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Tectonic Cycles and Sedimentary Sequences in the Brazilian Intracratonic Basins

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Tectonic Cycles and Sedimentary Sequences in the Brazilian Intracratonic Basins Tectonic cycles and sedimentary sequences in the Brazilian intracratonic basins PAULO CESAR SOARES ] Departamento de Geocièncias, Universidade Estadual Paulista, Rio Claro, Sào Paulo, PAULO MILTON BARBOSA LAND IM J Brazil VICENTE JOSE FULFARO Instituto de Geocièncias, Universidade de Sào Paulo, Sào Paulo, Brazil ABSTRACT by widespread continental sedimentation nature, and the preserved thickness of suc- under platform conditions. The second cessive stratigraphic units at basin depocen- The geometry and petrology of sedimen- reactivation cycle was responsible for ac- ters. These criteria permit a semiquantita- tary rocks preserved in the three intra- cumulation of the Zeta sequence (Ceno- tive evaluation of oscillatory movements of cratonic basins of the Brazilian craton zoic), which was characterized by thin re- the Brazilian craton. Figures 3, 4, and 5 il- (Paraná, Parnaiba, and Amazon) indicate sidual deposits on an extensive Tertiary lustrate the nature of the stratigraphic rec- the history and character of vertical move- peneplain and by accumulations in Quater- ord, amount of subsidence, and rate of ments of the cratonic area. Cyclic succes- nary basins, the latter of minor importance subsidence for the three intracratonic ba- sions of erosional and depositional events except where adjacent to the uplifted east- sins. The age assignments for each strati- are synchronous on the Brazilian craton ern continental margin. graphic unit are according to biostrati- and are correlated with cratons of other graphic works of Lange (1967a, 1967b), continents. The principal evolutionary INTRODUCTION Daemon and Quadros (1970), and Daemon stages of the Brazilian craton are inter- and Contreiras (1971); absolute ages are preted as tectonic-sedimentary cycles, each In this paper the geological evolution of from Kulp (1961) and Harland and others represented by a stratigraphic record iden- the Brazilian craton is investigated in terms (1964). tified as a sequence, and each distinguished of the major sedimentary and erosional by its own special characteristics. events of Phanerozoic time. Vertical move- STAGES AND CYCLES OF Cambrian-Ordovician sedimentary rocks, ments, particularly those of cyclical charac- TECTONIC-SEDIMENTARY representing deposition in paraplatform ter, have been determined from amount of EVOLUTION OF BRAZILIAN basins during a transitional stage at the subsidence and rates of accumulation of INTRACRATONIC BASINS close of the Brazilian orogenic cycle, are as- sediments in the three intracratonic basins signed to the Alpha sequence. The Beta (Paraná, Parnaiba, and Amazon) of the The lithological associations and the un- (Ordovician and Silurian), Gamma (Devon- Brazilian craton (Fig. 1). conformities, mentioned above, in the three ian-early Carboniferous), and Delta (late The question of cyclical evolution of interior basins document the variation of Carboniferous-Late Permian sequences) cratonic areas of North America and the the depositional interface in relation to base and the Delta-A subsequence (Middle Russian platform have been considered by level through Phanerozoic time. Triassic-Jurassic), corresponding to Sloss (1963,1964,1972) and by Ronov and Episodes of subsidence in interior basins geotectonic cycles of the cratonic stabiliza- others (1969), respectively. Sloss (1963) are characterized by an initial phase of con- tion stage, indicate accumulation in large proposed that major stratigraphic succes- tinental sedimentation; the depositional in- subsiding basins. The succession of facies in sions separated by interregional uncon- terface is below base level, but the rate of each of these sequences documents cyclical formities were identified as stratigraphic se- sediment supply compensates for subsi- changes in the ratio of sediment supply to quences recognized as the preserved record dence. With continuing subsidence at an ac- subsidence. Marine transgression and basin of cratonic subsidence and accompanying celerated rate, the depositional interface subsidence increased progressively through sedimentation followed by an episode of passes below sea level to initiate marine the Devonian phase of the Gamma se- broad uplift and erosion. Wheeler (1958) sedimentation. The greater the ratio of quence and declined thereafter, in a pattern expressed a similar concept in his definition subsidence to sediment supply, the deeper similar to that of the North American cra- of depositional holosomes. Gomes (1968), the depositional interface becomes, and vice ton and the Russian platform. The fre- Almeida (1969), Ghignone (1972), and Ful- versa. Thus, regression, continental sed- quency of stratigraphic discordances in the faro and Landim (1976) studied deposi- imentation, deltaic progradation, or the ap- three lower sequences suggests a higher de- tional cycles in Brazilian intracratonic ba- pearance of areas of nondeposition or ero- gree of cratonic upwarping, progressively sins, subdividing the Phanerozoic succes- sion define events characterized by subsi- diminishing to a stage of maximum stabili- sion into units designated as holostromes, dence rates that are less than the rate of sed- zation during Delta-A deposition, perhaps sequences, or stages (Fig. 2) with iment accumulation, or by tectonic uplift. related to conditions immediately prior to similarities and differences that are dis- Figure 3 represents the geomorphological rupture of the Gondwana plate. cussed below. position of the depositional interface under Breakup of the Gondwana plate, accom- To evaluate the variations of cratonic these conditions (it does not necessarily ex- panied by volcanism and remobilization of tectonism we have used the following data press only oscillatory tectonic motions). In cratonic areas, initiated the reactivation and criteria: volume and thickness of sedi- constructing the curves, consideration has stage during which two geotectonic cycles ment per time unit, area of preserved sedi- been given to the entire history of each ba- are recognized. The first, represented by the ment representing successive stratigraphic sin, including both aggradational and de- Epsilon sequence (Cretaceous), began with units, episodes of transgression and regres- gradational regimes. The nature of ob- local subsidence in isolated basins, followed sion, stratigraphic unconformities and their served stratigraphic discontinuities (from Geological Society of America Bulletin, v. 89, p. 181-191, 9 figs., February 1978, Doc. no. 80203. 181 Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/89/2/181/3444122/i0016-7606-89-2-181.pdf by guest on 26 September 2021 182 SO ARES AND OTHERS NORTH AMERICA SOUTH AMERICA FULFARO SLOSS GOMES ALMEIDA GHIGNONE ndLANDIM SOARES et al. 1963 1968 1969 1972 1976 THIS PAPER 21 2T T Iff 5 2: Y 4 K ZUNI m E 12 J 3 I P m n ni ABSAROKA : 2 u C —L GAMMft' I lb D n n S 10 0 i € I W- -E AM PB PR Figure 2. Subdivision of Brazilian Phanerozoic stratigraphie succession into sequences by several authors, compared to North American sequences of Sloss (1963). Figure 1. Location of the three major Brazilian intracratonic basins and quantity of material accumulated and their basements. 1, Sedimentary cover from Precambrian to Holocene; 2, preserved in a chronostratigraphic unit is middle Paleozoic cratonic areas (structural trends); 3, late Precambrian the record of tectonic movement in the ba- cratonic areas: I, Amazon; II, Sao Francisco; 4, approximate boundaries of sin, whereas the kind of material supplied intracratonic basins; 5, approximate boundaries of cratonic areas in late Precambrian time. to the basin is determined by tectonic activ- ity in the source area. diastem to angular unconformity) and of graphic sequences represent the sediments Examination of the data given in Figures the depositional environment (from conti- deposited in each cycle when basinal areas 3, 4, and 5 leads to the following conclu- nental to abyssal marine) are interpreted were below depositional base level. Figure 4 sions: (1) The preserved stratigraphie rec- from the sedimentary record in order to shows the amount of subsidence at the de- ord of the Brazilian craton can be divided identify the amount of vertical motion pocenter of each basin in each of the into six sequences — Alpha (Cambrian- characteristic of each basinal area during tectonic-sedimentary cycles. The curves Early Ordovician), Beta (Late Ordovi- each cycle. show cumulative maximum thicknesses as a cian-Silurian), Gamma (Early Devo- Episodes of broad cratonic uplift corre- function of geologic time for each cycle; the nian-Early Carboniferous), Delta (late spond to times of clastic supply to basin slopes of the curves are functions of subsi- Carboniferous-Late Permian or Early sedimentation and to times of erosion of dence rates. Subsidence ratios, shown in Triassic), Epsilon (Late Jurassic-Late Cre- previously accumulated deposits. The na- Figure 5, represent thicknesses per unit time taceous), and Zeta (Tertiry). Strata dated as ture of uplift at depositional sites is esti- for successive stratigraphic units at basin Middle Triassic to Late Jurassic are here mated by the angularity of the unconfor- depocenters. Subsidence of broad regions is provisionally identified as subsequence mity separating adjacent sequences. Local considered the fundamental control of the Delta-A (Piramboia, Botucatu, and Sam- and regional disconformities and angular cumulative sedimentation and preservation baiba Formations). (2) The six sequences unconformities were evaluated to suggest
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