ABSTRACT

The present paper intend to show the main geological and geomorphological sites preserved in the Chapada dos Veadeiros National Park and neighbourhod. Among the sites of geologic interrest the lithologic, sedimentological and structural aspects are evidenced, while the most important geomorphological features are associated to the highlands, ridges and hills of great natural beauty. The publication of these data set is important because the region shows ample touristic potential, and the sites preservation is associated to the knowledge of their importance, fragility or rarity. In general the tourists do not have any information about the origin, importance or particularity of the places and structures visited, what brings risks to the preservation of the natural sites found in the region.

INTRODUCTION

The Chapada dos Veadeiros National Park (CVNP) is one important area of environmental preservation that includes on its limits many natural monuments and sites with particular interest on geological and geomorphological features. In the park there are many areas that because of their natural beauty must be considered geological sites of Brazil. Despite being a permanent preservation area these sites are still exposed to risks, however the protection and publication of this information is of great importance.

This paper is the summary of the geologic mapping (1:100.000 scale) carried out at the region of the park and neighbourhood (Dardenne et al. 1998 and Martins 1999). The geologic map was elaborated by the integration of field data, satellite image (1:100.000 scale) and aerial photographs (1:60.000).

LOCALIZATION

The National Park of the Chapada dos Veadeiros is located in the northern segment of Goiás State in central Brazil, with an area of 60 square kilometers, in the follow coordinates: 13^o 51´ and 14^o 10´ south latitude and 47^o 25´and 47^o 42´ west longitude (figures 1 and 2). The access from Brasilia, is by the BR-020 until reach the GO-118 State road, from where turns towards north and get the São Gabriel and São João D´Aliança villages after what reaches to the de Alto Paraíso town. The east limit of the park is around the GO-118 State road (between Alto Paraíso and Teresina de Goiás towns) and the south limit follows the State road that links Alto Paraíso de Goiás to Colinas do Sul.

Figure 1 – Location and access map of the Chapada dos Veadeiros National Park.

Figure 2 – Distribution of the main attractions and important points with geological sites (sedimentary structures and geomorfological aspects).

Among the main tourism attractive (park and neighbourhood) the 120 meters, the 80 meters, the São Domingos, the Cordovil, the Raizama and the Carioquinhas waterfalls, the region of the Canyons, Carrossel, Vale da Lua and many trails and beautiful landscapes are the points most appreciated by the visitants (photographs from 1 to 8).

Photographs 1 and 2 – General view of I and II Canyons (Preto River).

The Rio Preto region called the I and II Canyons is basically represented by the Q₂ Unit. These rock types are characteristically composed by medium to coarse quartzite associated to fine conglomerates lenses, generally present at the top of the quartzite banks. Intercalated beyond the two canyons, there is a metric level (2,5 to 3,0 meters) of a grey metasiltstone rich in non-orientated cyanite crystals. Along the two margins of the river it can observed many sedimentary structures that indicate depositional conditions related to high tidal energy environment. Among the structures the parallel bedding, cross stratification, herringbone and asymmetric ripple marks are the most common. The lithology show general attitude N60-70E dipping 25^o towards SE. The features called I and II canyons represent the channeling of the water flux in great open vertical fractures, respectively in the N30W e N60E directions.

Photography 3 – Partial view of the Carioquinhas Water Fall (Preto River).

This locality represents a little water fall about 12 meters preserved in the Q₂ Unit quartzite. In this place the cross stratification indicating opposite paleo currents directions are quit common, what show tidal depositional conditions. There is also observed along the river margin scarps many sandy sigmoid bodies associated to tidal environment. The quartzite are medium to coarse but rarely show conglometaic lenses. In the area many, fracturing directions are observed, the N60W pattern is associated to the waterfall and the N30W and N45E are also observed.

Photography 4 – Overturned cross bedding of the Pedreira region.

The Pedreira region is represented by a great sequence of quartzite outcrops along the river margins and fast stream. In this place the medium to coarse quartzite show many different cross stratification (overturned, tabular and herringbone). All types of cross stratification indicate high energy in a context of tidal reworking environment. Especially the overturned types show the reworking of previously deposited sandy layers.

The geomorphology observed in this area is associated to an intense fracturing pattern, where quartzite blocks in the boundary of fracture planes make easy the preservation of the structures due to the silicification of the rock.

Photography 5 – General view of the 80 meters Waterfall (Preto River).

Waterfall located next to the geological contact between the Q₂ quartzite Unit and the MS₂ metasiltstone Unit. In the sandy and pelitic intercalation observed next to the base of the waterfall there are many quick sand structures. The waterfall is related to a N60E fracture plane.

Photography 6 – General view of the 120 meters Waterfall (Preto River).

Waterfall supported by carbonate bearing metasiltstone, where there are fine to medium quartzite intercalation in the upper portion. The bedding and the horizontal lamination are the sedimentary structures observed in the quartzite, and in the metasiltstone there are a pervasive slate cleavage.

The geologic context indicates the external portion of the marine shelf with pelitic deposition by suspensive processes. The quartzite intercalation indicates the sandy entrance as the result of fast sea level variation or as a result of storm events in the internal shelf portion.

Photography 7 – General aspect of Vale da Lua site (São Miguel River).

It corresponds to a sequence of fast stream and boreholes present along the São Miguel River. This visiting point is not in the CVNP boundary, and is located about 5 km southwest the São Jorge Village. The area is composed by diamictites showing a greenish grey pelitic matrix and immersed clasts, belonging to the basal unit of the Paranoá Group. The great boreholes observed are produced by the dissolution of the carbonate material present in the matrix and in the clasts of the diamictite. The sedimentation of this unit is related to alluvial fans in arid climate, and deposition is associated to debris flow processes.

Photography 8 – General view of the Salto do Raizama (point of convergence of the Raizama Stream and the São Miguel River).

It corresponds to a waterfall, also located out of the boundary of the park. The waterfall is supported by metasiltstone correlated to the upper unit of the Araí Group. Next to this area there are diamictites associated to the São Miguel Unit.

Regional Geological Context

The region of the CVNP is associated to the northern portion of Brasilia Thrust and Fold Belt in the Tocantins Structural Province. In the park, the metasediments of the Araí Group cover the major area. Towards north there are the gneiss and the granitic rocks that configure the regional basement. Towards south, there is the discordant contact of the Paranoá Group rocks. In this sense there will be described the Paleoproterozoic gneiss-granitic complex, the Paleo-Mesoproterozoic Araí Group and the Meso-Neoproterozoic Paranoá Group.

The gneiss-granitic Complex represents the regional basement, is well distributed towards north of the park and comprises the low lands of the Rio Claro valley. This gneiss and granitic rock complex is constituted by tonalitic and granodioritic orthogneiss associated to great batholiths of granitic composition, commonly represented by biotite granite. In general the foliation is marked by mafic and felsic banding and shear bands with milonitic and cataclastic foliation in ruptile and ruptile-ductile zones.

The majority of age determinations by K/Ar radiometric methods provide ages varying from 500 to 2500 Ma. (Hasui & Almeida, 1970; Cordani & Hasui, 1975 and Hasui et al., 1975). However, Rb/Sr isocrons and U/Pb dating in the supracrustal rocks allow the interpretation of Paleoproterozoic ages to these rocks (Pimentel et al., 1991). The youngest rocks are related to metamorphic events during the following orogenetic cycles.

All along the basement belt there are granitic batholiths intrusions associated to the Paranã Tin Sub-Province. U/Pb dating indicates Paleo-Mesoproterozoic ages (ca 1770 Ma.; Pimentel et al., 1991) to these rocks. The batholiths are represented by biotite granite, chemically compatible to anorogenic granites (type A granites).

The Araí Group corresponds to low grade greenschist metamorphic sediments, deposited in continental, transitional and marine environments associated to the evolution of a Paleo-Mesoproterozoic rift. This unit was initially described by Barbosa et al. (1969) and Dyer (1970), and has been divided into the Arraias and Traíras formations. The Arraias Formation represents the sandy-conglomerate basal succession with 1000 meters thickness, that recovers in discordance the gneiss and granitic basement. The Traíras Formation is constituted by a sandy-pelitic sequence with little carbonate contribution in the upper portion of the succession, that reaches 1200 meters in total thickness. Araújo & Alves (1979) in detailed geological mapping considered a total thickness of 1140 meters to all the Araí Group and divided it in six units, where the 1 to 3 units correspond to the Arraias Formation and the units 4 to 6 are related to the Traíras Formation.

Marini et al. (1984) consider important lateral variations in the thickness and compositions of each facies due to the distance of the source areas of the sediments.

The Araí Group presents a structural polarity, where the most intense deformation (isoclinal folds) is in the internal portion of the Brasilia Belt. Towardss the cratonic area open folds represent the deformation. Locally the structural features are complicated by the lineaments that represent important transcurrent zones, resulting in stratigraphic problems with the elimination or thickening of units.

The Araí Basin origin is related to the evolution of a north-south trend continental rift, which was evolved by reactivation of weakness zones present in the gneiss-granitic basement. The U/Pb ages obtained from zircons of the acid volcanic rocks from the base of the Araí Group show that the rift evolved in limit of the Paleo to the Mesoproterozoic (1770 Ma., Pimentel et al., 1991).

Covering the Araí Group in erosive discordance, the Paranoá Group which is present southwards the CVNP is a psamo-pelitic-carbonated sequence. This unit can be followed towards south along the Serra Geral do Paranã Ridge in the Alto Paraíso, São João D’Aliança, São Gabriel e Distrito Federal regions (Faria, 1995). Faria (1995) purposed an integrated stratigraphy that can be correlated regionally in the external portion of the Brasilia Belt. The units are called from code-letters, from the base to the upper: SM, R₁, Q₁, R₂, Q₂, S, A, R₃, Q₃, R₄, PC. The main characteristic of the units distributed to the south of the CVNP, including some of the geological sites considered here, are described:

- SM Unit (locally called the São Miguel conglomerate): represented by a diamictite with siltstone, quartz, quartzite and marble clasts, immerse in a siltic- argillaceous-carbonatic matrix. The massive aspect of the rock makes difficult to observe the form and composition of the clasts. This unit can be followed for great distances even though it is not a continuum layer.

- R₁ Unit: shows a concordant contact with the basal conglomerate and is constituted by a succession of intercalation of siltstones, pelitic bearing carbonates and fine to coarse feldspatic quartzite. Dissecation cracks and salt cube pseudomorphs are often observed in the base of the sequence. Towards the top of the sequence undulated quartzite and argillaceous metasiltstone intercalations are predominant.

- Q₁ Unit: is represented by fine to medium, white, well stratified banks (30 to 40 cm) quartzite and occasionally intercalation of argillaceous siltstone. Cross stratification is quite common in the top of the layer.

- R₂ Unit: shows an abrupt contact with the Q₁ quartzite, and is characterized by fine pink quartzite banks intercalated with siltstone and white pelitic levels. Cross laminations cut by waves, ripple marks, quick sand, fluidization structures and dissecation cracks are commonly observed.

- Q₂ Unit: constituted by centimetric to metric, white to yellow, medium quartzite, commonly fine, with rounded clasts and feldspatic rich conglomerate filling channels. Many types of cross stratification are common.

The depositional systems associated to the Paranoá Group are related to shallow marine conditions, and the variation in sand and pelitic proportions attributed to the variations of the water deepness due to transgressive and regressive events.

The metamorphism related to the Paranoá Group can be determinate by the phengite and chlorite paragenesis and is characteristic of very low grade (low greenschist facies). Just in the internal zone of the Brasilia Belt (e.g. Niquelândia or Minaçu) the rocks may be associated to the biotite zone of the greenschist metamorphic facies. In the great majority of the occurrence areas the sedimentary structures are well preserved.

Stratigraphy and Depositional Systems of the CVNP

The stratigraphy of the Araí Group was made up in the occidental portion of the park (Rio Preto Ridge) where the sedimentary layers are just few affected by the folding associated to the transcurrent zones. This stratigraphy is representative of the major area of the CVNP, excepting the north portion associated to the Santana Ridge, where a different succession can be observed. In both cases, the Araí Group lies over the granitic basement.

The Rio Preto Ridge occupies the main area of the CVNP and presents a WSW-ENE trend. These quartzite and metasiltstone are divided in six main units.

The basal quartzite Q₁ overlies in discordance the basement granites. Two main facies Q_1f and Q_1P were established.

The Q_1f facies is distributed towardss the westhern portion of the Rio Preto Ridge, and outcrops as one straight south to the Gavião Farm. It is constituted by coarse quartzite, and lithic/arkosean metaconglomerates of fluviatile origin with cut and fill channels and cross stratification. The thickness of this facies is about 50 meters.

The Q_1P facies occurs preferentially at the base of the Rio Preto Ridge scarp, as laminated quartzite with low angle cross stratification, probably associated to a beach transitional environment.

The MS₁ Unit overlies the basal Q₁ quartzite. This unit is distributed in the occidental portion of the Rio Preto Ridge, and is represented by a thick horizon of grey, laminated calciferous metasiltstone, locally undulated. They show quartzite intercalation that may reach 20 meters thickness. Locally, pink to red carbonate boxwork can be observed. A cleavage dipping southward is commonly developed. The sedimentation is represented by agradation process in low energy marine conditions. The thickness is variable, and the great values are measured in the region of the Rio Preto waterfalls, where values of 100 meters can be observed. Laterally towards northeast the metasiltstones reach thickness of 30 to 50 meters.

Intermediate Quartzite: Q₂

The intermediate quartzite Q₂ overlies the MS₁ metasiltstone and is the most representative and well-distributed unit of the park in the NE-SW direction. The quartzite marks the scarp of the north front that limits the low lands of the basement (Rio Claro Valley) and the central portion of the CVNP. This unit is characterized by a thick medium to coarse quartzite sequence with tabular, channeled inverse and herringbone cross stratification that is typical of a tidal environment (photography 9). The thickness of the intermediate quartzite can locally reach 200 meters. Some horizons of laminated metasiltstone are found intercalating the quartzite and the thickness of these pelitic rocks vary from 5 to 30 meters. The great diversity of the sedimentary structures with different cross stratifications and convolute laminations, asymmetric ripple marks and fine conglomerates characterize an environment of transitional deposition dominated by tidal.

Photography 9 – Herringbone cross stratification. The upper set indicates flow to north/northeast, while the bottom one show flux direction from north to south/southeast.

Intermediate Metasiltstone: MS₂

The MS2 unit overlies concordantly the Q₂ quartzite. They are weathered foliated metasiltstone with brownish marks interpreted as weathered carbonates. These rocks represent the low lands of the CVNP, associated to the isolated so-called Ferro de Engomar, Chapéu and Conceição hills. Fine to medium quartzite intercalations with low hummocky and tabular cross stratification are present. The thickness is variable from 50 to 100 meters. The depositional conditions are interpreted as the external shelf associated to storm events.

Upper Quartzite: Q₃

The Q₃ unit is represented by fine to medium, white, micaceous, weathered quartzite sequence, with tabular cross stratification. The thickness is about 125 meters. The Q₃ quartzite is responsible for the preservation of the scarps observed in the south portion of the park, which show important landscapes of geomorphological interest. A tidal reworking environment represents the sedimentation.

Upper Metasiltstone: MS₃

The MS₃ unit overlies concordantly the Q₃ quartzite and represents the last unit of the Araí Group in the CVNP region. This unit is recovered in erosive discordance by the São Miguel conglomerate (base of the Paranoá Group) that is distributed southward. The MS₃ metasiltstone show a massive aspect, they are generally grey to greenish grey and contain carbonaceous intercalations, when they turn dark grey to black. The rich carbonaceous layers may present fine sand intercalation and show abundant quick sand structures (photography 10). The metasiltstone are folded, but commonly dipping south about 5 to 10^º. A pervasive cleavage is observed. The sedimentation is related to a calm deep marine environment. However the sandy intercalation show HCS and wavy undulations that represent the episodic influence of storms during the sedimentation. At the top of the unit, lenses of intraclastic and oolithic limestone may be observed in the São Miguel River, immediately below the basal Paranoá Group conglomerate. This carbonate facies is associated to regressive events related to the final stages of the Araí Basin sedimentation.

Photography 10 – Quick sand structure developed in the early stages of the diagenesis, when the sand was forced out because of the conate water expulsion due to the burying of basin.

SANTANA RIDGE

This corresponds to the northern portion of the CVNP where the stratigraphy observed is totally different from that one described to the Rio Preto Ridge (the stratigraphhy presented was defined in the trail of the old "Chiqueirinho" quartz mining.

Aeolian Quartzito: Qe

Over the granitic basement, there is a sequence of fine white quartzite showing metric cross stratification typical of eolic sedimentation (photography 12). The thin section analysis shows bimodal laminations and locally well rounded grains. The thickness of the Qe unit is between 50 and 70 meters.

Photography 11 – Cross stratification set. The aspect of high angle at top and low angle in the base is typical of aeolian origin

Conglomerate: Cg

The conglomerates overlie the eolic quartzite. This unit is characterized by a thick sequence of conglomerates with clasts composed essentially by intraformational quartzite, less or more rounded or elongated which depositional environment is interpreted as storm beach deposits. This unit reaches thickness up to 20 meters. The lateral distribution shows a lenticular pattern and its continuity, although not well defined, seems to overlap the limits of the park (the conglomerate has been observed in the Cavalcante Ridge). Locally there are intraformational conglomerates, supported by the clasts, with angulous fragments (breccias) with little sandy matrix related to gravitational flux in fault scarps.

Upper Quartzite: Qs

After the conglomerates, there is a quartzite sequence with cross stratification and little cut and fill channels that are related to a tidal depositional environment. The thickness is estimated to be between 50 and 100 meters.

The figure 3 shows the integrated stratigraphy defined by the main geologic sections and the figure 4 detail of two schematic geologic sections that show the distribution of the units.

Figure 3 - Integrated stratigraphy of the Chapada dos Veadeiros National Park. The great majority of the sites are preserved in the Q₂ Unit.

Figure 4 - Two schematic sections, showing the spatial distribution of the main units that constitute the geology of the CVNP.

Paleogeography

In a general view the paleogeography in the CVNP area is related to the evolution of an intracratonic rift, where the basal sediments of the Araí Group show the continental environments (sin rift phase) and the marine sediments of final stage characterize the post rift phase. This basin gets deep northwards and probably towardss west. Two mega sequences were identified, the basal continental one and the transgressive marine one (figure 5). The marine mega sequence show three transgressive cycles, with finning upward sequence, characterized by sandy sediments at base and pelitic ones towardss the top of each cycle. The main terrigenous apports were from north to south, how can be shown by the preliminary paleocurrent data obtained from cross stratification structures.

At north, in the Santana Ridge, the presence of aeolian and conglomeratic facies may mark the northern limit of the marine facies. Regionally these continental facies seem to be distributed until next to the Cavalcante Town, around the gneiss granitic nucleus.

Part of the conglomeratic facies (breccias) must represent talus deposits of basin margin or faults scarps. In areas uplifted by WE faults, the psefitic products are reworked by the storms in a beach environment.

The paleocurrents in the Q₂ quartzite indicate intense tidal influence, showing variable flux direction and even for opposite direction. The main poles indicate 300/350^o and 170^o azimuths.

Figure 5 – Diagram block showing schematically the regional distribution of the main sedimentary facies. Data from geologic mapping in areas located northward confirm the position of the source areas.

Structuration

The CVNP area is situated in a stable area (in the tectonic point of view), where the sediments of the Araí Group lie over the gneiss granitic basement. However, the region is intensively affected by a ruptile tectonism characterized by the presence of great transcurrent and normal faults that modify the sedimentary sequence of the Araí Group. Four different structures assembly was distinguished:

1- Transcurrent faults – the most important structures are parallel to the sedimentary layers, striking N60E. These structures affect indiscriminately the gneiss granitic basement and the Araí Group sediments, by milonitization of the basement and perturbation of the sedimentary succession. Regionally these structures are related to the fracturing parallel to the main direction, locally "en echelon" (photography 13). Some large quartz bearing veins are associated to these faults. The movement of the transcurrent faults is dextral, and is responsible in the NE portion of the CVNP for the development of folds with axis varying from N60-70E to NS (Fonseca & Dardenne, 1995). At the southwest of the park a transcurrent fault runs along the contact between the Araí and the Paranoá groups.

Photography 12 – Detail of fracturing showing escalated pattern developed in a quartzite layer intercalated in metasilstone sequence.

2 – Normal faults and fractures – some apparently normal faults show regional importance, with directions varying from N30-60 E to N30W. The main N30E direction is characterized by quartz vein filling, which has been intensively explored by garimpeiros. A pervasive fracturing is typical in the area with vertical attitude of N60E to N40-60W. The N40-60W fractures are also na important quartz vein control.

3 - Cleavage/schistosity – in all the area a pervasive cleavage showing variable direction can be observed, but the main attitude is N30E dipping to southeast. This cleavage is locally well defined in the quartzite, evolving to a schistosity in the metasiltstone, and indicates the occurrence of compressive stress from NW to SE. In the pelitic rocks, the foliation can be defined as a slate cleavage.

4 - Folds – in general in the CVNP there are just open folds, reflecting the large ondulations observed in the isolated hills along the road from the Alto Paraíso town to the São Jorge Village. In the northeastern portion of the park the NS and N20E folds well preserved in the Araí Group are rotate to the N60-70E direction by the transcurrent fault called Cavalcante-TerezinaTranscurrent System (Fonseca & Dardenne, 1995). They are represented by holomorphic folds with vertical axial plane or dipping westward and promoting layers thickening, what is well observed in aerial photographs and satellite images.

Geomorphology

In the CVNP region and neighbourhood three geomorphological compartments can be defined and the evolution of the relief pattern is related to the bedrock and tectonic structuration. The compartments are called the Rio Claro Valley Region, Ridge Region and Highlands Region. The Rio Claro Valley Region corresponds to the low lands, with plane to undulated terrain, developed at 400 meters over granitic basement rocks. The boundary between this compartment and the Ridge Region is evidenced by a great scarp with SW-NE general direction and with 40 km long, that represents the northern limit of the park.

The Ridge Region is located in the middle-northern portion of the park, including the Rio Preto, Santana, Capim Branco and all areas of high lands in the south of the park (south of the Cordovil and São Miguel streams). This geomorphological compartment is related to the bedrock where quartzite is the dominant petrographic type, and where the greatest altitude are observed (1,200 and 1,500 meters). In the north portion the scarps are supported by the Araí Group quartzite while southward the ridges are related to the basal Paranoá quartzite (mainly the Q₁ and Q₂ units). The road that links the Alto Paraíso Town to the de São Jorge Village is situated along a plane region between two high lands associated to the Araí quartzite (towards north) and to the Paranoá quartzite (towards south).

The Highlands are distributed along the central portion of the park and are characterized by plane relief pattern with some isolated tabular hills that mark the regional landscape, among them the Baleia Hill, Palha Virada Hill, Peito de Moça Hill and the Ferro de Engomar Hill.

The soil coverage is characterized by cambisoils and litholic soils. The hidromorphic soils are observed in the great majority of the spring regions. The Três Lagoas region is a very beautiful area associated to hidromorphic soils, with specially adapted vegetation. The vegetation cover is characterized by typical savanna in the great part of the region. Along river and stream valleys the ciliar forest is commonly observed.

The CVNP area is important in the geomorphological point of view, because in its limits rare geomorfological compartments are preserved, and the study of the origin and evolution of these features is useful to the understanding of the geodynamic regional processes. In the region landscape the most elevated point of the Middle-West region of Brazil with altitude superior than 1.700 meters is found (Boa Vista Ridge, next to the western limit of the CVNP).

PRESERVATION PROGRAM

As the CVNP is a region of environmental protection, the great majority of the areas with geological or geomorphological interest are preserved. However there are areas, especially those out of the CVNP limits, where the risks of degradation really exist. The risks are related to the bad management of the touristic exploration. The main problems are listed as following:

• Waste accumulation in the visiting areas and neighbourhood;
• Pitching of natural monuments (as locally observed);

• Reactivation of erosive processes in bad programmed trails;
• Elimination of the native vegetation for the construction of trails and roads.

To get improvement in the touristic exploration of the CVNP several measures can be taken on, mainly in the sense of getting a more cultural character of the local ecoturism exploration. The visitors may be informed about the genetic aspects of the structures observed, of the landscapes, of the rock formation and some other features of the natural environment, which are important for the space transformation. Among these measures the following can be listed:

• Production of spelling books in simple language, with the main aspects of the general environment;
• Distribution of plates with local references of the most important types of rocks and formation environment and sedimentary structures, type of geomorphological compartment and so one;
• Restriction to the number of simultaneous visitors in each point of visitation.

ARAÚJO, V.A. & ALVES, A.C. 1979. Projeto Cana Brava - Porto Real. Relatório Final. DNPM/CPRM. Goiânia 5 Vol.

BARBOSA, O. et al. 1969. Projeto Brasília - Goiás: Geologia e inventário dos recursos minerais. DNPM-PROSPEC. 2 vol.

CORDANI, U.G. & HASUI, Y. 1975. Comentário sobre os dados geocronológicos disponíveis para a Folha de Goiás. Carta Geológica do Brasil ao Milionésimo. Brasília. p. 85-95.

DYER, R.C. 1970. Grupo Araí, um grupo de metamorfitos do centro leste de Goiás. Rev. Esc. Minas, 28(2). Ouro Preto.

FARIA, A. de 1995. Estratigrafia e sistemas deposicionais do Grupo Paranoá nas áreas de Cristalina, Distrito Federal e São João D’Aliança-Alto Paraíso de Goiás. Universidade de Brasília. (Doctorate Thesis). 199p.

FONSECA, M.A. & DARDENNE, M.A. 1995. Tectônica transpressional no contexto do núcleo metamórfico externo da Faixa Brasília em seu segmento setentrional. 5o. Simp. Geol. Centro-Oeste. SBG, Núcleos Goiânia e Brasília. p. 84-86.

HASUI, Y. & ALMEIDA, F.F.M. 1970. Geocronologia do Centro-Oeste brasileiro. Bol SBG 19(1):5-26. São Paulo.

HASUI, Y.; HENNIES, W.T. & IWANUCH, W. 1975. Idades K-Ar do Pré-Cambriano da região centro norte do Brasil. Bol. Inst. Geoc., USP. 6:77-83. São Paulo.

MARINI, O.J.; FUCK, R.A.; DARDENNE, M.A. & DANNI, J.M.C. 1984. Província Tocantins - Setores Central e Sudoeste, in: Almeida, F.F.M de & Hasui, Y. O Pré-Cambriano do Brasil. p. 251-299.

PIMENTEL, M.M.; HEAMAN, L.; FUCK, R.A & MARINI, J.O. 1991. U-Pb zircon geochronology of Precambrian tin-bearing continental type acid magmatism in central Brasil. Precambrian Res. 52:321-335.