Palynostratigraphy of the Chapada Group and its significance in the ...

Palynostratigraphy of the Chapada Group and its significance in the Devonian 

stratigraphy of the Paraná Basin, south Brazil 

Palinoestratigrafia do Grupo Chapada e sua importância para a Estratigrafia 

do Devoniano, na Bacia do Paraná, Sul do Brasil 

Yngve Grahn *, Paula Mendlowicz Mauller, Egberto Pereira, Stanislas Loboziak 1 

Universidade do Estado do Rio de Janeiro, Faculdade de Geologia, Bloco A – Sala 4001, Rua São Francisco Xavier 524, 20550-013 Rio de Janeiro, RJ, Brazil 

article info 

Article history: 

Received 6 April 2009 

Accepted 11 September 2009 

Keywords: 

Chapada Group 

Palynostratigraphy 

Devonian 

Paraná Basin 

article info 

Article history: 

Received 6 April 2009 

Accepted 11 September 2009 

Palavras-chave: 

Grupo Chapada 

Palinoestratigrafia 

abstract 

The Alto Garças Sub-basin in the northern part of the Paraná Basin evolved differently from the Apucarana 

Sub-basin in the south. The marine environment was shallower in the Alto Garças Sub-basin, which 

contains proportionately more silty and arenaceous rocks. The formations and members defined in the 

Apucarana Sub-basin are therefore difficult to apply in the Alto Garças Sub-basin, where the Chapada 

Group (units 1–4) is more applicable. An integrated miospore and chitinozoan biozonation of the Chapada 

Group facilitates direct correlation between the Chapada Group’s units and the classical formations of 

the Paraná Basin as defined in the Apucarana Sub-basin. The Furnas Formation and Chapada unit 1 constitute 

the same lithostratigraphic unit. Beds with rhyniophytes in the uppermost part of the Furnas Formation 

contain palynomorphs representative of the Si phylozone within the MN spore Zone (late 

Lochkovian), and the rhyniophyte beds occupy the same stratigraphic interval within Chapada unit 1 

(the Lochkovian of the Paraná Basin lacks chitinozoans). The lower part of Chapada unit 2 contains spores 

of the PoW Su spore Zone and chitinozoans of the Ramochitina magnifica and Ancyrochitina pachycerata 

zones, together indicating a late Pragian–early Emsian age-span. The upper part of Chapada unit 2 corresponds 

to the GS (AP) and Per (AD pre-Lem) spore Zones, and chitinozoans of the Ancyrochitina parisi, the 

informal Ancyrochitina varispinosa and Alpenachitina eisenacki chitinozoan zones, thus suggestive of a late 

Emsian – earliest Givetian age-span. Unit 3 is a proximal and lateral facies equivalent of the upper part of 

unit 2. The lower part of unit 4 includes spores typical of the early Givetian Lli (AD Lem) spore Zone and 

chitinozoans of the Ramochitina stiphrospinata chitinozoan Zone; the uppermost (early late Frasnian) part 

contains spores of the lower BMu (IV) spore Zone and chitinozoans of the Lagenochitina avelinoi chitinozoan 

Zone. The sandstones of unit 3 were inundated during the earliest Givetian, and the resultant flooding 

surface marks the base of unit 4 basin-wide. Clearly, the two sub-basins were distinct depositional 

centers during the Devonian. 

Ó 2009 Elsevier Ltd. All rights reserved. 

resumo 

* Corresponding author. Tel.: +55 21 38654700; fax: +55 21 38657093. 

E-mail address: yngvegrahn@hotmail.com (Y. Grahn). 

1 Deceased author. 

0895-9811/$ - see front matter Ó 2009 Elsevier Ltd. All rights reserved. 

doi:10.1016/j.jsames.2009.09.001 

Journal of South American Earth Sciences 29 (2010) 354–370 

Contents lists available at ScienceDirect 

Journal of South American Earth Sciences 

journal homepage: www.elsevier.com/locate/jsames 

A Sub-bacia de Alto Garças, na parte norte da Bacia do Paraná, evoluiu de forma distinta da Sub-bacia de 

Apucarana, ao sul. O ambiente marinho na Sub-bacia de Alto Garças era mais raso, contendo proporcionalmente 

mais siltito e rochas arenosas. Desta forma, é difícil utilizar para a Sub-bacia de Alto Garças, as 

formações e membros definidos para a Sub-bacia de Apucarana, sendo o uso do Grupo Chapada (unidades 

1–4) mais apropriado. Assim, um biozoneamento integrado com base em miospóros e quitinozoários do 

Grupo Chapada toma mais fácil a correlação direta entre as unidades deste grupo e as formações clássicas 

da Bacia do Paraná, tal como definido na Sub-bacia de Apucarana. A Formação Furnas e a unidade 1 do

Devoniano 

Bacia do Paraná 

1. Introduction 

The northwestern part of the Paraná Basin (Fig. 1A) was first 

investigated by Smith (1883). He indicated a stratigraphic succession 

for the Devonian with five layers, in ascending order: (1) coarse 

conglomerate of quartz pebbles passing into; (2) very soft friable 

pink sandstone; (3) mottled arenaceous clays; (4) whitish clay 

shales; (5) succession of thin beds of shales, arenaceous clays and 

sandstones. The fossils collected by Smith in the Sant’Ana da Chapada 

(present day Chapada dos Guimarães) area were later studied 

by Derby (1896), who assigned them a Middle Devonian age. Derby 

(1896) considered Smith’s layer 5 to be overlain by a Mesozoic reddish 

sandstone. Caster (1947, 1952) and Almeida (1948, 1954) were 

of the opinion that this sandstone was present beneath the Devonian 

rocks. Later works by Bigarella and Oliveira (1966) and Oliveira 

and Muhlmann (1967) interpreted the sandstone as Mesozoic (Triassic?), 

and that it progressively overlies older Devonian beds towards 

the northwest. Bigarella and Oliveira (1966) correlated 

Smith’s layers 4 and 5 with the Ponta Grossa shales, and the arenaceous 

layers below with the Furnas Formation. Lange (1967) referred 

the upper layer of Bigarella and Oliveira’s Furnas Sandstone 

(Smith’s layer 3) to his Jaguariaiva Member of the Ponta Grossa Formation. 

Ammon (1893) assigned a Lower Devonian age to fossils 

found by Vogel (1893) at Lagoinha (Fig. 1B), about 40 km east of 

Chapada dos Guimarães, and Clarke (1913) suggested the same 

age for fossils collected by Carnier at Chapada dos Guimarães. However, 

Caster (1947, 1952) and Lange (1967) recognized Middle 

Devonian fossils in the Devonian shales, confirming the results of 

Derby (1896). More recent investigations (Oliveira, 1991, 1997; Oliveira 

et al., 1995; Loboziak et al., 1998; Grahn et al., 2000, 2002; 

Gaugris and Grahn, 2006; Mendlowicz Mauller et al., 2007, in press; 

Mendlowicz Mauller, 2008) gave a more detailed picture of the 

Devonian stratigraphy in the northwestern outcrop belt (Fig. 1A). 

Above the Lochkovian (Gerrienne et al., 2001; Rubinstein et al., 

2005) sandstones (Furnas Fm.) occur late Pragian–early Emsian 

strata (Mendlowicz Mauller et al., in press). No paleontological evidence 

for most of the Pragian (PoW, pre-Su Zone) and middle Emsian 

(FD-AB miospore zones) has been found. Late Emsian to early 

late Frasnian strata are well supported by paleontological evidence, 

but the extent of Eifelian strata is still insufficiently known (Loboziak 

et al., 1988; Grahn et al., 2000, 2002; Gaugris and Grahn, 

2006; Mendlowicz Mauller et al., in press). 

Evans (1894) introduced the term Chapada Group for rocks in 

the northwestern part of the Paraná Basin (Alto Garças Sub-basin), 

and with Chapada dos Guimarães as the type area (Fig. 1B). The 

lithology differs from that of correlative units in the Apucarana 

Sub-basin mainly in that the content of silt and sand is higher. Four 

units were identified and described by Andrade and Camarço 

(1980, 1982) from southwestern Goiás in the northeastern part 

Y. Grahn et al. / Journal of South American Earth Sciences 29 (2010) 354–370 355 

Grupo Chapada constituem a mesma unidade litoestratigráfica. Camadas com riniófitas na parte mais 

superior da Formação Furnas contêm palinomorfos representantivos da filozona Si, dentro da zona MN 

(Neo-Lochkoviano), e as camadas de riniófitas ocupam o mesmo intervalo estratigráfico dentro da 

unidade 1 do Grupo Chapada (o intervalo Lochkoviano da Bacia do Paraná carece de quitinozoários). A 

parte inferior da unidade 2 do Grupo Chapada contém esporos da zona Pow Su e quitinozoários das zonas 

Ramochitina magnifica e Ancyrochitina pachycerata, ambos indicando uma idade Neo-Pragiana – Eo-Emsiana. 

A parte superior da unidade 2 do Grupo Chapada corresponde às zonas GS (AP) e Per (AD pré-Lem), 

quitinozoários das zonas Ancyrochitina parisi, biozona informal Ancyrochitina varispinosa e Alpenachitina 

eisenacki, sugerindo assim uma idade Neo-Emsiana – Eo-Givetiana. A unidade 3 é uma fácies proximal, 

e lateralmente equivalente à parte superior da unidade 2. A parte inferior da unidade 4 inclui esporos típicos 

do início do Givetiano, zona Lli (AD Lem) e da Zona de quitinozoários Ramochitina stiphrospinata; a 

parte mais superior (início do Neo-Frasniano) contém esporos da parte inferior da zona BMu (IV) e da 

Zona de quitinozoários Lagenochitina avelinoi. Os arenitos da unidade 3 foram afogados durante o início 

do Givetiano, e a superfície de inundação resultante marca a base da unidade 4 em toda a Bacia. Claramente, 

as duas sub-bacias apresentavam depocentros distintos durante o Devoniano. 

Ó 2009 Elsevier Ltd. All rights reserved. 

of the basin (Fig. 1A). They referred to them as Furnas Formation 

and the lower, middle, and upper members of the Ponta Grossa 

Formation. Melo (1988) re-validated the Chapada Group of Evans 

(1894), and divided the group into Chapada units 1–4, each of formational 

rank, and each corresponding to the units defined by 

Andrade and Camarço (1978, 1980). 

2. Material and methods 

Except for the locality at Sr. Cristóvão those in the Chapada dos 

Guimarães area (see Fig. 1B and Appendix B) were sampled by Sandra 

Fátima de Oliveira (Universidade de São Paulo, USP) in 1995. 

The predominant Devonian lithologies in the area are reddish siltstones 

and sandstones, which are unsuitable for palynomorph 

preservation. Thus, only the intervals with greyish shales were collected. 

The road-cut at Sr. Cristóvão was sampled by geologists 

from the Federal University of Rio de Janeiro (UFRJ). Details of sample 

thicknesses are unavailable to the present authors. The laboratory 

processing followed standard Petrobras methods (Quadros 

and Melo, 1987). Miospores and chitinozoans were investigated 

in some detail, and the miospore biozones established by Melo 

and Loboziak (2003) were applied together with the chitinozoan 

biozones sensu Grahn (2005) and Gaugris and Grahn (2006). All 

palynomorphs identified are listed in Appendix A. 

3. Geologic setting 

An angular unconformity is present at the base of the Jurassic 

Botucatu Formation sandstones in the northwestern outcrop belt 

of the Paraná Basin. These sandstones cut, from the southeast to 

northwest, a succession of Paleozoic and older rocks ranging from 

the Permian Terezina Formation through crystalline basement 

(Oliveira and Muhlmann, 1967). In the Chapada dos Guimarães 

area the Paleozoic beds dip towards the north–northeast (Oliveira 

and Muhlmann, 1967). The Butucatu Formation dips north–northwest, 

and is in contact with the Furnas (Chapada Group unit 1) 

sandstones immediately west of Buritis town (Fig. 1B). The Furnas 

sandstone has two different facies. The upper facies is a finegrained, 

well-sorted, and mainly plane parallel bedded white to 

purple sandstone. The lower facies is a more coarse grained, 

cross-bedded, grayish or yellowish sandstone, locally with a conglomerate 

containing quartz pebbles at the base. The beds above 

the basal Devonian sandstones consist of grey shales with interbedded 

siltstones and argillaceous sandstones. Several large faults 

are present in the Chapada dos Guimarães area that represent large 

areal displacement during the Mesozoic (Cretaceous?) tectonic 

episodes (Oliveira and Muhlmann, 1967). As pointed out by Melo 

(1988) and Grahn et al. (2000, 2002) the Alto Garças Sub-basin in

356 Y. Grahn et al. / Journal of South American Earth Sciences 29 (2010) 354–370 

S14 o 

S18 o 

S22 o 

1A 

o 

S1520´ 

to Cuiabá S152 

o 5´ 

Sample points 

Unit 2 

Unit 4 

W58 o 

BOLIVIA 

Bauru Fm. 

(Cretaceous) 

Botucatu Fm. 

(Jurassic) 

Cuiabá 

Asunción High 

PARA- 

GUAY 

W54 o 

BURITIS 

CHAPADA 

DOS 

GUIMARÃES 

o 

W5550´ 

W 55 4 

o 5´ 

Cachoerinha Fm. 

(Tertiary) 

Chapada unit 1 

the northern part of the Paraná Basin had a different evolution than 

the Apucarana Sub-basin in the south. The marine environment is 

shallower in the Alto Garças Sub-basin, which contains more arenaceous 

rocks. The two sub-basins were distinct sedimentation 

centers during the Devonian (Melo, 1988; Grahn et al., 2002). 

4. The Devonian stratigraphy of the Apucarana Sub-basin 

Apucarana 

Sub-basin 

The Apucarana Sub-basin geology, first described by Derby 

(1878), is the classical area in the Devonian stratigraphy of the 

1B 

Dom Aquino 

RVR-1 1 

RSP-1 

Jaciara 

2-AG-1-MT 

Felix 

Quarry 

Campo Grande 

High 

2-JA-1-GO 

Paleosul-02-RV-MT 

2-RP-1-MS 

Alto Garças 

Sub-basin 

Precambrian 

basement 

W50 o 

Upper Xingu High 

0 200 400 Km 

5 10 

9 

11 

6 

7 

4 

8 

2 

3 

3 

2 

o 

S1530´ 

Chapada units 2 and 4 

1 

o 

W5540´ 

BRAZIL 

Brasília 

Goiânia or Canastra 

High 

Três Lagoas High 

São Paulo 

W46 o 

LAGOINHA 

Precambrian 

basement 

Devonian 

outcrop belt 

W553 

o 5´ 

0 5 10 km 

Paraná Basin. The Furnas Formation was proposed by Oliveira 

(1912) for basal Paleozoic sandstones in Serra das Furnas, State 

of Paraná. The type area is from west of Campo Largo and extends 

from northwest of Castro to south–southeast of Jaguariaiva (Fig. 2). 

The lithologies consists of coarse-grained, white to yellowish sandstones 

of fluviatile origin, and with a marine influence in its uppermost 

part, where rhyniophyte-bearing siltstones are present. 

Spores and fresh-water phytoplankton (Schizocystia spp.) from 

these siltstones at the Pisa (Fig. 2) locality (Dino and Rodrigues, 

1995; Mendlowicz Mauller, 2008) suggest a late Lochkovian age 

city 

borehole 

outcrop 

International 

boundary 

Arch or 

High 

1 Baliza 

2 South of 

Amorinópolis 

3 Well 02/14 

Iporá 

Fig. 1. A. Location map of the localities from the Alto Garças Sub-basin investigated and/or discussed in this study. B is in the northwestern area of Fig. 1A. B. Geological map 

and sample points in the Chapada dos Guimarães area. Localities: 1 = 11 SD-2. 2 = 11 SD-16. 3 = 7 SD-3. 4 = 11 SD-17. 5 = 7 SD-6. 6 = 11 SD-3. 7 = 11 SD-19. 8 = 11 SD-18. 9 = 7 

SD-7. 10 = 7 SD-1. 11 = Sr. Cristóvão. 

1B

N10 o 

0 o 

S10 o 

S20 o 

S30 o 

S40 o 

S50 o 

W70 o 

W80 o 

W50 o 

W40 o 

W60 o 

W50 o 

BRAZIL 

Paraná Basin 

MATO GROSSO 

DO SUL 

PARAGUAY 

ARGENTINA 

(Rubinstein et al., 2005). Rhyniophyte remains in the uppermost 

part of the Furnas Formation at the Jackson de Figueiredo locality 

(Fig. 2) were dated as early Lochkovian by Gerrienne et al. (2001, 

2006). Conglomeratic layers containing mainly quartz gravel up 

to 1 mm in diameter in a kaolinitic matrix are common through 

the formation, especially in the lower part. The sandstones have 

a consistent paleocurrent pattern towards the southwest 

(Melo, 1988), and the maximum thickness is estimated to be about 

250 m. 

The richly fossiliferous transgressive shales overlaying the Furnas 

Fm. were defined as the Ponta Grossa shales by Oliveira (1912). 

The type section is exposed in railroad cuts between Jaguariaiva to 

Arapoti from km 2.2 to km 6.6 (altitude 860–960 m). The lithology 

consists of grey shales with intercalations of siltstone and sandstone. 

As defined by Oliveira, these shales are clearly underlying 

the Tibaji ‘‘sandstones”, defined by Oliveira (1912) for a 20 m thick 

section of tempestitic, micaceous, silty sandstone exposed along 

São Domingos Creek, a tributary to the Santa Rosa Stream, which 

flows into the Tibaji River. The fauna in the Tibaji ‘‘sandstones” is 

similar to that in the upper part of the Ponta Grossa shales, and 

Tibaji is considered as a member of the Ponta Grossa Fm. in its original 

sense. The fossils display a Malvinokaffric affinity and were 

first described by Clarke (1913), and later partly revised by Melo 

(1988). The age of the lowermost part of the Ponta Grossa Fm. remains 

uncertain in the type area, and the first fossils, some tens of 

meters above the contact with the Furnas Formation, indicate a 

late Pragian–early Emsian age (Mendlowicz Mauller, 2008; Mendlowicz 

Mauller et al., in press). There is no paleontological evidence 

for most of the Pragian (PoW pre-Su miospore Zone) and middle 

Emsian (FD-AB miospore Zones), and the upper part of the formation, 

including the Tibaji Member, is upper Emsian. The Ponta 

Grossa Fm. has a maximum thickness of about 250 m. The Tibaji 

Member s.s. pinches out basinward and reaches a maximum thickness 

of 35 m. According to Candido (2007) the maximum thickness 

of the Tibaji Member should be 130 m, but this figure obviously includes 

the thickness of all upper Emsian–Eifelian sandstones in the 

Paraná Basin. The absence of the Tibaji Member makes the difference 

between Ponta Grossa and overlaying shales less obvious towards 

the center of the basin, and is probably the reason for 


W55 o 

W54 o 

Ponta Grossa/São 

Domingos Formations 

Furnas Formation 

W53 o 

PARANÁ 

Outcrop 

City 

W52 o 

W51 o 

Ponta Grossa 

SÃO PAULO 

Jackson de Figueiredo 

Campo Largo 

W50 o 

Castro 

SANTA CATARINA 

Fig. 2. Location map of the localities from the Apucarana Sub-basin discussed in this study. 

PISA 

Jaguariaiva 

Curitiba 

W49 o 

Oppenheim (1936) lumping all Devonian rocks above the Furnas 

Fm. together in a single ‘‘Ponta Grossa Formation”, and in that process 

the original definitions by Oliveira lost their stratigraphic and 

paleontologic significance. Oppenheim based his conclusions on 

the geology of the Apucarana Sub-basin, and his opinion has ever 

since been accepted by most geologists working with the Paraná 

Basin. An approximately 90 m thick unnamed shale unit above 

the Tibaji unit, at the type locality for the latter, was defined as 

São Domingos shales by Bodziak and Maack (1946). These shales 

differ from the Ponta Grossa shales below. The lithologies are 

shales with siltstone intercalations, and with an increasing content 

of argillaceous shales towards the top. The basal part of these 

shales are at the Emsian–Eifelian transition, and the top is of an 

early late Frasnian age. Most of the Malvinokaffric fauna disappear 

in the lowermost part, and only a few holdovers survive into the 

Givetian (Melo, 1988). The total thickness is about 350 m. Although 

Lange and Petri (1967) recognized the merit of the original definitions 

by Oliveira (1912) and Bodziak and Maack (1946), they introduced 

the Jaguariaiva Member of the Ponta Grossa Fm. for the 

Ponta Grossa Fm. s.s., and considered the Tibaji ‘‘sandstones” as a 

member of this formation. The São Domingos shales were likewise 

regarded as a member of the Ponta Grossa Fm. Melo (1988) and 

Grahn et al. (2000) considered the Jaguariaiva Member as a junior 

synonym of the Ponta Grossa Fm. as originally defined by Oliveira 

(1912). Grahn (1992) regarded Ponta Grossa and São Domingos as 

formations of equal rank, and the Tibaji as a member of the former. 

This approach is followed for the rocks in the Apucarana Sub-basin 

in this study. 

5. The Devonian stratigraphy of the Alto Garças Sub-basin 

When Evans (1894) introduced the Chapada Group for rocks in 

the outcrop belt on the northwestern flank of Paraná Basin very little 

was known about their relationship with rocks in other parts of 

the basin. Nevertheless, his observations and proposal of the Chapada 

Group for the Alto Garças Sub-basin received no general recognition, 

except for the re-validation by Melo (1988). Andrade and 

Camarço (1980, 1982) identified Evan’s units in the Alto Garças 

Sub-basin, and refer to them as Furnas Fm. and the lower, middle, 

N 

ATLANTIC 

OCEAN 

S23 o 

S24 o 

S25 o 

S26 o


and upper members of the Ponta Grossa Fm. These units can easily 

be traced over the sub-basin, but they were not considered by 

Grahn (1992), Grahn et al. (2000, 2002), and Gaugris and Grahn 

(2006), that referred to time equivalence of the classical formations 

in the Apucarana Sub-basin. Units 1–4 of the Chapada Group correspond 

to the four units defined by Andrade and Camarço 

(1980), and they are briefly discussed below. 

Itararé 

Fm. 

South of 

Amorinópolis 

U n i t 1 

Unit 

2 

Unit 3 

Unit 

4 

PC 

1 

Arkosic arenites 

2 

Well 02/14 

Iporá 

3 

4 

5.1. Chapada Group unit 1 (=Furnas Fm.) 

The Furnas Fm. in the Alto Garças Sub-basin was defined by 

Andrade and Camarço (1980, p. 2830) in the Iporá and Amorinópolis 

region (Fig. 1A). The lithology is virtually the same as for the 

Furnas Fm. in the Apucarana Sub-basin, and Chapada Group unit 

1 is considered synonymous with the Furnas Fm. as defined by 

Givetian 

Eifelian 

? 

? 

Late Emsian 

Late Pragianearly 

Emsian 

Late Lochkovian 

Samples 

1. Givetian 

(Daemon in 

Andrade and 

Camarço, 1978) 

2. 

3-4. 

0 

10 

20 

30 m 

Late Pragianearly 

Emsian 

(Grahn et al., 2000) 

Emsian 

(Daemon in 

Andrade and 

Camarço, 1978) 

Coarse-grained 

sandstone with 

channels 

Fine-grained 

argillaceous/silty 

sandstone 

Fine-grained 

kaolinitic 


Conglomeratic 


Silty 

shales 

Diamictites 

Hiatus 

Pre-Cambrian 

basement 

Fig. 3. Lithologic column and ages for the Chapada Group reference sections in the northeastern outcrop belt of the Alto Garças Sub-basin (Outcrop south of Amorinópolis city 

and well 02/14 Iporá). Lithology after Andrade and Camaço (1978, 1980). Biostratigraphy after Daemon in Andrade and Camarço (1978) and Grahn et al. (2000).

Oliveira (1912). However, there are minor differences (e.g. paleocurrent 

pattern is consistently towards the northwest). 

The maximum thickness is estimated to be about 400 m in the 

subsurface (Melo, 1988). Chapada unit 1 is present in the section 

south of Amorinópolis, well 02/14 Iporá (Fig. 3), well RVR-1 

(Fig. 4), Jaciara section, and well Paleosul-02-RV-MT (Fig. 1A; Pereira 

et al., 2007). None of these localities (Fig. 1A) have yielded any 

fossil evidence for the age of Chapada unit 1. Quadros and Melo 

(1986) reported on locally abundant rhyniophyte remains in siltstone 

lenses within the uppermost part of the unit in southwestern 

Goiás, and in the same stratigraphic position as those from the Furnas 

Fm. at Pisa locality (Si phylozone within MN spore Zone of late 

Lochkovian age, Rubinstein et al., 2005). 


5.2. Chapada Group unit 2 

This unit consists of a basal conglomerate with sandstones and 

shales, overlain by reddish sandstones with intercalated siltstones 

and shales, and towards the top grayish–reddish sandstone layers. 

The unit was defined by Andrade and Camarço (1980, p. 2831) in 

the same region as for unit 1 (Fig. 1A). Only the late Pragian – Emsian 

part of unit 2 is present in its type area, where a sample 1 m 

above the base of unit 2 in the Amorinópolis section (Fig. 3) was 

dated as Pragian by Grahn et al. (2000), but the chitinozoan assemblage 

is more likely late Pragian–early Emsian. This concurs with 

the dating of lowermost unit 2, about 4 m above its contact with 

unit 1 in well RVR-1 (Mendlowicz Mauller et al., in press): 

Fig. 4. Lithologic column and ages for the Chapada Group reference section in the center of the Alto Garças Sub-basin (well 2-AG-1-MT). Lithology and biostratigraphy after 

Lange (1967), Grahn et al. (2000, 2002), and Melo and Loboziak (2003).


Figs. 1A and 5. Therefore, most of the Pragian rocks are probably 

missing in accordance with the stratigraphy elsewhere in the 

Paraná Basin. A layer with arkosic arenites might represent the 

middle Emsian, but this requires further investigations of e.g. the 

Amorinópolis section (Fig. 3) to establish. The lower part of Chapada 

unit 2 (=D2a by Lange, 1967) is paleontologically characterized 

by late Pragian–early Emsian palynomorphs. This interval is well 

developed on the northwestern flank of the basin (Fig. 1A) in the 

Jaciara section (Mendlowicz Mauller et al., 2007), well RVR-1 

(Fig. 5), well Paleosul-02-RV-MT (Mendlowicz Mauller, 2008; 

Mendlowicz Mauller et al., in press), and Felix Quarry (Grahn 

et al., 2000), where the shales in the latter locality are overlain 

by a tempestitic sandstone of unknown age. The upper part of 

Chapada unit 2 (=D2b/D3 by Lange, 1967), is complete in well 2- 

AG-1-MT (Fig. 4; Lange, 1967; Daemon et al., 1967; Assine and 

Soares, 1989; Assine et al., 1994; Grahn et al., 2000, 2002) and well 

Fig. 5. Lithologic column and ages for the Chapada Group reference sections in the northwestern outcrop belt of the Alto Garças Sub-basin (wells RVR-1 and RSP-1). L = late 

Lochkovian, E = Eifelian. Lithology and biostratigraphy after Loboziak et al. (1988), Gaugris and Grahn (2006), Mendlowicz Mauller, 2008, and Mendlowicz Mauller et al. (in 

press).

RVR-1 (Fig. 5; Gaugris and Grahn, 2006; Mendlowicz Mauller, 

2008; Mendlowicz Mauller et al., in press). 

The late Emsian part is represented in the Baliza section 

(Fig. 1A; Pereira, 1992; Grahn et al., 2000) and in the Amorinópolis 

– Iporá (Figs. 1A and 3) region (Andrade and Camarço, 1980). The 

total thickness of Chapada unit 2 is about 60 m on the northeastern 

margin of the basin (Fig. 3; only the lower part present), about 270 

m in the center (Fig. 4), and about 200 m in the northwestern margin 

(Fig. 5). 


Chapada unit 3 is restricted to the northeast part of the basin, 

and is laterally replaced by the shales and sandstones of the upper 


(latest Emsian–earliest Givetian) part of unit 2 towards the center 

of the Alto Garças Sub-basin (cf. Andrade and Camarço, 1980). The 

lithologies are reddish sandstones with conglomeratic levels. An 

erosive unconformity at the base of unit 3 extends towards the 

northeast margin of the basin (Pereira et al., 1998). Transitional 

beds between Chapada units 2 and 3 contain the same fauna as 

in the upper Ponta Grossa Fm. and Tibaji Member of the Ponta 

Grossa Fm. (Glaser, 1969; Melo, 1988), thus suggesting a late Emsian 

age for these beds. The sandstones represent a deltaic environment 

on a shallow platform strongly influenced by waves, and also 

contain shale clasts and sporadic channels. The unit has a maximum 

thickness of about 250 m. It was drowned by the earliest 

Givetian inundation. This flooding surface represents the base of 

unit 4 all over the basin (Fig. 8). 

Fig. 6. Table showing selected miospore species present and their occurrences in the Chapada dos Guimarães area. Open circles symbolize probably reworked specimens. = 

Verrucosisporites n. sp. sensu Grahn et al. (2005). The miospores are illustrated in Figs. 10–12. (See above-mentioned references for further information).



The transition between Chapada unit 2 and 4 is developed in 

wells 2-JA-1-GO (Fig. 1A; Lange, 1967; Daemon et al., 1967; Grahn 

et al., 2002), 2-AG-1-MT (Fig. 4; Lange, 1967; Daemon et al., 1967; 

Grahn et al., 2002), 2-RP-1-MS (Fig. 1A; Lange, 1967; Daemon et al., 

1967; Grahn et al., 2002), RVR-1 (Fig. 5; Gaugris and Grahn, 2006; 

Mendlowicz Mauller, 2008) and RSP-1 (Fig. 5; Burjack et al., 1987; 

Loboziak et al., 1988; Burjack and Paris, 1989; Oliveira, 1991, 1997; 

Gaugris and Grahn, 2006; Mendlowicz Mauller, 2008). Chapada 

unit 4 consists of dark grey shales with intercalated fine-grained 

argillaceous sandstones and siltstones. The thickness reaches about 

350 m in the northwest margin of the basin (Fig. 5), ca. 200 m in 

the center (well 2-AG-1-MT, Fig. 4), and about 60 m in the Iporá 

and Amorinópolis region (Figs. 1A and 3; Andrade and Camarço, 

1980, p. 2832). This unit is also developed in the same wells as 

the transition between units 2 and 4, and in the Dom Aquino section 

(Fig. 1A; Oliveira et al., 1995; Pereira, 2000; Grahn et al., 2002). 

The contact with the Carboniferous diamictites in the lower Itararé 

Group is erosional (Fig. 3). 

6. Devonian palynostratigraphy of the Chapada dos Guimarães 

area 

The palynomorphs present in the samples from the Chapada 

dos Guimarães area are representative for a late Pragian to early 

Givetian age span (Fig. 6). Post early Givetian beds are not identified 

in the Chapada dos Guimarães area. The miospore biozonation 

in this area (Figs. 1B and 6) partly corroborates the miospore biozonation 

outlined by Loboziak et al. (1988, 1998), Mendlowicz 

Mauller et al. (2007), and Mendlowicz Mauller (2008) for the 

Paraná Basin. New chitinozoan data have also made it possible to 

refine the Emsian–Eifelian biozonation of Gaugris and Grahn 

(2006) and Mendlowicz Mauller (2008). The presence of Ancyrochitina 

varispinosa in Lange’s unit D3 shows that this unit has a latest 

Emsian–earliest Givetian age span, and that this species is a good 

index chitinozoan for that interval. The outcrop localities are listed 

in Appendix B. 

6.1. Lower part of Chapada Group unit 2 

The lower part of the Chapada unit 2 was collected at locality 11 

SD-2 (Bocaina-Laranjal Stream). Acritarchs were used to achieve a 

more precise age for a critical sample (274) at this locality (Figs. 1B, 

6). Loboziak et al. (1998) considered this sample to represent BZ 

(late Lochkovian) or lowermost PoW (earliest Pragian) miospore 

Zones, an interval corresponding to the uppermost part of the Furnas 

Fm. in the Apucarana Sub-basin (Gerrienne et al., 2001; 

Rubinstein et al., 2005). However, the presence of the acritarch 

Polyedryxium fragosulum in the sample (Oliveira, 1997) indicates 

an age no older than the late Pragian (PoW Su miospore Zone). Furthermore, 

acritarchs are unknown from the Furnas Fm., and the 

Fig. 7. Table showing chitinozoan and common acritarch species present and their occurrences in the Chapada dos Guimarães area. R. stiph. = Ramochitina stiphrospinata. The 

chitinozoans are illustrated in Fig. 9 and the acritarchs in Fig. 12.

chitinozoan fragments present in sample 274 show features unknown 

from the latest Lochkovian. Higher in the outcrop (sample 

273), the miospores indicate a latest Pragian–early Emsian time 

interval (Loboziak et al., 1998). Other localities are 11 SD-16 (Condominio 

Morro das Esperanças) situated on the east margin of 

Capão do Boi Stream (sample 287), 7 SD-3 (Jamacá Stream) represented 

by sample 267, and 11 SD-17 (Source of Jamacá Stream; see 

below). The presence of a short form of Navifusa bacilla (Figs. 9, 

12L) together with Dictyotriletes subgranifer in sample 267 suggests 

an early Emsian age for locality 7 SD-3. The size of the Navifusa 

specimens is probably due to environmental conditions (Fatka 

and Brocke, 2008), and the early Emsian occurrence of Navifusa bacilla 

is in agreement with their contemporary presence low in the 

Stooping River Formation, Moose River Basin, Ontario (Playford, 


Fig. 8. Correlation scheme for the Chapada Group. = Time equivalents in the Alto Garças Sub-basin. = Angochitina praedensibaculata Zone. = Informal biozone. Ti = 

Tibaji Member of the Ponta Grossa Fm. 

1977). In locality 11 SD-17 samples were taken 1.50 m above the 

base of a 5 m thick section (sample 290), and two samples at the 

top (samples 288 and 289). All samples from the localities mentioned 

above are from grey, micaceous shales. The miospore index 

species Dictyotriletes subgranifer (Fig. 10H) is recorded from locality 

11 SD-17 (Fig. 6) together with other common miospore species in 

this interval, e.g. Brochotriletes? foveolatus (Figs. 10A and B), Brochotriletes 

hudsonii (Fig. 11S), Dictyotriletes emsiensis (Fig. 10C), 

Perotriletes caperatus (Fig. 10D), and Zonotriletes simplicissimus 

(Fig. 10E). The presence of Bimerga sp. A (Figs. 7 and 12N), known 

from contemporary strata elsewhere in the Paraná Basin and Bolivia 

(Mendlowicz Mauller et al., in press), is in agreement with the 

miospore data (Fig. 6). The chitinozoan index species Ramochitina 

magnifica does not occur in the Chapada dos Guimarães samples,


Fig. 9. Selected chitinozoan species from the Chapada Group at Chapada dos Guimarães. The scale bar represents 50 lm. A. Ancyrochitina langei. Early Givetian. Sr. Cristóvão. 

Sample 260. L40/1. B. Ancyrochitina langei. Early Givetian. Sr. Cristóvão. Sample 260. U42/4. C. Ancyrochitina cf. A. maacki. Late Eifelian. 11 SD-18. Sample 294. K45/2. D. 

Ancyrochitina multibrachiata. Early Givetian. Sr. Cristóvão. Sample 260. L46c. E. Ancyrochitina morzadeci. Late Emsian–early Eifelian. 7 SD-6. Sample 269. L68/3. F. Ancyrochitina 

parisi. Late Pragian–early Emsian. 7 SD-3. Sample 267. T62c. G. Ancyrochitina parisi. Late Emsian–early Eifelian. 7 SD-6. Sample 266. D48/1. H. Ancyrochitina cf. A. parisi. Late 

Pragian–early Emsian. 11 SD-16. Sample 287. S48/4. I. Ancyrochitina varispinosa. Late Eifelian. 11 SD-18. Sample 294. W61/3. J. Ancyrochitina varispinosa. Earliest Givetian. 7 

SD-1. Sample 263. J57c. K. Angochitina daemoni. Late Eifelian. 11 SD-18. Sample 294. H40c. L. Hoegisphaera cf. H. glabra. Late Pragian–early Emsian. 11 SD-17. Sample 289. Q43/ 

3. M. Ramochitina spp. Late Eifelian. 11 SD-18. Sample 294. Q51/1. N. Alpenachitina eisenacki. Late Eifelian. 11 SD-18. Sample 291. Y53/4. 

but is common elsewhere in the Paraná Basin (Grahn et al., 2000; 

Gaugris and Grahn, 2006; Mendlowicz Mauller, 2008). The first 

scattered occurrences of Ancyrochitina parisi (Figs. 7, 9F and G) 

are already in the PoW Su Zone, but the species reaches its optimum 

in the late Emsian. 

6.2. Upper part of Chapada Group unit 2 

The late Emsian–early Eifelian part of the upper Chapada unit 2 

(equivalent to the GS miospore Zone) was sampled from grey, 

micaceous shales at locality 7 SD-6 (Source of Aldeia Velha Stream) 

at the following heights above base: 2.30 m (sample 268), 3.25 m 

(sample 269), and 3.85 m (top of section, sample 266). Characteristic 

miospore species known to range through the upper part of 

Chapada unit 2 have their first appearance in the Paraná Basin in 

the late Emsian (Fig. 6), e.g. Emphanisporites annulatus (Fig. 10K), 

Grandispora protea (Fig. 10L), Acinosporites apiculatus (Fig. 10N), 

Acinosporites lindlarensis Fig. 10O), and Grandispora velata 

(Fig. 10Q). Ancyrochitina parisi (Fig. 9G) is a common chitinozoan 

species, and Ancyrochitina varispinosa (Figs. 9I and J) has its first 

occurrence (Fig. 7). Ancyrochitina morzadeci (Figs. 7, 9E) appears 

in the same stratigraphic position (late Emsian) as in its type locality 

the Lézais section, Gahard, Ille et Vilaine, France (Paris, 1981). 

The Eifelian part of Chapada unit 2 (Per miospore Zone) is 

widely distributed north of Chapada dos Guimarães (Fig. 1B). At 

locality 11 SD-3 (Cachoeira Aspiral, Jamacá Stream) a 7 m thick 

section with levels of grey, bluish, micaceous shale was sampled 

below the waterfall at 1 m (samples 277/278), 4.5 m (sample 

276), and 7 m above the base of the section (sample 279). In the 

lower part of this section occur miospores characteristic for the Eifelian 

and younger strata (Fig. 6), and among these the index species 

Grandispora permulta (Fig. 11D). Other common species 

(Fig. 6) are Acinosporites acanthomammillatus (Fig. 10S) and Acinosporites 

macrospinosus (Fig. 10T). Ancyrochitina varispinosa dominates 

the chitinozoan fauna (Fig. 7). At locality 11 SD-19 (Fazenda 

Bocaina) a 10 m thick section was sampled. Grey, micaceous shales 

were collected 3.5 m (sample 295), 6 m (sample 297), 8 m (sample 

298), and 10 m above the base of the section (sample 296). The biostratigraphy 

suggests that early Eifelian strata are present. Late Eifelian 

was sampled at locality 11 SD-18 (Fazenda Bocaina, 

Cachoeira Segredo) in a 5 m thick section, with the same lithologies 

as the locality mentioned above. At the base (sample 294), 1.80 m 

(sample 297), 3.5 m (sample 291), and 5 m above the base of the 

section (sample 292). Based on the miospores it is difficult to separate 

the early Eifelian from the younger Eifelian in this region, but 

Grandispora gabesensis (Figs. 6 and 11E) has its first occurrence at 

approximately this level. Furthermore, the co-occurrence of Ancyrochitina 

langei (Figs. 9A and B) and Alpenachitina eisenacki 

(Fig. 9N) are characteristic for late Eifelian strata (Fig. 7). The youngest 

Eifelian was sampled at locality 7 SD-7, in an outcrop at the 

first of two waterfalls in Monjolo Stream at Chácara Monjolinho 

(sample 270), and at Chácara Monjolinho (sample 272). The composite 

section is between 16 and 20 m thick. The uppermost Chapada 

unit 2 (earliest Givetian) occurs 1.5 m above the base in an

about 58 m thick section at locality 7SD-1 (Vassoural section, 

Morrinhos/Vassoural Stream). Samples 56.50 and 58.00 m above 

the base of the section were not investigated for spores and chitinozoans, 

and according to Oliveira (1997) they are barren of acritarchs. 

The sampled lithologies are grey, micaceous shales. The 

occurrence of Geminospora lemurata (Fig. 11G), Camarozonotriletes 

concavus (Fig. 11F), and Grandispora macrotuberculata (Fig. 11H) 

indicate the Lli miospore Zone (Fig. 6) and an early Givetian age. 


Fig. 10. Selected miospore species from the Chapada Group at Chapada dos Guimarães. The scale bar represents 20 lm. A. Brochotriletes? foveolatus. Late Pragian–early 

Emsian. 11 SD-2. Sample 274. T22/3. B. Brochotriletes? foveolatus. Late Pragian–early Emsian. 11 SD-2. Sample 274. P20c. C. Dictyotriletes emsiensis. Late Pragian–early Emsian. 

11 SD-17. Sample 288. V28c. D. Perotriletes caperatus. Late Pragian–early Emsian. 7 SD-3. Sample 267. X28/2-4. E. Zonotriletes simplicissimus. Late Pragian–early Emsian. 11 SD- 

17. Sample 290. P24/1. F. Dibolisporites eifeliensis. Late Pragian–early Emsian. 7 SD-3. Sample 267. S31c. G. Synorisporites papillensis. Late Pragian–early Emsian. 11 SD-16. 

Sample 287. L29c. H. Dictyotriletes subgranifer. Late Pragian–early Emsian. 11 SD-17. Sample 288. L11c. I. Rhabdosporites minutus. Late Emsian–early Eifelian. 7 SD-6. Sample 

268. X30c. J. Diatomozonotriletes franklinii. Early Givetian. 7 SD-1. Sample 263. P6/4. K. Emphanisporites annulatus. Late Emsian–early Eifelian. 7 SD-6. Sample 268. K34c. L. 

Grandispora protea. Late Eifelian. 7 SD-7. Sample 272. K14c. M. Grandispora douglastownense. Late Emsian–early Eifelian. 7 SD-6. Sample 269. O29/4. N. Acinosporites apiculatus. 

Late Emsian–early Eifelian. 7 SD-6. Sample 268. G26/3. O. Acinosporites lindlarensis. Early Eifelian. 11 SD-19. Sample 297. W34c. P. Grandispora megaformis. Early Givetian. Sr. 

Cristóvão. Sample 261. M28/3-4. Q. Grandispora velata. Late Emsian–early Eifelian. 7 SD-6. Sample 269. D20/4. R. Samarisporites eximius. Late Eifelian. 7 SD-7. Sample 270. 

O24c. S. Acinosporites acanthomammillatus. Early Eifelian. 11 SD-19. Sample 297. R10c. T. Acinosporites macrospinosus. Late Eifelian. 7 SD-7. Sample 270. P28/2. 

The presence of Ancyrochitina varispinosa (Fig. 9J) suggests the earliest 

Givetian, near the top of Chapada unit 2. 


In a road-cut along the road to sitio Sr. Cristóvão (Fig. 1B) two 

samples were taken. One in an argillaceous layer (sample 260) and 

another in a silty layer (sample 261). The presence of Chelinospora


Fig. 11. Selected miospore species from the Chapada Group at Chapada dos Guimarães. The scale bar represents 20 lm. A. Craspedispora ghadamisensis. Early Givetian. Sr. 

Cristóvão. Sample 260. S32/3. B. Craspedispora paranaensis. Early Givetian. Sr. Cristóvão. Sample 260. B14/3. C. Geminospora punctata. Late Eifelian. 11 SD-18. Sample 294. B25/ 

4. D. Grandispora permulta. Early Eifelian. 11 SD-19. Sample 296. W20c. E. Grandispora gabesensis. Early Givetian. 7 SD-1. Sample 263. P31/1. F. Camarozonotriletes concavus. 

Early Givetian. Sr. Cristóvão. Sample 260. C21/2. G. Geminospora lemurata. Early Givetian. Sr. Cristóvão. Sample 260. W30/1. H. Grandispora macrotuberculata. Early Givetian. 7 

SD-1. Sample 263. G29c. I. Grandispora libyensis. Early Givetian. Sr. Cristóvão. Sample 261. N29/4. J. Chelinospora ligurata. Early Givetian. Sr. Cristóvão. Sample 260. V25/4. K. 

Chelinospora timanica. Early Givetian. Sr. Cristóvão. Sample 260. G32c. L. Grandispora incognita. Early Givetian. Sr. Cristóvão. Sample 261. H20/2. M. Verrucosisporites premnus. 

Early Givetian. Sr. Cristóvão. Sample 260. R27/3-4. N. Verrucosisporites scurrus. Early Givetian. Sr. Cristóvão. Sample 261. Q29/1. O. Archaeozonotriletes variabilis. Early Givetian. 

Sr. Cristóvão. Sample 260. S15/2. P. Apiculiretusispora brandtii. Late Pragian–early Emsian. 7 SD-3. Sample 267. E23/1. Q. Archaeozonotriletes chulus. Late Pragian–early Emsian. 

11 SD-17. Sample 289. P19/1. R. Artemopyra recticosta. Late Pragian–early Emsian. 7 SD-3. Sample 267. E19/4. S. Brochotriletes hudsonii. Late Pragian–early Emsian. 11 SD-17. 

Sample 288. D34c. T. Emphanisporites mcgregorii. Late Eifelian. 7 SD-7. Sample 270. C6/4. 

ligurata (Fig. 11J) in both samples confirms the Lli miospore Zone 

of early Givetian age (Fig. 6). Other characteristic early Givetian 

miospores (Fig. 6) present are e.g. Archaeozonotriletes variabilis 

(Fig. 11O), Grandispora libyensis (Fig. 11I), Verrucosisporites premnus 

(Fig. 11M), and Verrucosisporites scurrus (Fig. 11N). Ancyrochitina 

multibrachiata (Fig. 9D) is a characteristic early Givetian chitinozoan 

that occurs at this locality (Fig. 7). There is no evidence for post early 

Givetian rocks in the Chapada dos Guimarães region (Fig. 1B). 

7. Concluding remarks 

The data presented herein suggest a correlation between the 

Chapada Group units 1–4 (proposed by Evans (1894) and re-validated 

by Melo (1988)), and the classical Devonian formations 

currently in use for the Paraná Basin. The uppermost Pragian 

(PoW Su miospore Zone) is present above Chapada unit 1 (=Furnas 

Fm.), and the possible (no paleontological evidence) Pragian gap

(Mendlowicz Mauller, 2008; Mendlowicz Mauller et al., in press) 

corresponds to the lower part of the PoW (pre-Su) miospore Zone. 

The major part of the lower part of Chapada unit 2 (D2a by Lange 

(1967)) equals the lower part of the Ponta Grossa Fm., as defined 

by Oliveira (1912), and is of late Pragian–early Emsian age (PoW 

Su spore Zone, Ramochitina magnifica and Ancyrochitina pachycerata 

chitinozoan zones). A gap corresponding to middle Emsian strata 

(AB-FD zones) probably results from sea-level variations during 

the Precordilleran orogeny (see Astini, 1996). The upper part of 

Chapada unit 2 ranges from late Emsian (D2b by Lange, 1967) to 

earliest Givetian (GS and Per spore Zones, Ancyrochitina parisi, 

the informal Ancyrochitina varispinosa and Alpenachitina eisenacki 

chitinozoan zones). There is a generally transgressive trend in the 

basin from late Eifelian to earliest Givetian, interrupted by minor 

forced regressions that deposited arenaceous sediments (cf. Ber- 


Fig. 12. Selected miospore and acritarch species from the Chapada Group at Chapada dos Guimarães. The scale bar represents 20 lm. A. Gneudnaspora divellomedia. Late 

Pragian–early Emsian. 7 SD-3. Sample 267. W33/3. B. Granulatisporites granulatus. Late Emsian–early Eifelian. 7 SD-6. Sample 268. M30/1. C. Knoxisporites riondae. Late 

Pragian–early Emsian. 11 SD-17. Sample 289. W33/3. D. Latosporites ovalis. Late Pragian–early Emsian. 11 SD-2. Sample 274. E24/1-2. E. Lophotriletes devonicus. Late Eifelian. 7 

SD-7. Sample 270. G24c. F. Tetrahedraletes medinensis. Late Pragian–early Emsian. 11 SD-2. Sample 273. U25/2-4. G. Verrucosisporites n. sp. sensu Grahn et al. (2005). Late 

Pragian–early Emsian. 11 SD-17. Sample 288. Q34/3. H. Retusotriletes maculatus. Late Pragian–early Emsian. 11 SD-2. Sample 274. S24c. I. Rimosotetras problematica. Late 

Pragian–early Emsian. 11 SD-2. Sample 274. C24c. J. Navifusa bacilla. Early Givetian. Sr. Cristóvão. Sample 260. X33/1. K. Diexallophasis remota. Late Pragian–early Emsian. 11 

SD-2. Sample 273. R12/3-4. L. Navifusa bacilla (short form). Late Pragian–early Emsian. 7 SD-3. Sample 267. R12/3-4. M. Tyligmasoma alargadum. Late Pragian–early Emsian. 11 

SD-17. Sample 288. K37c. N. Bimerga sp. A. Late Pragian–early Emsian. 11 SD-17. Sample 288. M35/2. 

gamaschi and Pereira, 2001). Similar conditions are known from 

the Parnaíba Basin (Grahn et al., 2008). The latest Emsian Tibaji 

Member of the Ponta Grossa Fm. in the Apucarana Sub-basin occurs 

at the same stratigraphic level as the lowermost Chapada unit 

3 in the Alto Garças Sub-basin. In the Apucarana Sub-basin the São 

Domingos shales overly the Tibaji Member and the Ponta Grossa 

Fm. s.s., which is less obvious when the Tibaji Member is missing. 

The sandstones of Chapada unit 3 are a proximal and lateral facies 

to the major part of the shaly-silty rocks of upper Chapada unit 2. 

The Chapada unit 3 is restricted to the eastern margin of the Alto 

Garças Sub-basin, and the contact between Chapada units 2 and 

4 towards the center and western margin of the basin is likewise 

less obvious. An inundation during the earliest Givetian flooded 

Chapada unit 3, and changed the lithologies all over the basin. This 

flooding surface marks the base of Chapada unit 4 of early


Givetian–early late Frasnian age (Lli – Bmu zones, Ramochitina 

stiphrospinata – Lagenochitina avelinoi chitinozoan zones). A minor 

gap is probably present at this level (cf. Grahn et al., 2008). The chitinozoan 

species Ancyrochitina varispinosa can be used as an index 

species for latest Emsian – late early Eifelian strata, from where the 

Alpenachitina eisenacki Zone marks the rest of Chapada unit 2 

(Fig. 8). The interval from the latest Emsian to earliest Givetian 

corresponds to interval D3 of Lange (1967). Hence, units D4a–c 

and D5 of Lange (1967) correspond to Chapada unit 4. 

Acknowledgements 

Yngve Grahn thanks the Conselho Nacional de Desenvolvimento 

Científico e Tecnológico (CNPq, PQ 309751/2007-1), which made 

his work possible through grants, Paula Mendlowicz Mauller 

thanks CAPES (Coordenação de Aperfeiçoamento de Pessoal de 

Nível Superior, BEX 4515/05-6) for grants. Egberto Pereira also 

thanks CNPq (304961/2007-8) and FAPERJ (Fundação de Amparo 

a Pesquisa do Estado do Rio de Janeiro) for grants supporting his 

research. Thanks are also due to the Faculty of Geology at Universidade 

do Estado do Rio de Janeiro (UERJ), Prof. Claudia Sayão Valladares, 

head of the post-graduation program at the Faculty of 

Geology at UERJ for access to the facilities. Prof. Leonardo Borghi 

(UFRJ, Rio de Janeiro) gave access to slides for palynological investigations. 

Prof. emer. Art Boucot (Corvallis, Oregon) checked the 

English, and Prof. Geoffrey Playford (Brisbane, Australia) the English 

in Abstract and Material and methods in a second version. 

Two anonymous reviewers greatly improved the manuscript. Our 

sincere thanks to all. 

Appendix A 

Chitinozoans discussed in text and illustrations. 

Ancyrochitina biconstricta (Lange 1949) 

Ancyrochitina langei Sommer and Boekel 1964 

Ancyrochitina cf. A. maacki Gaugris and Grahn 2006 

Ancyrochitina multibrachiata Grahn and Melo 2004 

Ancyrochitina morzadeci Paris 1981 

Ancyrochitina parisi Volkheimer, Melendi and Salas 1986 

Ancyrochitina varispinosa (Lange 1967) 

Angochitina daemoni Grahn 2000 (in Grahn et al. 2000) 

Hoegisphaera cf. H. glabra Staplin 1961 

Ramochitina magnifica Lange 1967 

Ramochitina spp. 

Miospores discussed in text and illustrations 

Acinosporites acanthomammillatus Richardson 1965 

Acinosporites apiculatus (Streel) Streel 1967 

Acinosporites lindlarensis Riegel 1968 

Acinosporites macrospinosus Richardson 1965 

Apiculiretusispora brandtii Streel 1964 

Archaeozonotriletes chulus (Cramer) Richardson and Lister 

1969 

Archaeozonotriletes variabilis Naumova emend Allen, 1965 

Artemopyra recticosta Breuer et al. 2007 

Brochotriletes? foveolatus Naumova 1953 

Brochotriletes hudsonii (McGregor and Camfield 1976) 

Camarozonotriletes concavus Loboziak and Streel 1989 

Camarozonotriletes sextantii McGregor and Camfield 1976 

Chelinospora ligurata Allen 1965 

Chelinospora timanica (Naumova) Loboziak and Streel 1989 

Chelinospora spp. 

Craspedispora ghadamisensis Loboziak and Streel 1989 

Craspedispora paranaensis Loboziak, Streel and Burjack 1988 

Diatomozonotriletes franklinii McGregor and Camfield 1982 

Dibolisporites eifeliensis (Lanninger) McGregor 1973 

Dictyotriletes emsiensis (Allen) McGregor 1973 

Dictyotriletes subgranifer (Allen) McGregor 1973 

Dyad sp. 

Dyadospora murusdensa Strother and Traverse emend 

Burgess and Richardson 1991 

Emphanisporites annulatus McGregor 1961 

Emphanisporites mcgregorii Cramer 1966 

Geminospora lemurata Balme emend Playford 1983 

Geminospora punctata Owens 1971 

Gneudnaspora divellomedia (Chibrikova) Balme 1988 

Grandispora douglastownense McGregor 1973 

Grandispora gabesensis Loboziak and Streel 1989 

Grandispora incognita (Kedo) McGregor and Camfield 1976 

Grandispora libyensis Moreau-Benoit 1980 

Grandispora macrotuberculata (Arkhangelskaya) McGregor 

1973 

Grandispora megaformis (Richardson) McGregor 1973 

Grandispora permulta (Daemon) Loboziak, Streel and Melo 

1999 

Grandispora protea (Naumova) Moreau-Benoit 1980 

Grandispora velata (Eisenack) Playford 1971 

Granulatisporites granulatus Ibrahim 1933 

Knoxisporites riondae Cramer and Díez 1975 

Lophotriletes devonicus (Naumova ex. Chibrikova) McGregor 

and Camfield 1982 

Latosporites ovalis Breuer et al. 2007 

Perotriletes caperatus (McGregor, 1973) Steemans 1989 

Quadrisporites sp. 

Retusotriletes maculatus McGregor and Camfield 1976 

Rhabdosporites minutus Tiwari and Schaarschmidt 1975 

Rimosotetras problematica Burgess 1991 

Samarisporites eximius (Allen) Loboziak and Streel 1989 

Synorisporites papillensis McGregor 1973 

Tetrahedraletes medinensis Strother and Traverse emend 

Wellman and Richardson 1993 

Verrucosisporites premnus Richardson 1965 

Verrucosisporites scurrus (Naumova) McGregor and Camfield 

1982 

Verrucosisporites n. sp. sensu Grahn et al. 2005 

Zonotriletes simplicissimus Breuer, Al-Ghazi, Al-Ruwali, 

Higgs, Steemans and Wellman 2007 

Acritarchs and freshwater phytoplankton discussed in text and 

illustrations 

Bimerga sp.A sensu Mendlowicz Mauller et al. in press 

Diexallophasis remota (Deunff) emend Playford 1977 

Navifusa bacilla (Deunff) Playford 1977 

Polyedryxium fragosulum Playford 1977 

Schizocystia spp. 

Tyligmasoma alargadum (Cramer) Playford 1977

Appendix B 

List of localities in the Chapada dos Guimarães area = 2 samples a.b = above base of section. 

Code Locality Geographic 

co-ordinates 

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