9944-60330-1-PB Seppomen

7/29/2019 9944-60330-1-PB Seppomen

1/8

http://www.uem.br/actaISSN printed: 1806-2563ISSN on-line: 1807-8664

Acta Scientiarum

Doi: 10.4025/actascitechnol.v34i1.9944

Acta Scientiarum. Technology Maring, v. 34, n. 1, p. 71-78, Jan.-Mar., 2012

Edivando Vitor Couto*, Edison Fortes, Michael Vinicius Sordi, Amrico Jos Marques and

Bruno Aurlio Camolezi

Universidade Estadual de Maring, Av. Colombo, 5790, 87020-900, Maring, Paran, Brazil. *Author for correspondence.E-mail: [email protected]

ABSTRACT. This article presents the seppmen map technique through the computer applicationby using the free GIS software SPRING. The methodology was applied to the study in the case ofthe geomorphologhical evolution of the Parana plateaux edges contained in the Faxinal topographicsheet state of Paran - Brazil, the results were the digital elevation models (DEM) and topographicshapes that leads to the landform evolution of the area both by differential erosion but also by strong

tectonic control.Keywords: seppmen, Faxinal sheet, Parana plateaux edges, GIS.

RESUMO. O presente artigo apresenta a metodologia da tcnica de confeco de mapas de seppmen(mapa de nvel de topos) por meio da aplicao computacional pelo geoprocessamento utilizando osoftware livre SPRING. A metodologia foi aplicada ao estudo de caso da evoluo geomorfolgica dasbordas planlticas paranaenses presentes na carta de Faxinal, Estado do Paran, os resultados foram modelosdigitais de elevao do terreno e perfis topogrficos que apontam para a evoluo da rea tanto por erosodiferencial como tambm por forte controle tectnico.Palavras-chave: seppmen, carta de Faxinal, bordas planlticas paranaenses, geoprocessamento.

Seppmen maps (top level map) aimed at themodeled reconstruction of the past relief, and aremade from topographic maps. The technique wasoriginally presented by Japanese geologists andgeomorphologists (HUZITA; KASAMA, 1977).The English translation of the term "summit levelmap" was little known in scientific circles. The termseppmen comes from the Japanese language whichmeans the plane formed by the contact with thehighest points.

The main seppmen map applications are forpaleorelieves and eroded volcanic buildingsinvestigations as well as morphostructural andmorphotectonic analysis (HUZITA; KASAMA,1977; MOTOKI et al., 2007, 2008, 2009; SICHELet al., 2008).

This paper aims to present the methodologyfrom the use of geoprocessing techniques, using thefree software SPRING version 5 of the NationalInstitute for Space Research (INPE), allowing theminimization of errors in the manual form ofpreparation and in the runtime.

Through seppmen, combined with fieldcontrol, its possible to partially understand theerosion processes that drive the relief evolution, herethe Paran plateau edge, represented by the Triassic-

Jurassic Escarpment, as well as the lithostructuraland morphoclimatic controls, responsible for thesemorphologies development.

This study covers the area represented in thetopographical sheet of Faxinal State of Paran, on the

scale of 1/50.000 (Chart SG-22-V-III-1), locatedbetween 2400' and 2415' south latitude and 5115' and5130' west longitude, including the municipalities ofFaxinal, Cruzmaltina, Grandes Rios, Rosrio do Ivaand Ortigueira in the State of Paran.

This area is in a part of the Paran SedimentaryBasin, north-central region of Paran State. Most of thearea is included in the Second Paran Plateau(MAACK, 1981). The Third Paran Plateau isrepresented by a small portion in the northwest andnortheast of the sheet. The boundary between bothrelief units is represented by the Serra Geral (Figure 1).

7/29/2019 9944-60330-1-PB Seppomen

2/8

72 Couto et al.


Figure 1. Location of the study area - digital elevation model of the Faxinal topographic sheet (Chart SG-22-V-III-1).

In lithostratigraphic terms, the study areacomprises a combination of red to purplesiltstones and mudstones, laminated and withfriable aspect, with gray and red tabular sandstonelayers. These lithologies are from the Paleozoicand correspond to the older units in the area,belonging to the Rio do Rasto Formation.The contact with the Piramboia Formation,superimposed, is through lithological and mildangularity disagreement and marks the beginningof the Mesozoic (SOARES, 1975).

The Piramboia Formation corresponds to a fineto very fine and very crispy sandstone, in a packagethat can reach up to 20 meters thick. The color islight gray to white, with low-angle cross-beddingand sigmoidal and plane-parallel.

The Botucatu Formation occurs over theprevious one and includes red and quartz sandstone,fine to very fine until conglomeratic, very resistantto erosion, and displaying medium to large slottedcross bedding.

Superimposed on the Botucatu Formation andoccupying the stratigraphic column of the studyarea, there are basalts and dolerites of the Serra GeralFormation. This Formation is composed ofsuccessive basalt flows with sandy intercalationsfrom Botucatu Formation at the base.

In the geomorphological context, the areacomprises the Morphostructural Compartment I(DMI) from Fortes et al. (2008), located at thenorthern end of the study area (Figure 1). The mostsingular aspect of this relief unit is the structuralscarps, which mark the contact with theMorphostructural Compartment III (DMII) fromFortes et al. (2008).

The Morphostructural Compartment III(FORTES et al., 2008) corresponds to a zone located inthe western area (Figure 1), and comprises the scarpscontrolled by basalts and dolerites of the Serra GeralFormation and sandstones of the Botucatu Formation.

Lower areas are represented by more friablelithologies, formed by siltstones and sandstones ofthe Rio do Rasto Formation that outcrop in thecentral-southern area (Figure 1). It corresponds tothe Morphostructural Domain IV (DMIV) proposedby Fortes et al. (2008). It presents residual reliefsupported by silicified sandstones of the BotucatuFormation. Diabase dikes cut this relief unit,forming flat tops elongated mountains.

The Faxinal topographic sheet, scale 1/50,000,published by the Ministry of Defense, Chart SG-22-V-III-1, was used as a database to conduct this

7/29/2019 9944-60330-1-PB Seppomen

3/8

Seppmen maps for geomorphic developments analysis 73


work, subsequently the topographic dataprocessing was executed through the softwares"SPRING version 5, (INPE, 2004) and "Surferfor Windows, version 7 (GOLDENSOFTWARE, 1999).

The seppmen maps elaboration, hand made, is

done from the transparent graph paper overlappingon the topographic map, and based on graph paper, amesh is defined which may be 0.5, 1 and 2 km.In each area defined in the mesh, the highest point isplotted, as well as latitude and longitude aredetermined.

By the defined points, a table with theobtained data is create (latitude, longitude, highestmesh altitude) and in the Surfer software, these

values are interpolated generating isolines(contour lines) and allowing to generate digitalterrain elevation models (DEMs) and topographicprofiles.

The seppmen maps development obeys thefollowing steps: a) topographic map division intosquare areas from a pre-defined grid of 0.5 km, b)the highest point marking in each square defined inthe mesh, c) a new topographic map elaborationfrom the contour construction, using only thehighest point in each quadrant, as shown in Figure 2(MOTOKI et al., 2008).

For a computational form development, first, adatabase is prepared in SPRING Software and after

the georeferencing and digitizing of topographic maps,by the isolines (contour lines), it was generated a

rectangular grid or a regular grid. It is definedaccording Felgueiras and Cmara (2001) "as a digitalmodel that approximates surfaces through a rectangularpolyhedron faces."

In the rectangular grid generation process, withSPRING software, you should inform the type ofinput (sample) consisting of the contour and theplane of output information (PI), where the readygrid will be stored.

The interpolator used for generating the grid wasweighted average per share and per quadrant, wherethe weighted average is calculated, the value of theshare of each grid point is calculated from the

weighted average of shares of the eight closestneighbors to this point, but attributed to varying

weights to each sampled by the function thatconsiders the distance from the quoted point to the

grid point, as shown in Figure 3 (FELGUEIRAS;CMARA, 2001).

Through this method it was possible to highlightthe highest points, as shown in Figure 4. Thus, it

was possible to plot the chosen points moreprecisely, since we do not have the problem ofsuperimpose the paper to the chart and theinformation loss that occurs in the traditionalseppmen map preparing method.

After this stage of the study, fine meshes werecompiled, as already shown in the values of 0.5 and

1 km, and superimposed on a rectangular, as shownin Figure 4.

Figure 2. Illustration of the conventional method to prepare the seppmem map (MOTOKI et al., 2008).

7/29/2019 9944-60330-1-PB Seppomen

4/8

74 Couto et al.


Figure 3. Source Felgueiras and Cmara (2001). Neighborsselection per quadrant and per share.

The highest points were sampled, first to the0.5 km grid and then to 1 km grid. In this step, weused the SPRING editing tool. The points wereedited into information plans in MNT categoriesto allow the possibility of informing the altitude

value of each point at the edition moment, usingthe tools to edit points and so provide the highestpoints and graphics editing checked to assign the

altimetric values of each point. Thus, we haveanother points type sample with values of x, y,and z, the points collected for the grids 0.5 and1 km can be observed in Figure 5.

From the points collected, you can createother isoline values for the respective grids 0.5

and 1 km, the actual SPRING softwareautomatically generates the new isolines from anew triangular grid compiled from the collectedsamples.

After the triangular grid generation (TIN), usingthe same MNT tool in isolines generation, you canchoose the completed file or a sample on screen, thesoftware sets the minimum and maximum valuesand after it is chosen the desired interval betweenthe isolines.

Seppmen maps were made for Faxinaltopographic sheet based on 0.5 km and 1 km meshes(Figure 6).

Figure 4. Rectangular grid or regular grid. The screen contains items with altitude values, of which the information of the highest points areextracted for the elaboration of the seppmen map.

7/29/2019 9944-60330-1-PB Seppomen

5/8



Figure 5. Quoted points samples, A) 0.5 km sample grid and B) 1 km sample grid.

Figure 6. A) Paleosurfaces Maps based on seppmen technique, based on 0.5 km grid, and B) 1 km grid.

The cliffs that surround the sedimentary basin ofParan edges, present in the topographic sheet of

Faxinal, show high topographic variations, withvalues less than 380 m in the valleys and reachingclose to 1,100 m in the cliff tops. They also presenthigh angle with slopes above 40 degrees or 47% atthe cliff edges, hills and dikes, as it can be seen inHipsometry and slope maps (Figure 7).

The comparative analysis of the seppmen mapsand Digital Elevation Models (Figures 6 and 8)show that despite the small retreat of theescarpment, the valleys widths were already verysubstantial, very close to the current situation.

The profiles of Figure 9 show a sharp verticalkneeling process of the landscape, typical of

morphoclimatic humid areas, which can range from20 to over 100 m depth, to 0.5 km scale, and from 20to over 150 m when considering the 1.0 km scale.These evidences can be verified from the thickalteration mantle, whose thickness can reach up to25 m, like those developed on basaltic rocks of theSerra Geral Formation, located in the northern area(Figure 9).

Although the topographic profiles extracted fromthe seppmen map indicate morphogenetic activityassociated with the relief intense supergenic change,

7/29/2019 9944-60330-1-PB Seppomen

6/8

76 Couto et al.


evidence of relief polycyclic evolution associated withmorphoclimatic areas more stringent than the currentone can be determined by the different grades of levelsand thresholds, as well as by residual relief andcorrelative deposits of these stages, as detritalpediments, all observed in the field (Figure 9B and C).

Figure 7. A) Hipsometry and B) Slope of the Faxinaltopographical sheet. Chart SG-22-V-B-III-1.

Figure 8. Digital terrain elevation model for the Faxinaltopographic sheet isolines, A) 1 x 1 km resolution, andB) 0.5 x 0.5 km resolution and finally C) MDT without theseppmen technique application.

The presence of residual relief in the lower thirdof the So Pedro basin, near the watersheds of theleft margin of the basin also show paleoclimaticlegacies associated with parallel retreat of the SerraGeral slopes (Figure 10). However, their presencerecorded on seppmen maps indicates that the

activity of harsher climates in ancient times is olderthan that covered by the maps in question.

Figure 9. Faxinal Topographic sheet profile. In all profiles, it isevident the relief lowering by the vertical erosion. The residualrelief and the cliffs show decreases of about 1.0 to 1.0 km scaleand less 300 m to 0.5 km scale.

Figure 10. Partial view of the northern part of the area, whichhighlights the modeled wavy relief on basaltic rocks of SerraGeral Formation and with thick soil predominance (A). Partialview of the scarped fronts relieves, which form the First to theSecond Paran Plateau edges (B, C). The residual relief in formsof inselbergs and pediments (B and C) testify parallel slope retreatprocesses in semiarid climates.

2.5 km 5.0 km 7.5 km 10 km

1.0 km 2.0 km 3.0 km 4.0 km 5.0 km 6.0 km 7.0 km 8.2 km

1.0 km 2.0 km 3.0 km 4.0 km 5.0 km 6.0 km 7.0 km

1 x 1 km

0.5 x 0.5 km

Topographical Sheet

km

7/29/2019 9944-60330-1-PB Seppomen

7/8



The Figure 10 shows that this area of study hasalways been at least two distinct compartments ofrelief. The first located in the north and southwest,

where the higher surfaces are almost flat (Figure10A). This feature shows the basalt flowsimportance in the relief configuration, whichhorizontal arrangement and lithological resistancerepresent the main controlling factors of the hillymorphology current and past. The secondcompartment is represented by the most loweredareas, whose residual relieves were already present(Figure 10).

The digital elevation models of Figure 10 showan increasing process of vertical landscapedissection, which could lead to the conclusion in achange in climatic conditions from dry to morehumid. However, this fact demonstrates thelimitation of the technique, because it assumes that

the highest tops were always at that same altitude.Figure 10 serves to show, in this case, the role ofdifferential erosion in the definition and reworkingof inherited forms (Figure 11).

Figure 11. Extensive alignments of diabase dikes of the SerraGeral Formation. These dikes can control the structure of theescarpment and underline the differential erosion action in thereworking of the inherited relieves from drier climates of the past.

Paleoclimatic interpretations alone do not justify

the rotation from E - W to NW - SE (Figures 6 and8), observed mainly in the amount of So Pedro andBufadeiras river which remains to this day. Thisrotation also shows strong diabase dikes influence inthe differential erosion process.

The present direction (NW-SE) is associated withthe presence of numerous diabase dikes. It is possiblethat the rotation is related to erosion and escarpmentretreat on more friable lithologies of the Rio do Rasto,Piramboia and Botucatu Formations. Thus, theescarpment retreat would have been aborted or evenreduced when erosion has reached the diabase dikes,

lending this geometry for the escarpment.The topographic profiles and the digital terrainmodels demonstrated the differential erosionimportance on relief reorganization and on the

vertical landscape lowering.The litoestructural influence was evidenced by the

rotation of the main escarpment, the upper course ofSo Pedro river, and that limits the Second of theThird Paran Plateau, from a position in the first stagesubstantially W-E to NW-SE today (Figure 6).The lithologic control is achieved by the increasedstrength of diabase dikes in NW-SE, for the pelitic andpsammitic lithologies surrounding the areas.

The cyclic morphoclimatic evolution is wellrepresented by typical relief features and correlativedeposits of cliffs retreat, which were not presentedin this study by the limitations of space in the article.These palaeoclimates testimonials relieves showthemselves quite reworked by the action ofdifferential erosion.

In referring to the limitations of this technique,these are related to the impossibility of thechronological treatment, it is only possible to inferrelative dating by altimetry correlation with knownpaleosurfaces already addressed in scientific literature.

The association between paleosurfaces data withneotectonic evidence also has serious limitations,

although it may submit a good correlation withstructural elements. The paleosurfaces data analysis,based on the seppmen technique requires to startfrom local tectonic stability, considering thatsubsiding tectonic movements may obscure or evenalter the landscape development interpretations.Therefore, interpretations of morphotectoniccharacter require careful analysis.

FELGUEIRAS, A. C.; CMARA, G. Modelagemnumrica de terreno. In: CMARA, G.; DAVIS, C.;

MONTEIRO, A. M. V. (Ed.). Introduo cincia dageoinformao. 2001. Available from: . Acessed on: May.11,2009.FORTES, E.; CAVALINI, A.; VOLKMER, S.;MANIERI, D.; SANTOS, F. Controles morfoestruturaisda compartimentao da Serra Geral: uma abordagempreliminar. Terr@Plural, v. 2, n. 2, p. 279-292, 2008.GOLDEN SOFTWARE. Surfer for Window (version 7).Colorado, 1999. (CD-ROM).HUZITA, K.; KASAMA, T. Kbe oyobi rinsetsu chiikichisitu-zu, 1/50,000. 3. ed. Japo: Secretaria dePlanejamento da Prefeitura Municipal de Kobe, 1977.

7/29/2019 9944-60330-1-PB Seppomen

8/8

78 Couto et al.


MAACK, R. Geografia fsica do Estado do Paran.Rio de Janeiro: Livraria Jos Olympio, 1981.INPE-Instituto Nacional de Pesquisas Espaciais.SPRING (verso 5): geoprocessamento ao alcance detodos. So Jos dos Campos: INPE, 2004. (CD-ROM).MOTOKI, A.; PETRAKIS, G. H.; SICHEL, S. E.;

CARDOSO, C. E.; MELO, R. C.; SOARES, R. S.;MOTOKI. K. F. Origem dos relevos do macio sienticodo Mendanha, RJ, com base nas anlises geomorfolgicase sua relao com a hiptese do vulco de nova Iguau.Geocincias, v. 27, n. 1, p. 97-113, 2008.MOTOKI, A.; SICHEL, S. E.; CAMPOS, T. F. C.;SRIVASTAVA, N. K.; SOARES, R. S. Taxa desoerguimento atual do Arquiplago de So Pedro e SoPaulo, Oceano Atlntico Equatorial. Revista Escola deMinas, v. 62, n. 3, p. 331-342, 2009.MOTOKI, A.; SOARES, R. S.; NETTO, A. M.;SICHEL, S. E.; AIRES, J. R.; LOBATO, M. Reavaliao

do modelo gentico do Vulco de Nova Iguau, RJ:origem eruptiva ou intruso subvulcnica? RevistaEscola de Minas, v. 60, n. 4, p. 538-592, 2007.SICHEL, S. E.; MOTOKI, A.; SAVI, D. C.; SOARES, R.Subvolcanic vent-filling welded tuff breccia of the CaboFrio Island, State of Rio de Janeiro, Brazil. RevistaEscola de Minas, v. 61, n. 4, p. 423-432, 2008.SOARES, P. C. Diviso estratigrfica do mesozico noEstado de So Paulo. Revista Brasileira deGeocincias, v. 5, n. 4, p. 229-25, 1975.

Received on April 11, 2010.

Accepted on August 2, 2010.

License information: This is an open-access article distributed under the terms of theCreative Commons Attribution License, which permits unrestricted use, distribution,and reproduction in any medium, provided the original work is properly cited.

9944-60330-1-PB Seppomen

Documents

Transcript of 9944-60330-1-PB Seppomen