Flood-dominated fluvio-deltaic system: a new depositional model for the Devonian Cabeças Formation, Parnaíba Basin, Piauí, Brazil

EARTH SCIENCES

Flood-dominated fluvio-deltaic system: a new depositional model for the Devonian Cabeças Formation, Parnaíba Basin, Piauí, Brazil

Luiza Corral M.O. Ponciano^{I, II}; Jorge C. Della Fávera^III

^IDepartamento de Geologia, Instituto de Geociências, Universidade Federal do Rio de Janeiro / UFRJ Av. Athos da Silveira Ramos, 274, CCMN, Cidade Universitária, 21941-916 Rio de Janeiro, RJ, Brasil

^IIDepartamento de Geologia e Paleontologia, Museu Nacional, Universidade Federal do Rio de Janeiro /UFRJ Quinta da Boa Vista s/n , São Cristóvão, 20940-040 Rio de Janeiro, RJ, Brasil

^IIIStarfish Oil & Gas S.A., Av. Rio Branco, 01, 15° andar, sala 1506, 20090-003 Rio de Janeiro, RJ, Brasil

^{Correspondence}

ABSTRACT

The depositional model of the Cabeças Formation is re-evaluated in the context of the Devonian paleogeography of the Parnaíba Basin, and with particular reference to similarities between the formation's facies associations on the eastern border of the basin and the flood-dominated fluvio-deltaic system facies that have been discussed in recent literature. The widespread occurrence and nature of sigmoidal clinoforms (with asymptotic cross-stratification and climbing ripples) of the Cabeças Formation are here considered as strong evidence of flood-influenced depositional settings. Sandy strata of the Passagem Member, in the vicinity of Pimenteiras and Picos (Piauí State), are interpreted as the distal part of fine-grained mouth-bar deposits interbedded with delta-front sandstone lobes showing hummocky cross-stratification. Richly fossiliferous levels, with diverse megainvertebrates and plant cuticles, occur within the delta-front lobes and the distal mouth-bar deposits, reflecting continuation of shallow marine conditions.

Key words: Parnaíba Basin, Devonian, Cabeças Formation, flood-dominated fluvio-deltaic system, delta-front sandstone lobes, mouth-bar deposits, hummocky cross-stratification.

RESUMO

O modelo deposicional da Formação Cabeças é reinterpretado no presente estudo com base no contexto paleogeográfico da Bacia do Parnaíba durante o Devoniano e na similaridade entre as fácies encontradas na Formação Cabeças com as fácies características dos sistemas flúvio-deltaicos dominados por inundações. O tipo das clinoformas sigmoidais (com estratificação cruzada assintótica e laminação cruzada cavalgante), e a sua predominância na Formação Cabeças, são consideradas como as principais evidências da influência de inundações nesta unidade. Depósitos do Membro Passagem, localizados nos arredores das cidades de Pimenteiras e Picos, são interpretados como o componente distal de um tipo de barra de desembocadura com a predominância de arenitos finos a conglomeráticos, intercalados com lobos arenosos tabulares de frente deltaica com estratificação cruzada hummocky. Diversos intervalos fossilíferos, com abundantes macrofósseis de invertebrados e fragmentos vegetais, ocorrem tanto nos lobos de frente deltaica quanto nos depósitos distais de barra de desembocadura, ainda no contexto de um paleoambiente marinho raso.

Palavras-chave: Bacia do Parnaíba, Devoniano, Formação Cabeças, sistema flúvio-deltaico dominado por inundações, lobos de frente deltaica, depósitos de barra de desembocadura, estratificação cruzada hummocky.

INTRODUCTION

The present-day intracratonic Parnaíba Basin covers an area of ca. 600,000 km² in northeastern and north-central Brazil. Devonian lithostratigraphic units of the Parnaíba Basin are, in ascending order, the Itaim, Pimenteira, Cabeças, and lowermost Longá formations (Fig. 1). The Cabeças Formation was proposed by Plummer (1948) for a thick (ca. 100-400 m) sequence of sandstones exposed in the Cabeças locality (known nowadays as Dom Expedito Lopes) on the eastern margin of the Parnaíba Basin (Fig. 1A). Plummer (1948) proposed a three-fold subdivision of the Cabeças sand-stones; from the base upwards, the Passagem, Oeiras and Ipiranga members. Only the first two members are currently accepted, and even these are of problematic validity in terms of their putative lithological discrimination (Beurlen 1965, Mabessone 1994).

The Cabeças Formation consists chiefly of finegrained to pebbly sandstones with asymptotic and hum-mocky cross-stratification, and with subordinate inter-beds of siltstone. The upper part of the formation comprises tillites, striated pavements with faceted, striated and polished clasts and varvelike rhythmites. Miospores and chitinozoans are indicative of an early to latest Famennian age for the uppermost part of Cabeças Formation on the western margin of the Parnaíba Basin (Grahn et al. 2006). On the basin's eastern margin, in outcrops around Pimenteiras and Picos (Fig. 1A), marine megafossil faunas indicate a Givetian age (Melo 1988) for the lower part of the Cabeças Formation (Passagem Member).

The Cabeças Formation provides an example of a sedimentary unit whose origin cannot be explained adequately in accordance with classical depositional models. It displays thick sigmoidal clinoforms with asymptotic cross-stratification (sensu Zavala 2008) and climbing ripples, here considered to represent the main evidence of the significant flooding in its depositional setting. Climbing ripples are related to traction plus fallout processes generated by a turbulent flow with high suspended load. Recently, this structure has been considered a major sedimentary feature in hyperpycnal deposits, as it manifests the steady migration of sedimentary bedforms while sediment supply is maintained and sedimentation rate is significant (Mulder et al. 2003, Zavala et al. 2006).

Della Fávera (J.C. Della Fávera, unpublished data) has proposed that the Cabeças sandstones were deposited under the influence of tidal currents, based on his observations in the south-central Pyrenees Basin, where sand structures with sigmoids are interpreted as tidal deposits. Subsequently, in 1990, Della Fávera linked the origin of the Eocene Roda Formation in the south-central Pyrenees Basin to that of the Cabeças sandstones. The Roda Formation is now interpreted as a flood-generated deposit (Tinterri 2007). Moreover, tidal influence could hardly be envisaged as substantial in epicontinental basins like the Parnaíba Basin. Della Fávera and Medeiros (J.C. Della Fávera and M.A.M. Medeiros, unpublished data) have interpreted a set of sigmoidal clinoforms in the Cabeças Formation as mega-climbing ripples caused by catastrophic floods.

Episodic sedimentation has been reappraised considerably in recent years, following the intensive discussions of the early 1980s (as detailed by Della Fávera 1984), when the gradualistic character of sedimentation was considered to have prevailed.

The unusual nature of this kind of event in terms of the human timeframe should be considered in the application of modern settings studies, because these may be unsuited or not necessarily applicable to the interpretation of some paleoenvironments, such as that considered here.

Ancient flood-dominated fluvio-deltaic systems cannot be described and interpreted according to the current sedimentological models for fluvial and deltaic sedimentation, because such models are usually derived from modern depositional environments dominated by "normal" fluvial and marine processes (see extensive discussion in Mutti et al. 1996). The modern analogs of these flood-dominated systems could be the small and medium-sized mountainous rivers described by Milliman and Syvitski (1992) and the "dirty rivers" of Mulder and Syvitski (1995), which can generate frequent hyperpycnal flows during a year (Mutti et al. 2000).

Hyperpycnal flows result from a sediment-laden fluvial discharge entering a standing body of water, mainly during a flood (Mulder and Syvitski 1995). A hyperpycnal system could be defined as the subaqueous extension of the fluvial system, delivering a huge volume of sediment into a basin, with facies and facies associations that depart significantly from classical models. Consequently, their deposits and depositional features could resemble certain characteristics common to both fluvial and turbidite deposits (Zavala et al. 2006).

Although hyperpycnal flows are evidently common at contemporary river mouths (Mulder and Syvitski 1995, Mulder et al. 2003), their manifestation in ancient deposits has been poorly documented (Zavala et al. 2006).

A classic example of cataclysmic floods is the Channeled Scablands of Washington, U.S.A., which inundated the Columbia River basin during the Pleistocene. In 1923, J. Harlen Bretz envisaged huge floods to explain the immense ripples with wavelengths up to 100 m and amplitudes of 9 m, fluvial bars 120 m high, erratic boulders, and other structures found in the Channeled Scablands (Della Fávera 2001). In complying with the Lyellian concept of gradualism, the scientific community of that time rejected Bretz's model, which was not fully recognized until 1965.

FLOOD-DOMINATED FLUVIO-DELTAIC SYSTEMS: FACIES AND PROCESSES

It is appropriate to reinterpret the sandstones of the Cabeças Formation based on recent published data on fluvio-deltaic sedimentation pertaining to flood-dominated depositional systems.

Mutti et al. (1996) introduced a depositional model for ancient flood-dominated fluvio-deltaic systems, typical of tectonically active basins, but applicable also to interior cratonic basins such as the Parnaíba Basin. These flood-dominated fluvio-deltaic systems can be viewed as developing in elevated catchment basins and short and high gradient transfer zones. In such settings, floods generate sediment-water mixtures that enter sea-water as density-driven underflows (hyperpycnal flows).

Flood-dominated fluvio-deltaic systems produce sedimentary units with distinct vertical and longitudinal grading formed during a discrete flood event. These elementary flood-units may diverge considerably from each other due to many local controlling factors such as volume, sediment concentration, duration of individual flood events, type of process, type of sediment involved and depositional setting (Mutti et al. 2000).

Therefore, individual flood-units may vary from, on the one hand, crudely graded, small and lenticular coarse-grained bars produced by the sudden deceleration of low-volume and short-duration flash floods to, on the other hand, graded and comparatively well-sorted and laterally extensive sandstone beds deposited by long-lived and relatively confined hyperpycnal flows (Mutti et al. 2000).

In flood-dominated fluvio-deltaic systems, climatic and minor eustatic variations, generated by orbitally forced cyclicity within the Milankovitch range, are considered the primary factor in controlling sedimentation; see Milliman and Syvitski (1992) and Mutti et al. (1996, 2000) for a detailed discussion. Catastrophic floods can originate only if large amounts of water are available in drainage basins over short time intervals; these could result from breaches of natural dams (including failure of ice dams that blocked large drainage systems), proglacial-lake overflows, subglacial volcanic eruptions, landslide-dam failures, lake-basin overflows and ice-jam floods. Large floods resulting from meteorological conditions and atmospheric water sources played a minor role at least in Quaternary flooding episodes (O'Connor and Costa 2004).

Although the incidence of floods has changed through time, the relative proportions of those caused by breaches of natural dams and those that resulted from meteorological phenomena would not be expected to vary appreciably through geologic time. During the so-called "flood epochs", climate and topography are jointly responsible for producing unusually high frequencies of large floods, especially in times of advancing continental ice sheets and rapid changes in sea level (O'Connor and Costa 2004).

According to Mutti (1992) and Mutti et al. (2000), the most common and distinctive depositional unit of a flood-dominated fluvio-deltaic system consists of sharp-based and parallel-sided graded sandstone beds characterized by hummocky cross-stratification (HCS). These sheet-like sandstone beds typically form packets 3-15 m thick, with muddier interbeds that may be richly fossil-iferous and bioturbated. These sediments, which are notable for their lateral continuity and their internal cyclic stacking pattern, constitute the typical delta-front facies association of a flood-dominated system.

First recognized by Goldring and Bridges (1973), these deposits were initially named "sublittoral sheet sandstones" and variously attributed to storms, tsunamis, floods, tides, rip and turbidity currents. Mutti et al. (1996) termed the deposits "shelfal sandstone lobes", which were redefined by Mutti et al. (2000) as "flood-generated delta-front sandstone lobes". Vertical and lateral stratigraphic relationships indicate that delta-front sandstone lobes pass basinward into mudstone-dominated prodelta facies, and that their landward equivalents are represented by very distinctive mouth-bar deposits (Fig. 2A).

Mouth-bar deposits display considerable variation in terms of geometry and facies types, essentially recording locally prevailing conditions. Depending on the kind of flow, different types of mouth-bars could develop, such as the fine-grained or the coarse-grained mouth bars, ranging from medium to fine sand or boulder and small pebble sized clasts to fine sand, respectively (Mutti et al. 2000).

Facies distribution patterns are thus mainly controlled by the volume of sand trapped at a river mouth and whether sufficient can be liberated to form turbulent hyperpycnal flows. The latter can then move farther basinward, depending on flow efficiency, and ultimately deposit their sand load as delta-front lobes.

Mouth-bar deposits of flood-dominated systems form very distinctive meter-thick progradational units, and their slope varies as a function of the water depth seaward of the river mouth. Even though displaying various types of bedding geometry and internal depositional structures, including plane-bed laminae and climbing ripples, mouth-bar deposits ost frequently show a typical sigmoidal clinoform bearing asymptotic cross-stratification. This developed at different physical scales as a function of the magnitude and duration of individual flows (Mutti et al. 2000, Zavala et al. 2006).

First described by Mutti et al. (1996), sigmoidal clinoforms produced by flood-generated flows are typically expressed by sigmoidal sets of cross-laminae which markedly thin and flatten downcurrent and are truncated upcurrent by a flat or slightly convex-upward erosional surface, produced by the bypassing of a turbulent flow. Sigmoidal clinoforms are readily distinguishable from those of tidal origin, inasmuch as the distinctive features of tide-dominated facies, like mud drapes and current reversal, are unrepresented in flood-dominated sediments.

The presence of hummocky cross-stratification (HCS) may also cause uncertainties in the interpretation of flood deposits. Flood-generated delta-front sandstone lobes have usually been mistakenly identified as storm-dominated nearshore and shelfal deposits, mainly because of the pervasiveness of the HCS. However, combined-flow conditions are inherent in the dynamics of flood-generated flows, particularly in those flows entering seawater as hyperpycnal flows. Hence the interpretation of the HCS origin has changed from the classic storm-layer theory of Harms et al. (1975) to that involving turbidites generated by a hyperpycnal flow (Mutti et al. 1996). Hyperpycnal flows behave essentially as shallow-water turbidity currents, and, except for the occurrence of HCS, locally abundant fossil debris and bioturbation, these flows produce facies tracts very similar to those generated by turbidity currents in a deep-water environment (Mutti et al. 2007).

Basinward of mouth-bar and delta-front regions, where the bulk of sand is trapped, flood-dominated fluvio-deltaic systems grade into prodeltaic mudstones with interbedded fine-grained sandstones. The delta-front is considered the terminal depositional zone of these systems, with facies deposited by hypopycnal flows (buoyant plumes) and low-density hyperpycnal flows (Mutti et al. 2003). Hypopycnal flows can form either during normal river flooding or by the separation and lift-off of more dilute flows from an underlying hyperpycnal flow (Mutti et al. 2000).

Zavala et al. (2008) interpreted the deposits of low-density hyperpycnal flows as lofting rhythmites, where rhythmic sand-silt couplets containing abundant plant material are interbedded with massive to laminated tabular sandstone lobes (the delta-front sandstone lobes sensu Mutti etal. 2000). Lofting rhythmites accumulate from a lofting plume, which characterizes hyperpycnal inflows in marine environments. When the flow gradually deposits part of its suspended load, the freshwater current will ascend from the substrate through buoyancy reversal, forming lofting plumes charged with finegrained sediments, plant debris and micas.

Alternatively, the interbedded sandstone lobes result from traction plus fallout processes, and often show vertical facies recurrences, which are interpreted as evidence of deposition from flow fluctuations in long-lived and quasi-steady hyperpycnal flows. In contradistinction to classic models of turbidity sedimentation, coarsegrained materials are not transported at the flow head, but are transported at the flow base as bedload (Zavala 2008).

The facies tract proposed by Zavala (2008) comprises three main genetically related facies groups, termed B, S and L. These correspond to bedload, suspended load and lofting transport processes, respectively (Fig. 2B).

Facies B (bedload) is the coarsest grained and relates to shear and frictional drag forces induced by the overpassing long-lived turbulent flow. Three main subcategories are identified, termed B1 (massive or crude bedding conglomerates), B2 (pebbly sandstones with asymptotic cross-stratification, with the subdivision B2s, characterized by fine to coarse grained sandstones with asymptotic cross-stratification and clay chips) and B3 (pebbly sandstones with diffuse planar lamination and aligned clasts). Facies S is essentially fine grained, and reflects the gravitational collapse of sand-size materials transported as suspended load. Four S facies sub-types are recognized: S1 (massive sandstones), S2 (parallellaminated sandstones, with the subdivision S2h, characterized by fine grained sandstones with isotropic HCS), S3 (sandstones with climbing ripples) and S4 (massive siltstones and mudstones). Facies L (lofting) is a manifestation of the buoyancy reversal of the hyperpycnal flow. Finest materials suspended in the flow (very fine grained sand, silt, plant debris and micas) are lifted from the substrate and are re-deposited as laterally extensive silt/sand couplets (Zavala 2008, Zavala et al. 2008).

A NEW DEPOSITIONAL MODEL FOR THE CABEÇAS FORMATION

The depositional paradigm of the Cabeças Formation is re-evaluated here with reference to the Devonian paleo-geography of the Panaíba Basin, and to similarities between the formation's facies associations on the eastern side of the basin and the flood-dominated fluvio-deltaic system facies described in recent literature.

The widespread occurrence and nature of sigmoidal clinoforms in the Cabeças Formation (i.e., sandstones, several meters thick, bearing asymptotic cross-stratification and climbing ripples, without the distinctive features of tide-dominated facies, like mud drapes and current reversal) are here considered to constitute persuasive evidence of flood-influenced depositional settings.

The set of sigmoidal clinoforms attributed to mega-climbing ripples from some outcrops of the Cabeças Formation (e.g., BR-343 Highway, km 168.5, near Piracuruca, Piauí) signifies a water depth of 50 m during flooding, due to the ripple geometry with 10-15 m ripple-spacing and height of 2 m (Della Fávera and Medeiros 2007).

The distributional patterns among the Cabeças Formation's sigmoidal clinoforms bearing asymptotic cross-stratification (the mouth-bar deposits) and the interbed-ded hummocky cross-stratified tabular sandstones (the delta-front lobes) reflect the density and transformations experienced by these turbidite-like flows.

High-density turbulent flows, in which the unidirectional component of the hyperpycnal flow predominates, are responsible for the deposition of the flood-generated mouth-bars and for the sigmoidal clinoform's genesis. Basinward, the delta-front lobes with HCS (where the oscillatory component of the hyperpycnal flow prevails) would result from low-density turbulent flows bypassing the high-density deposits and carrying their suspended load to more distal regions. Finally, when the flow gradually deposits part of its suspended load, the low-density current with freshwater will ascend from the substrate, forming lofting plumes charged with fine-grained sediments, plant debris and micas, and producing rhythmic sand-silt couplets with abundant plant material (i.e., constituting facies L of Zavala et al. 2008).

As a result, the Cabeças Formation's delta-front sandstone lobes with HCS (corresponding to facies S2h of Zavala 2008, see Fig. 2B) would onlap the sandstones bearing asymptotic cross-stratification (comparable to facies B2s of Zavala 2008) and reach deeper regions. Depending on flow efficiency, these delta-front lobes could remain attached (in the case of less efficient flows) or be detached (efficient flows) from the proximal mouth-bar deposits (Mutti et al. 2000, Zavala et al. 2000).

In the Passagem Member, the fine-grained sandstone lobes with HCS contain an allochthonous assemblage with diverse and plentiful megainvertebrates (Fig. 3B) consisting mostly of terebratulid brachiopods and tentaculitids, together with rare bivalves and trilobites.

Mouth-bar deposits of the Cabeças Formation (Passagem Member) are exposed in the eastern border of the Parnaíba Basin: notably, in the Oiti region (municipality of Pimenteiras, Piauí) and in the vicinity of Picos (Fig. 4). These deposits are interpreted herein as the distal component of a fine-grained mouth-bar within a flood-dominated fluvio-deltaic system. Vertical sections of these outcrops in the Pimenteiras and Picos areas are composed of two portions.

The downstream section, the mouth-bar slope, comprises medium- to fine-grained sandstones with plane bedding and climbing ripple cross-lamination interbed-ded with massive to laminated siltstones at its base and current ripples at its top (Fig. 4A).

The upstream portion is characterized by typical asymptotic cross-stratification of pebbly to fine-grained sandstones (Fig. 4B). These mouth-bar deposits show erosional features such as mudstone clasts and an abundant para-autochthonous megainvertebrate assemblage (Fig. 3A). The megafossils consist chiefly of Pleurochonetes comstocki (Rathbun, 1874), associated with spiriferid, terebratulid and lingulid brachiopods, bivalves, tentaculitids, trilobites, crinoids and gastropods.

Lofting related facies (Zavala et al. 2008) also occur, as rhythmic sand-silt couplets with abundant plant debris (Spongiophyton) and mica (Fig. 3C), indicating the proximity of a fluvial source (Martinsen 1990). These rhythmites are interbedded with massive to laminated tabular sandstone lobes (the delta-front sandstone lobes) and distal mouth-bar deposits.

Paleogeographically, the Parnaíba Basin was situated during Devonian time at Lat. 40°-60°S (according to Isaacson et al. 2008), experiencing intermittent glacial conditions during its first sedimentary cycle (Late Ordovician through Early Mississippian).

A glacial origin was initially proposed by Moura (1938) for Devonian diamictites penetrated by wells in the Tapajós River area of the Amazonas Basin, and Kegel (1953) was the first to interpret the diamictite as a tillite, based on the texture of cores recovered from Petrobras CL-1-MA well in the Parnaíba Basin.

Furthermore, glacial and periglacial conditions have been inferred for the upper Cabeças Formation by Carozzi et al. (1975), Caputo (1985), Caputo and Crowell (1985), Loboziak et al. (2000), Streel et al. (2000), Caputo et al. (2008) and Isaacson et al. (2008). Caputo (1985) proposed that during the late Frasnian-early Famennian the glaciers were restricted to upland regions and that during subsequent Famennian time they advanced over the Parnaíba, Amazonas and Solimões basins.

In addition to the latest Famennian glaciation evidenced by the upper Cabeças Formation, Caputo et al. (2008) speculated about the possibility of an earlier glaciation at the Frasnian-Famennian boundary. They considered that the regressive sandy and conglomeratic beds within the Pimenteira Formation could signify a small-scale glaciation. However, the erosional consequences of the major late Famennian glaciation would very likely have acted to remove the evidence of this postulated earlier Devonian glaciation.

The glacial conditions of the Late Devonian (Frasnian-Famennian) could well have been preceded by small-scale upland glaciation during the late Middle Devonian (Givetian). This could at times have generated floods in the Parnaíba Basin, by breaching of natural dams or meteorological circumstances. The extremely effective flows triggered by such flood events would enter seawater as hyperpycnal flows, thus generating the flood-dominated fluvio-deltaic system facies documented in the previous section.

CONCLUDING REMARKS

Ongoing climate changes are at the forefront of current scientific and public debate (Eyles 2008, O'Connor and Costa 2004). Turning to the geological past, the widespread interest in cyclic climatic fluctuations and ancient episodic events, such as catastrophic floods, emphasizes the vital necessity of obtaining much more detailed information concerning the origin of these events and their resultant facies associations.

The fluvio-deltaic systemic models proposed by Mutti et al. (1996, 2000, 2003, 2007), Zavala et al. (2000, 2006, 2008) and Zavala (2008) can be applied in this new hypothesis about the deposition of the Cabeças Formation along the eastern border of the Parnaíba Basin, thus facilitating a reassessment of its paleoenvironmental setting, including the influence of floods. The deposits of this fluvio-deltaic system dominated by rivers in flood are here considered as having been generated by hyperpycnal flows operating as shallow-water turbidity currents.

The shallow marine faunas of the Cabeças Formation are preserved in the distal mouth-bar deposits and proximal delta-front lobes, in particular the facies of the Passagem Member near Pimenteiras and Picos. The hyperpycnal flows triggered by fluvial floods caused a mixing of megainvertebrate skeletal remains from different shallow-water communities; these latter can be distinguished according to the taphonomic signatures represented in the fossil assemblages. Hence, these data provide an objective basis for taphonomic and paleo-ecologic analyses of the Cabeças Formation's Devonian megafaunas.

In a wider context, the model proposed by Mutti et al. (1996, 2000, 2003, 2007) is also applicable to taphonomic analysis of diverse megafossils (Fürsich et al. 2005, Astibia et al. 2005, Dominici and Kowalke 2007). Furthermore, the model could assist in paleo-environmental reconstructions (Torricelli et al. 2006) and in reassessment of depositional settings in other Brazilian epicontinental basins, including the Paraná Basin (Vesely 2007).

In contrast to the considerable knowledge that has accrued concerning the latest Famennian glaciation (Caputo et al. 2008), the nature, extent and precise dating of other possible Devonian glaciations in the Parnaíba Basin, and their effects on the dynamics of depositional systems, clearly warrant further investigation.

ACKNOWLEDGMENTS

José Henrique Gonçalves de Melo (Petrobras/Cenpes) and Vera Maria Medina da Fonseca (Museu Nacional/ UFRJ) are thanked for their encouragement and constructive criticisms regarding this paper. Carlos Emanoel de Souza Cruz (Petrobras/E&P), Geoffrey Playford (The University of Queensland), Mario Vicente Caputo (UFPA) and two anonymous peer reviewers provided helpful comments that resulted in improvements to the manuscript. The authors are very grateful to Geoffrey Playford and Fabiana Rodrigues Costa (Museu Nacional/UFRJ) for linguistic revision of the text. Funding was provided by the Fundação Carlos Chagas Filho de Amparo à Pesquisa do Rio de Janeiro (FAPERJ, #E-26/110.284/2008). Luiza Ponciano also acknowledges the Ph.D. fellowship awarded by the Conselho Nacional de Desenvolvimento Científico e Tecnológico (CNPq).

Manuscript received on December 3, 2008; accepted for publication on August 6, 2009; presented by ALEXANDERW.A. KELLNER

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Publication Dates

• Publication in this collection
  16 Nov 2009
• Date of issue
  Dec 2009

History

• Accepted
  06 Aug 2009
• Received
  03 Dec 2008