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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

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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.

Bibliografia

• AUBOUIN J. (1964), An Essay on the post-Triassic paleogeography and evolution of secondaries and Tertiary eastern Southern Alps (Southern Alps, Lombardy and Veneto, Slovenia Western Jougoslavie, ecc). Bull Soc. Geol. F, s. 7 v.5 pp.730-766, 1tav. (Shift) 2fig., Paris.
• Bosellini A. (1989) Dynamics of Tethyan carbonate platform. In: CREVELLO PD, JAMES LW, JF SARG, JF READ (eds.), Controls on Carbonate Platform and Basin Evolution. Soc Econ. Paleont. Miner., Spec Publ. 44: 3-13.
• BOSELLINI A. (2004); The western passive margin of Adria and Its carbonate platforms. Lt Geol Soc, 32 (Special Volume).
• BOSELLINI A., BROGLIO LC, BUSETTO C. (1978); Cretaceous Basins of Trentino. Riv. Eng. Paleont. V. 84, No 4, pp. 887 to 946.
• BOSELLINI A., Mutti E., Ricci Lucchi F. (1997), and sedimentary rocks. UTET ed.
• BOSELLINI A., Luciani V. (1985), Contribution to the knowledge of Nago dell'hardground Rend. Italian Geological Society, 8: 61-64.
• Cassinis G., A. Castellarin (1988): Meaning of lines and Gallinera Giudicarie southern Adamello Geology and surrounding areas. Acts Ticinensi of Earth Sciences, 31, 446-62.
• Castellarin A. (1971), Geological Map of the area between the Adige and the south of the Sarca Bondeno (Trentino). Litogr. Art Cart, Florence.
• Castellarin A. (1972); paleotettonica synsedimentary evolution of the boundary between the "Platform of Venice" and "Bacino Lombardo" north of Riva del Garda. Giorn. Geol, v. 38, No 1, pp. 11-212, 20 pl., 18 fig., Bologna.
• DOGLIONE C.; BOSELLINI A. (1987); Eoalpine Mesoalpine and tectonics in the Southern Alps. Geologische Rundschau, 76 / 3, 735-754.
• DUNHAM RJ (1962), Classification of carbonate rocks According To depositional texture. In: WE HAM (eds.), Classification of carbonate rock. A Symposium. American Association of Petroleum Geologists Memoir 1, p. 108-121.
• FUGANTI A. (1964), The "tectonic pulse" of western Trentino (Eastern Alps). St. Tr. Sc Nat., V.61, No 2, pp. 138-158, 23 fig., Trento.
• Luciani V. (1989); sequence stratigraphy of the Monte Baldo in Trentino (Province di Verona e Trento). Memorie di Scienze Geologiche vol. XLI, pp. 263 – 351.
• WINTERER BOSELLINI (1981); Subsidence and sedimentation on a Jurassic Passive Continental Margin, Southern Alps, Italy. AAPG Bull., 65(3): 394-421.

High Oxalates In Toddler

morfostrutture pyramid of Sant'Agata de 'Goti and surrounding areas. Geological Map of the Apennines between

GENESI DELLE MORFOSTRUTTURE PIRAMIDALI
DI SANT’AGATA DE’ GOTI E ZONE LIMITROFE
-analisi macrostrutturale-

di Paolo Balocchi*

Introduzione
In questo breve studio si vogliono descrivere le considerazioni personali rispetto the description of some pyramids in southern Italy by the independent researcher Romano (2009) and Barbadoro.

This article is preferable to replace the term "pyramid" (Toys, 2010) the term "morfostruttura pyramid" because it expresses more of the genetic processes that led to their formation. In fact, it is believed that these morfostrutture pyramids are the result of tectonic processes and then the processes shaping the surface (chemical alteration and physical disintegration, together with those of the runoff) which produced the forms and the present landscape (Toys, 2010).

The study includes the following phases:
· Research bibliography of the major tectonic structures of the area of \u200b\u200bSant'Agata de 'Goti Benevento (Campania) and surrounding areas;
· Study of satellite photos taken from Google Maps to map the tectonic structures at the regional scale;
· Analysis of satellite imagery in 3D from Google Maps to map the "morfostrutture pyramid" and recognize the topography of the area with particular attention to morphotectonic (Brancaccio, 1977, 1978, Panizza, 1995).
This study aims to describe the processes of formation of "morfostrutture pyramid" in the territory of Sant'Agata de 'Goti and zone limitrofe, definendo una probabile ipotesi genetica plausibile con i dati geologici e geomorfologici ricavati dallo studio delle immagini satellitari di Google Maps.

Inquadramento geografico
Secondo quanto esposto dagli autori Romano, (2009) e Barbadoro la piramide presente a Sant’Agate de’ Goti si trova in corrispondenza della “collina Ariella” di altezza 348 m (a nord-ovest del M.te Traverso). Inoltre altre due piramidali si ritrovano a sud-est nei pressi del paese di Moiano (M.te Porrito, 380 m) e ancora più a sud-est nei pressi di Montesarchio. Una nuova piramide è stata rinvenuta nei pressi di Caiazzo (M.te Mesarinolo, 245 m), localizzata a nord-ovest rispetto il paese di Sant'Anna de 'Goti.Le pyramids described above are aligned along a direction (Romano, 2009) is clearly visible from satellite images (Google Maps), which show an actual alignment in a direction of 115 ° N (Fig. 1).

THE EXAMPLE OF Sant'Agata de 'Goti
Geological
The ares of study (Fig. 2) is characterized by north-west lithologies belonging to the Samnite units represented by sandstone , limestone and marl of Campoli, while in the south and west are lithologies belonging to the carbonate tectonic units of the Apennines, represented by Limestones Radiolaritidi (calciruditica in facies), and rudist Calciruditi orbitoline, Calacri with Requin and gastropods. There are also volcanic deposits belonging to Ignibrite Campana (Carannante C., Stanzione D.).

analysis of tectonic structures
In the paper the main tectonic features (Fig. 3) describes the major faults of a regional nature. A first fault system with sub-vertical plane and straight line shows a NE-SW (N 40/55 °) and a second system with NW-SE (N 120/130 degrees).
Through photo interpretation of satellite images of Google Maps with the 3D perspective view (Fig. 4) it was possible to detect the presence of other minor (Gelmini & Fazzini, 1982; Panizza, 1995; Toys, 2003) that preserve an approach similar to those mapped at the regional scale.

Analysis of Geomorphological
As for geomorphological aspects, the area under consideration shows a variety of forms related to different modeling agents. The forms include broad fluvial terraces probably of volcanic origin for the deposition of the Campanian Ignimbrite and then shaped and carved by surface water also forming along the edges of river embankments F. Isclero. The study correlated
satellite images and topographic maps (Ministry for the Environment, Land and Sea) has mapped the course of the ridges. From the 3D model and paper forms (Fig. 4 and 5) we see that the trend of the ridge follows the main tectonic features.

The pyramid described by Romano (2009) (coordinates: N 41 ° 5 '51.10 "E 14 ° 31' 23:20" of GRW.) Is located at the top post to NO of Mt Traverso and called "hill Ariella" (348 m). It has a pyramid type structure with geometric rhombic regular basis. The slope of the hill inclinato con una pendenza regolare di circa 25/30°. Sono presenti forme antropiche come i terrazzamenti a scopo agricolo visibili sul versante nord e nello spigolo a nord una concava di escavazione per cava (Romano, 2009; Barbadoro).
Dall’analisi fotogeologica non si riscontrano superfici strutturali ben conservate quali faccette triangolari se non quella posta sul lato nord della morfostruttura piramidale (Brancaccio e al., 1977; 1978; Panizza, 1995; Panizza & Piacente, 1978; Ufimtsev, 1990; Balocchi, 2010;). Le poche “superfici relitte” (Panizza & Del Vecchio, 1982; Panizza, 1995; Brancaccio e al., 1978) presenti nell’area di studio si presentano con forma planare e regular, aligned with the main tectonic structures.

OTHER MORFOSTRUTTURE PYRAMIDAL
We describe below the structural-geological and geomorphological features of the remaining morfostrutture pyramid found in areas adjacent to that of Sant'Agata de 'Goti. These minor mostrostrutture have a poor state of repair due to an intense process of modeling by chemical and physical alteration.

Moiano ( N 41 ° 5 '27.70 "E 14 ° 32' 49.87" to GRW).
Geologically the area is characterized by limestones and limestones with gastropods and Requin to Radiolaritidi (in calciruditica facies). In south east are composed of volcanic deposits Ignibrite Campana (Fig. 6).
On the geological map is mapped with an alleged fault NW-SE.

analysis of satellite images, geo-morphological area has a number of debris cones in the portion to the north, while along the F. Isclero are many edges of the escarpment by erosion of volcanic deposits. The pyramid
morfostruttura (Monte Porro, 380 m) shows a cone-shaped ill-defined and not very evident (Fig. 7).

Montesarchio ( N 41 ° 2 '42.19 "E14 ° 40' 24.39" of GRW)
Geologically the area is characterized by deposits colluvial (Chiocchini & Hammer, in press).

morfostruttura The pyramid (279 m) shows a form ill-defined, probably due to leaching of surface deposits by the agents of weather and water runoff (Fig. 8), resulting in a smooth and corrugated morphology almost the surrounding area.

Caiazzo ( N 41 ° 9 '25.29 "E 14 ° 20' 43.05 of GRW)
Geologically the area is characterized by sandstones of Caiazzo and on the east side of Calciruditi rudist and orbitoline with a contact with the previous tectonic formation above (Fig. 9).

analysis satellite images, geo-morphological area has different types of fluvial origin as the edges of the escarpment along F. Volturno. The pyramid
morfostruttura (Mt Mesarinolo, 245 m) shows a regular conical shape, and on the north side of a valley excavating probably a form of anthropogenic (Fig. 10) due to the excavation pit.

CONCLUSION
The phenomenon of morfostruttura pyramidal Sant'Agata de 'Goti in the Province of Benevento (Campania) and surrounding areas is a natural phenomenon linked to the processes of erosion and chemical alteration along the selective major tectonic lines.

The data obtained from geological maps and photo interpretation show that the pyramidal structure with a rhombic base of the ridge and trends inherent in the small mountain range consisting of the peaks of Monte Guardia (439 m), Mt Traverso (365 m) and the "hill Ariella" (348 m), are set along the main tectonic and local to regional scale. On carbonate lithologies of the second type Brancaccio and alt. (1977, 1978), fault surfaces are set with an inclination close to the average of 30/40 ° tilt morfostruttura described by Romano (2009) and Barbadoro.
There were no significant surface triangular or trapezoidal because of the morphogenetic processes that have dismantled the original fault scarp slope and varying the generation of "relict surfaces" (Panizza & Del Vecchio, 1982; Panizza, 1995) planar angles of 25/30 degrees.
Some of the faults at the sides tend to preserve the flatness of the original with remarkable fidelity mirror fault. In our case the slopes of the mountains are studied on the main tectonic features, but do not preserve the original tilt mirror fault (subvertical). A series of erosion has shaped mirror fault until the reduction of the slope (the slope current setting of 25/30 ° inclination, and Brancaccio al. 1977, 1978; Toys, 2010) and leaving the base of the slope accumulation of debris (Fig. 11).

Although data on other pyramidal morfostrutture are few and far inconclusive, it is believed that the "denudation model (for straight-line recession with variation of the slope) describes the genetic hypothesis is consistent with the geological data, Structural and geomorphological derived from this study.

It is also considered useful, further study with a monitoring campaign mesostrutturale and geomorphology, in order to verify the consistency of the genetic model described above.

BIBLIOGRAPHY

• Toys
  P. (2003); mesostrutturale and macrostructural analysis of the structures present in the fragile unity of the group of emerging Bismantova Zocca eCastel D'Aiano (Appennino Modena and Bologna). Unpublished Thesis, Dept. of Earth Sc University of Modena and Reggio Emilia.
• Toys
  P. (2010), Birth of a pyramidal structure Vesallo - macrostructural analysis. GeoR.C.it, pub. No 1. Available at Internet: http://georcit.blogspot.com/2010/05/piramide-di-vesallo.html
• Barbadoro G. (Unknown) The pyramids of Benevento (Campania Italy). Available at Internet: http://www.eco-spirituality.org/tdgr-prmdbnv.htm .
• Bosi C. (1975); Osservazioni preliminari su faglie probabilmente attive nell’Appennino centrale. Bol. Soc. Geol. It., 94, pp. 827-859.
• 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. It., 19, pp. 621-626.
• Carannante C., Stanzione D. (In press), F ° 431 "Caserta East" at the scale 1:50.000. Available at Internet: http://www.apat.gov.it/Media/carg/Rilevamenti_Def/431_CasertaEst/431.htm .
• Cocchini U., Martelli G., (in press), F ° 432 "Benevento" a scale of 1:50,000. Available at Internet: http://www.apat.gov.it/Media/carg/Allestimento/432_/432.htm .
• Fazzini P, Gelmini R. (1982), Tectonics of the Northern Cross. Mem Soc Geol lt, 24, pp. 299-309.
• Ministry for the Environment Land and Sea (unknown), National Cartographic Portal. IGMI mapping scale of 1:25.000. Available at Internet: http://www.pcn.minambiente.it/ .
• Ministry of the Environment, Land and Sea (unknown), National Cartographic Portal. Cartography of grazing pressure. Available at Internet: http://www.pcn.minambiente.it/ .
• Panizza M. (1995), Geomorphology. Pitagora Editrice Bologna.
• Panizza M., Del Vecchio R. (1982); The "relict surfaces" Appennino Modena. CNR, PF Geodynamics, pubbl. 506.
• Panizza M., Piacente S. (1978); Rapporti fra Geomorfologia e Neotettonica. Messa a punto concettuale. Geogr. Fis. Din. Quat., 1(2).
• Romano L. B. (2009); Scoperta una ulteriore piramide in Italia… Vesallo a Reggio Emilia. Consultabile all’indirizzo internet: http://piramidiinitalia.myblog.it/archive/2009/06/19/scoperta-una-ulteriore-piramide-in-italia-vesallo-reggio-emi.html ;
• Romano L. B. (2009); Santa Anna de’ Goti una seconda Visoko? Consultabile all’indirizzo internet: http://it.calameo.com/read/000068410d4a7a3498164 ;
• Ufimtsev GF (1990); Morphotectonics of the Baikal rift zone (USSR). Geogr. Fis. Dyn. Quat., 13.

Whipper Snipper Propeller Heads

Vogherese Sagliano and Torrent stafora.

Geological APENNINE Vogherese
BETWEEN THE TORRENT GmbH is Staffora
VARZI (PAVIA)
- geological survey of campaign - Toys

Paul Mazzoli Monica * * * Andrea Pivetti Gunel Rosenvik

* Graduates in Geology at the University of Modena and Reggio Emilia sweat


INTRODUCTION The purpose of the campaign survey, conducted between 4 and 8 June 2001, draws to deepen the study of this territorio approdando quindi a una piu’ dettagliata caratterizzazione geologica dell’area, rispetto a quanto non fosse gia’ noto in letteratura.
Abbiamo posto particolare attenzione all’interpretazione dell’intricato gioco di faglie che interessa la fascia a nord di Sagliano e alla ricerca di formazioni non individuate da precedenti lavori.

INQUADRAMENTO GEOLOGICO E GEOMORFOLOGICO
La cartina sottostante (fig. 1) illustra l’ubicazione dell’area studiata nei pressi di Varzi (PV).

Una notevole rottura di pendio identificata in gran parte da una scarpata di faglia, suddivide il territorio in due zone con caratteristiche completamente different. The area north of
Sagliano, characterized by competent lithologies, has a morphology remarkably steep and rugged, fully wooded .. The area south of the country, mainly clay with outcrops of lithologies very competent, has a sweet relief is often affected by active or dormant landslides. Vineyards and orchards, wheat fields or planted with grass are many in this' area suitable for agriculture. The valley floor and 'alluvial deposits affected by changing the competence of the river and terraced Staffora.

STRATIGRAPHY AND TECTONICS
formations that we found correspond to emerge Sandstones M. Vallassa, Marne di M. Lumello, Brecce Argillose 2 e Marne di M. Piano, facenti parte della successione Epiligure; le Argille di Viano delle Liguridi. (per colonna stratigrafica ed eta’ vedi la legenda fig. 4).

Le Argille di Viano affiorano a nord-est di Ponte Crenna lungo una fascia con direzione est-ovest definita da due limiti tettonici che le mettono a contatto con le Brecce Argillose 2 sia a sud sia a nord. Tale striscia, come d’altronde tutta la zona circostante,e’ fortemente tettonizzata ,per cui non abbiamo riscontrato assetti della stratificazione con andamenti omogenei tra i vari affioramenti. La formazione , di natura torbiditica, si presenta prevalentemente costituita da argille scure. A volte sono presenti marne con layering a thin, gray and pink alternating with carbonate banks. The latter have a thickness of the order of decimeters and a fine grained sandstone, are very competent and have dark patina of alteration, and sometimes' see a thin layer. The soil in this area differs from the surrounding area showing, sometimes with good evidence, more 'dark. The

Brecce 2 clay surface in all the remaining, lower part of the paper. They tend to creeks that outcrops are numerous. The training consists of a dark clayey matrix that incorporates clasts of different shapes and different genesis, angular, varying in color, mainly in carbonate-rich veins di calcite. A sud, le Brecce Argillose 2 sono ricoperti dai depositi del torrente Staffora mentre a nord vengono ricoperte quasi interamente da detriti di versante. In un punto toccano le Marne di M. Piano. Per giustificare il contatto tra queste due formazioni, che in affioramento risulta invertito rispetto alla successione stratigrafica, abbiamo ipotizzato l’esistenza di una piega isoclinale che che fa affiorare anche le sottostanti Argille di Viano.

Il suddetto detrito di versante su cui peraltro e’ costruita la parete bassa di Sagliano, e’ ricoperto da suolo. Occasionalmente al suo interno sono riscontrabili frammenti delle formazioni di M.Vallassa e M.Lumello, comunque fortemente alterati.
Nella zona a ovest di Sagliano, la fault, which creates a considerable slope, Touch the Marne M. Lumello clay with breccias 2, suppose that there are under the debris slope. In this 'area and the fault' and reverse, we hypothesized that it will continue eastwards. The fault would thus be a whole ', of a rotational system. Still in the area west of Sagliano, and 'one set of minor faults that intersect with dipping towards the east, the main fault. The latter, as mentioned above, and 'reverse, while the secondary ones are directed. You can 'assume that the main fault is generated during the orogeny, while the secondary ones in a post orogenic extensional phase.

Above the Marne M. Lumello, with a stratigraphic contact, there are the Sandstones M. Vallassa It continues to appear to the north in the upper part of the relief.
In the upper part of the country Sagliano, there emerges the M. Lumello. Nevertheless, it is' clearly manifested its presence just outside the village going west, just after a gully. It therefore seems possible that there is a fault along the gully sub-vertical moving and re-emerge in the west of the Marne M. Lumello. The existence of this fault and 'supported by the presence along the canyon of very irregular structure of M. Vallassa that suggest a somewhat sblocchettata by tectonics.

order to give more scorrevolezza alla precedente trattazione, abbiamo preferito limitarci a citare alcune delle formazioni interessate, che qui di seguito saranno meglio descritte.
Facilmente si individuano le Marne di M. Piano anche grazie alla presenza di una frana attiva rappresentata in carta. Esse si presentano con una matrice prevalentemente marnoso-agillosa che assume spesso una colorazione a bande rosate e grigie. All’interno sono presenti intercalazioni carbonatiche e silicee.

La Formazione di M. Lumello , contrassegnata da una buona competenza, e’ prevalentemente marnosa, caratterizzata da un cemento non completamente carbonatico ma in parte siliceo. Numerose sono le intercalazioni arenacee a grana medio-fine e presenta a light gray color with black and yellow patina of alteration. The

Sandstones M. Vallassa , which correspond to the redistribution of material deltaic deposits, granuometria to assume a medium-fine to coarse and often show a prominent layering with medium to thick layers (10-50 cm). Typically have a yellowish or blackish, largely due to the alteration. Their expertise and 'substantial and are strengthened by a carbonate cement. Applicants are traces of bioturbation and small fragments of fossils.

CONCLUSIONS From a structural standpoint it was found to have of a fold Sinform isoclinal geometry, formed during the orogenic process that led to the formation of the Apennines. The fold has been generated in the oldest age groups compared to the formation of M. Lumello.
Then in more recent, the formations were deposited displaced by thrust faults, parallel to each other and genetically related, which led to contact formations of different ages.
Upon detection of the faults we have found direct minor (in the formations of Mt and Mt Vallassa Lumello), not cartography, we hypothesize that the presence of these structures is caused by phenomena soothing during periods of stasis of wrinkling.