.

The tectonic conditions of the late Cretaceous (Dogger - Malm) provided a paleogeographic conformation formed by a platform of Trent (AUBOUIN 1964; Castellarin, 1972) Drowning (for soothing) and becomes a sblocchettato plateau (Fig. 10; BOSELLINI & Winterer, 1981; DOGLIONE & BOSELINI, 1978). Under these conditions, structural and topographic high formed by topographic low, you can define the different environments that we have obtained previously (Fig. 11):

1. Euxinico Environment: the deposition of the Black - Shale in protected conditions deep sea in the absence of oxygen and placed in low-current deep structural
2. Environment deep in the zone of minimum oxygen : the deposition of the Scaglia Variegata conditions in the deep sea (below-700m depth )
3. Environment deep zone above the minimum oxygen : the deposition of the Scaglia Rossa in open sea conditions.

the Scaglia Rossa are several intervals variable in texture, with coarse facies as Facies of nodular limestone, deposited on structural highs in the open sea and under conditions of ocean currents due to denudation ( BOSELLINI & Luciana, 1985) are formed of hard - ground.

A different pattern is Eocene (Fig. 12), where the deposition of facies belonging to the Limestone indicates a Torbole platform environment. This may be related to the lifting of the Trento Plateau due to the compression between the African and Eurasian plates. We are forming new environmental conditions, shallow carbonate platform and strong hydrodynamics Lessini - Shelf (BOSELLINI, 1989, 2004), with the deposition of Tertiary limestones.

conclusions from the study - stratigraphic sedimentological detail the sequence of coin was possible

• microscopic analysis has defined the beginning of sedimentation of the Scaglia Rossa (appearance of Marginotruncana) placing the stratigraphic boundary between the Scaglia Variegata e la sovrastante Scaglia Rossa;
• determinare le differenti facies e descrivere l’evoluzione stratigrafico – deposizionale delle Formazioni affioranti;
• definire un modello paleogeografico dell’area di Coniano e delle zone limitrofe dove sono presenti le medesime formazioni.

Dal modello paleogeografico ipotizzato nel presente studio, è possibile determinare alla scala regionale il medesimo assetto paleogeografico, con la deposizione delle differenti facies in corrispondenza di zone differenti. Tale modello è influenzato notevolmente dalle strutture tettoniche presenti nell’area di studio. La linea Giudicariense con la sua struttura a fiore eoalpino (E Bosellini AL. 1978; Bosellini & Doglioni, 1987) determines a di alti e bassi Assetto struttura determinando ambienti deposizionali different.

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