Geology Reference
In-Depth Information
PARANA BASIN (PB)
CONGO BASIN (CB)
South America-Africa
break-up (80-130 Ma)
south
south-central
south-central
north
C S fS mS cS Gr P
CSfSmScSGrP
C S fS mS cS Gr P
C S fS mS cS Gr P
CSfSmScSGrP
0 m
D1
Bauru Gp.
Kalahari Gp.
G1
D2
Fluvial
Stanleyville
Tidal
Lacustrine
D3
Serra Geral Fm.
G2
Bokungu Gp.
Dekese Fm.
500 m
Flood Basalts (132 Ma)
D4
Aeolian
Loia Gp.
G3
G4
G5
SW
D5
D6
Aeolian
Banalia
SW
NE
D7
Botucatu Fm.
Guara Fm.
Aeolian
1000 m
S
Anoxic Lake
Santa Maria Fm.
Sanga do Cabral
Playa
Corumbatai Fm.
Lukuga Gp.
D8
Anoxic Lake
Aeolian
Piramboia Fm.
G6
W
1500 m
Rio do Rastro Fm.
Teresina Fm.
Serra Alta Fm.
Irati Fm.
Palermo Fm.
Delta
Alolo Fm.
Aruwimi
D9
Galamboge
N
Marine
2000 m
G7
Itarare Gp.
Rio Bonito Fm.
Peri-glacial
turbidites and
diamictites
Lokoma
2500 m
Ituri Gp.
Ponta Grossa Fm.
G8
Parana Gp.
Marine
shelf
Furnas Fm.
SW
3000 m
G9
Vila Maria Fm.
Rio Ivai Gp.
Iapo Fm.
Alto Garcas
Inkisi Gp.
G10
Neoproterozoic (Pan African)
carbonate basement
3500 m
Phanerozoic Stratigraphy:
G11
Permian-Triassic
Carboniferous-Permian
Devonian
Cenozoic
Middle-Upper Cretaceous
Lower Cretaceous
Upper Jurassic-Lower Cretaceous
4000 m
Ordovician-Silurian
4500 m
Upper Neoproterozoic-lower Paleozoic
Upper Jurassic
G12
Fig. 13.6
New regional correlations between Phanerozoic sequences of the CB of central Africa and the PB of southeastern Brazil, based on core/
well data and field investigations (e.g.
'
Coluna White
'
, La Serra do Rio Rastro, Brazil)
benchmark at Witmarsum (Fig.
13.9
) that indicates N-S
advances and retreats of the Gondwana ice caps. The
overlying Carboniferous Itarar´ Group (maximum 1,500 m
thick) includes glacio-marine turbidites, diamictites and
rhythmites, forming five fining upward peri-glacial
sequences (Vesely and Assine
2006
; Vesely
2007
) that can
confidently be correlated with the Dwyka Group of southern
Africa (Milani and de Wit
2008
) and now, herewith, also
correlated with the Lower Lukuga Group in the CB
(Fig.
13.6
). In detail, these widely separated sequences,
however, show important variations in thickness, lithology
and sediment provenances
Lukuga diamictites date predominantly at 1.8-2.1 Ga, likely
derived from large mid-Paleoproterozoic (Eburnian) sources
in Uganda and Tanzania, thus suggesting a major paleo-
relief in east Africa (e.g. the Tanzanian Highland;
Fig.
13.10
). In contrast, in southern Africa the Dwyka
Group reaches a maximum thickness of 800 m in the south-
ern CKB (Catuneanu et al.
2005
; Johnson et al.
2006
) and
thins northward to about 250 m thick in the central Kalahari
(Smith
1984
). Ice-flow directions suggest a highland to the
north and to the northeast, e.g. the
of
du Toit (
1954
). U-Pb detrital zircon dates from the Dwyka
tillites (Craddock and Thomas
2011
) have two major peaks:
at 1100 Ma and 550 Ma, sourced from late Mesoproterozoic
(Kibaran) and late Neoproterozoic (Pan African) age-
sequences of the Kalahari and Central African Shields. U-
Pb detrital zircons results from tillites in southern South
America (Craddock
2011
) yield a dominant peak at
400-600 Ma that suggest important Brasiliano-Pan African
contributions to the PB, such as for example from the Don
'
Cargonian Highland
'
that
likely reflect
regional
differences in paleo-environments.
In central Africa, the Carboniferous-Permian Lukuga
Group is best preserved (300-600 m thick) in west-facing
paleo-glacial valleys along the eastern margin of the CB
(Boutakoff
1948
; Cahen and Lepersonne
1978
), and links
to depot-centers up to 1,400 m thick in the center of the basin
(Linol
2013
; Chap.
7
, this Topic). Detrital zircons from the
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