HoloceneCoastalEvolutionoftheRioAçuArea(RioGrandedoNorte...
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Journal of Coastal Research SI 39 141 - 145 ICS 2004 (Proceedings) Brazil ISSN 0749-0208 SCHWARZER, K.; STATTEGGER, K.; VITAL, H. and BECKER, M., 2006. Holocene coastal evolution of the Rio Açu area (Rio Grande do Norte, Brazil). Journal of Coastal Research, SI 39 (Proceedings of the 8th International Coastal Symposium), 141 - 145. Itajaí, SC, Brazil, ISSN 0749-0208. The coastal development of the Rio Açu area (Rio Grande do Norte, Brazil) and the response of the river mouth to the Holocene sea level rise were reconstructed from seismostratigraphy. A sharply defined stratigraphic boundary between the Pleistocene and Holocene deposits was recognised. The seismic data reveal that, during sea level lowstand, a valley up to 9 km wide was cut into the Pleistocene deposits of the shelf platform. This valley extends perpendicular to the shoreline and is preserved in the recent morphology. It narrows at ~20 km offshore to a 1km wide channel, which then widens to its former size a few hundred meters further offshore. Several incised valleys and cut and fill structures up to 2500 m wide and 12 m deep were observed in the Pleistocene deposits. These extend to 45 m below sea level, and indicate that the ancient Rio Açu meandered. A sediment sequence with sigmoidal structures increases in thickness offshore to 12 m, is composed of reworked material, and is interpreted as an embankment. A tilted block composed of more solid material was identified over a distance of at least 800 m. Holocene sediments thin out above this block, indicating postglacial neotectonics in the area. ADDITIONAL INDEX WORDS: NE Brazil, holocene sea level rise, seismostratigraphy, neotectonics. ABSTRACT Holocene Coastal Evolution of the Rio Açu Area (Rio Grande do Norte, Brazil) K. Schwarzer †; K. Stattegger †;, H. Vital ‡ and M. Becker † †Institute of Geosciences Kiel University, 24118 Kiel, Germany [email protected] [email protected] INTRODUCTION The Rio Açu coast is located in the federal state of Rio Grande do Norte, Brazil, in the eastern part of the Potiguar Basin. Together with the Recôncavo Tucano, Jatobá, Rio do Peixe and the Sergipe-Alagoas Basins, the Potiguar Basin forms part of the NE Brazilian Rift System ( , 1994). The Barreiras Formation was deposited in the Potiguar Basin during the Pliocene, and these sediments provided the source material for alluvial fans, beach ridges and offshore sediment bodies generated during the transgression and regression phases of the Pleistocene ( , 1993). Few previous studies have dealt with the early Holocene development of the northern Rio Grande do Norte coast. However, there has been recent interest in the hydro- and morphodynamics and geological development of the coastal domain during the Quaternary, especially with regard to sea level fluctuations ( , 2002, , 2003,). Most of these investigations were based on sediments taken from emerged shorelines or seabottom-surface sediments ( 1997). Seismic data from coastal areas were restricted to the shelter of spits and their use was limited ( , 2002). Our investigation covers part of the continental shelf offshore from Rio Grande do Norte (Figure 1). The specific area is bounded by latitudes 4°50'S 5°00'S and longitudes 36°30'W 36°50'W, where the shelf width is only 40 km. This area features an open, wave dominated, mesotidal coast with a tidal range of 3 m during spring tide and 0.8 m during neap tide ( , 1979). The coastline is interrupted by a number of small rivers, of which the most important is the Rio Açu. Sediment supply to the coastal area from this river is decreasing as a dam now controls the river discharge. A channel-like depression cut into the seafloor represents the seaward continuation of the river mouth. This channel extends to the shelf edge (Figure 1). In the Rio Grande do Norto region, sea level lowstand during the last glacial maximum (LGM), ~20 000 cal. yr. BP, is calculated at 107 m below present sea level ( , 1998). Sea level highstands occurred at 5800 to ~5000 cal. yr. BP, reaching about 1.2 - 4.0 m above present sea level ( , 2003, , 2004). The prime focus of our study is the late Pleistocene/early Holocene development of the Rio Açu valley, which was cut into former, pre-Holocene, shelf deposits. Hydroacoustic data were collected in March 2002 using the vessel SAO FRANCISCO III. The equipment consisted of an EG & G Uniboom shallow seismic boomer system (bandwidth 0.3 - 15 kHz) and NWC processing software. Pulses of 150 Joules were generated at a pulse rate of 2.7 shots per second. A single-channel system was used for data collection. Shallow seismic reflection pulses were amplified and digitally recorded. Seismic velocity can vary between 200-2000 m/s in soft, water saturated sediments. Therefore, the velocity of sound in water (~1500 m/s) was used for both water and sediments in order to calculate the penetration depth and thickness of the different layers. This approach has worked well elsewhere ( , 2000). The maximum penetration depth achieved was ~65 m below present sea level (where the seafloor was at 25 m water-depth), and the vertical resolution between different layers was 0.3 m. The furthest seaward extension of the seismic profiles was 24 km offshore (Figure 1). MATOS MARTIN CALDAS BEZERRA COSTA- NETO, HAYES PELTIER BEZERRA STATTEGGER SCHWARZER et al. et al. et al. et al. et al. et al. CALDAS VAIL VAN WAGONER LURTON ANDERSON HAMPTON METHODS Post-collection processing of the data consisted of contrast enhancement, filtering, stacking and the application of a time variable gain (TVG) to amplify deeper layers. Seismic interpretations were based on the principles of seismic stratigraphy ( , 1987), and the development of depositional sequences and system tracts by identifying discontinuities in reflector terminations and analysing the seismic facies within each seismic sequence ( , 1987). A seismic facies is defined by distinct reflection patterns including reflector configuration, continuity, amplitude, frequency and external form ( , 2002). A combination of these parameters enables a geological interpretation to be developed, including environmental setting, depositional processes, and an estimation of the lithology. Instances of acoustic turbidity, the so-called "gas effect", occurred in some areas and prevented the acoustic signals from penetrating into the sediment ( and , 1980 a,b). ‡ Dept. of Geology/CCET, Campus Universitário Universidade Federal do Rio Grande do Norte, CP 1639 - Natal - RN 59072-970, [email protected] Journal of Coastal Research Special Issue 39, 2006 ,
Transcript of HoloceneCoastalEvolutionoftheRioAçuArea(RioGrandedoNorte...
Journal of Coastal Research SI 39 141 - 145 ICS 2004 (Proceedings) Brazil ISSN 0749-0208
SCHWARZER, K.; STATTEGGER, K.; VITAL, H. and BECKER, M., 2006. Holocene coastal evolution of the RioAçu area (Rio Grande do Norte, Brazil). Journal of Coastal Research, SI 39 (Proceedings of the 8th InternationalCoastal Symposium), 141 - 145. Itajaí, SC, Brazil, ISSN 0749-0208.
The coastal development of the RioAçu area (Rio Grande do Norte, Brazil) and the response of the river mouth to theHolocene sea level rise were reconstructed from seismostratigraphy. A sharply defined stratigraphic boundarybetween the Pleistocene and Holocene deposits was recognised. The seismic data reveal that, during sea levellowstand, a valley up to 9 km wide was cut into the Pleistocene deposits of the shelf platform. This valley extendsperpendicular to the shoreline and is preserved in the recent morphology. It narrows at ~20 km offshore to a 1kmwide channel, which then widens to its former size a few hundred meters further offshore.Several incised valleys and cut and fill structures up to 2500 m wide and 12 m deep were observed in the Pleistocenedeposits. These extend to 45 m below sea level, and indicate that the ancient Rio Açu meandered. A sedimentsequence with sigmoidal structures increases in thickness offshore to 12 m, is composed of reworked material, and isinterpreted as an embankment.A tilted block composed of more solid material was identified over a distance of at least 800 m. Holocene sedimentsthin out above this block, indicating postglacial neotectonics in the area.
ADDITIONALINDEX WORDS: NE Brazil, holocene sea level rise, seismostratigraphy, neotectonics.
ABSTRACT
Holocene Coastal Evolution of the RioAçuArea (Rio Grande do Norte, Brazil)
K. Schwarzer †; K. Stattegger †;, H. Vital ‡ and M. Becker †
†Institute of GeosciencesKiel University,24118 Kiel, [email protected]@gpi.uni-kiel.de
INTRODUCTION
The Rio Açu coast is located in the federal state of RioGrande do Norte, Brazil, in the eastern part of the PotiguarBasin. Together with the Recôncavo Tucano, Jatobá, Rio doPeixe and the Sergipe-Alagoas Basins, the Potiguar Basinforms part of the NE Brazilian Rift System ( , 1994). TheBarreiras Formation was deposited in the Potiguar Basin duringthe Pliocene, and these sediments provided the source materialfor alluvial fans, beach ridges and offshore sediment bodiesgenerated during the transgression and regression phases of thePleistocene ( , 1993).
Few previous studies have dealt with the early Holocenedevelopment of the northern Rio Grande do Norte coast.However, there has been recent interest in the hydro- andmorphodynamics and geological development of the coastaldomain during the Quaternary, especially with regard to sealevel fluctuations ( , 2002, , 2003,). Mostof these investigations were based on sediments taken fromemerged shorelines or seabottom-surface sediments (
1997). Seismic data from coastal areas were restricted tothe shelter of spits and their use was limited ( , 2002).
Our investigation covers part of the continental shelfoffshore from Rio Grande do Norte (Figure 1). The specific areais bounded by latitudes 4°50'S 5°00'S and longitudes 36°30'W36°50'W, where the shelf width is only 40 km. This area featuresan open, wave dominated, mesotidal coast with a tidal range of 3m during spring tide and 0.8 m during neap tide ( , 1979).The coastline is interrupted by a number of small rivers, ofwhich the most important is the RioAçu. Sediment supply to thecoastal area from this river is decreasing as a dam now controlsthe river discharge. A channel-like depression cut into theseafloor represents the seaward continuation of the river mouth.This channel extends to the shelf edge (Figure 1).
In the Rio Grande do Norto region, sea level lowstand duringthe last glacial maximum (LGM), ~20 000 cal. yr. BP, iscalculated at 107 m below present sea level ( , 1998).Sea level highstands occurred at 5800 to ~5000 cal. yr. BP,reaching about 1.2 - 4.0 m above present sea level (
, 2003, , 2004).
The prime focus of our study is the late Pleistocene/earlyHolocene development of the Rio Açu valley, which was cutinto former, pre-Holocene, shelf deposits.
Hydroacoustic data were collected in March 2002 using thevessel SAO FRANCISCO III. The equipment consisted of anEG & G Uniboom shallow seismic boomer system (bandwidth0.3 - 15 kHz) and NWC processing software. Pulses of 150Joules were generated at a pulse rate of 2.7 shots per second. Asingle-channel system was used for data collection. Shallowseismic reflection pulses were amplified and digitally recorded.Seismic velocity can vary between 200-2000 m/s in soft, watersaturated sediments. Therefore, the velocity of sound in water(~1500 m/s) was used for both water and sediments in order tocalculate the penetration depth and thickness of the differentlayers. This approach has worked well elsewhere (
, 2000). The maximum penetration depth achieved was~65 m below present sea level (where the seafloor was at 25 mwater-depth), and the vertical resolution between differentlayers was 0.3 m. The furthest seaward extension of the seismicprofiles was 24 km offshore (Figure 1).
MATOS
MARTIN
CALDAS BEZERRA
COSTA-NETO,
HAYES
PELTIER
BEZERRA
STATTEGGER
SCHWARZER
et al.
etal.
et al.
et al.
et al.
et al.
CALDAS
VAIL
VAN WAGONER
LURTON
ANDERSON HAMPTON
METHODS
Post-collectionprocessing of the data consisted of contrast enhancement,filtering, stacking and the application of a time variable gain(TVG) to amplify deeper layers. Seismic interpretations werebased on the principles of seismic stratigraphy ( , 1987),and the development of depositional sequences and systemtracts by identifying discontinuities in reflector terminationsand analysing the seismic facies within each seismic sequence( , 1987). A seismic facies is defined bydistinct reflection patterns including reflector configuration,continuity, amplitude, frequency and external form ( ,2002). A combination of these parameters enables a geologicalinterpretation to be developed, including environmental setting,depositional processes, and an estimation of the lithology.Instances of acoustic turbidity, the so-called "gas effect",occurred in some areas and prevented the acoustic signals frompenetrating into the sediment ( and , 1980a,b).
‡ Dept. of Geology/CCET, Campus UniversitárioUniversidade Federal do Rio Grande do Norte,CP 1639 - Natal - RN 59072-970,[email protected]
Journal of Coastal Research Special Issue 39, 2006,
All profiles were run at a ship velocity of 3.5 knots. Shippositioning utilised DGPS, with accuracy in the range 0 10 m.Water depth was recorded digitally. The depth to different layersis reported in meters relative to the present sea level.
A channel extending from the river mouth to the shelf edgedominates the investigated area (Figure 1). This structure can becorrelated with the former river valley, now drowned, and isfilled with Pleistocene and Holocene deposits. In each of thetransverse profiles I - IV (Figure 2), the eastern margin of thechannel is relatively steep and pronounced whereas the westernmargin consists only of a gentle slope. The gradient of theeastern margin is 24 : 100, and the depth of the central channel is18 m relative to the surrounding seafloor. In the furthestoffshore profile V, the Channel narrows to an 1100 m-widetrench incised into a solid block-like structure (Figure 3). This
"block" has a steep northern flank, clearly visible in profile VI.Acoustic turbidity occurs in the vicinity of the block andprevents the signal from penetrating into the subsurface. This"gas effect" extends for approximately 2 km around the block,and also appears locally in other parts of the channel.
Figure 4 shows part of profile VI (12030201b-d), whichfollows the channel in a longitudinal direction. A strongreflector, horizon I, divides the subsurface into an uppersediment sequence characterised by sigmoidal structures and alower sediment sequence consisting of uniform sub-horizontallayers. This division extends over a distance of approximately1200 m. The upper sigmoidal sediment sequence increases inthickness offshore. Low contrast impedes exact differentiationbetween top- and downlapping structures. Nevertheless, it isevident that the single layers are dipping northwards and thatthe northern end of each layer is always below the southern endof the subsequent (and therefore younger) layer. This isconsistent with the upper sigmoidal sediment sequenceprogressively migrating offshore with decreasing age.
Sediment layers on both sides of the "tableau" structure havethe highest inclination recorded by the entire set of boomerprofiles. East of the tableau, these layers dip towards the incisedvalley structure at a gradient of 6 : 100. The tableau is entirelycovered by young sediments, but these thin strongly towards thetop of the tableau (Figure 6).
RESULTS
Figure 1. The investigation area showing the bathymetry andthe location of all seismic profiles. The first six numbers of theprofiles indicate day, month and year (ddmmyy).
Figure 2. Morphology of the channel offshore the Rio Açu. Thenarrow channel and steep eastern slope are evident in profile V.The boundary between Holocene and Pleistocene deposits ismarked by the lower solid line in Profile II.
Figure 3. Bathymetry and seismostratigraphy near the channel.The shaded area (small figure) marks the enlarged sector.Acoustic turbidity, the channel and its steep eastern flank arevisible .
Figure 4. Part of the channel-parallel profile VI (12030201c).Sigmoidal structures are evident in the sediment abovehorizon I.
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ANALYSIS
DISCUSSION
Figure 7 provides a summary of all seismostratigraphic unitsthat were clearly identified and distinguished in the Rio Açuarea. Most of these are best developed on profile III (11030201and 11030201b, see Figure 1). They are numbered from I to VII,with the order of numbering being from the uppermost(youngest) to the lowest (oldest). This order was chosen toallow for further subsurface studies that might identify moreunits below the deepest of our investigation.
Unit I is defined as the parallel layers extending from therecent seafloor down to horizon I. Unit II represents thesigmoidal sediment sequence, which was only recognised inone section of the valley-parallel profile VI (Figure 4). Thesigmoidal structures dip gently to the north, and are below Unit Ibut above horizon I. Unit III was not described in detail. Itoccurs directly below horizon I near the incised valley, andthickens towards the valley with a maximum thickness of 15 m.It is seismically transparent. Unit IV encompasses the incisedvalley structure. Unit V is a sediment sequence characterised by"chaotic structures", showing hummocky stratification andpronounced reflectors that extend only over short distances.This seismostratigraphic unit is also not described in detail.Unit VI represents the tableau-like structure. Unit VII wasidentified below the incised valley and below Unit V, but couldnot be penetrated during our survey. It is the deppest sedimentsequence.
Horizon I was located in all profiles, and is gentlynorthwards dipping at a gradient of 2 : 1000.
The continental shelf off Rio Grande do Norte hasexperienced regressive and transgressive stages during thePleistocene and until recent times. Therefore, the entire channelstructure from the mouth of the Rio Açu to the shelf edge can beregarded as an incised valley, cut into the shelf deposits duringsea level lowstands.
The ancient Rio Açu river meandered within this incisedvalley, cutting into the shelf deposits and forming smallerincised valleys now represented by cut and fill structures(Figure 7, Unit IV). These are indicative of the erosional force
....
of the river during lowstand conditions. Unit IV contains manystrong reflectors, which are interpreted as pebble beds orconsolidated sediments. The hummocky structures of Unit Vare probably relic fluvial sediments from the meandering river.Unit VII is interpreted as the surface and its underlying layersduring lowstand conditions. These sediments are clearlyseparated from those of Unit I, which forms the present seafloorthroughout the investigated area. Unit I is composed of parallelmarine sediment layers deposited during the Holocenetransgression up to now. Thus, horizon I delineates theboundary between marine sediments deposited after theHolocene transgression reached this area, and terrestrialdeposits formed during the Pleistocene and early Holocene.
The seismically transparent Unit III occurs immediatelybelow horizon I, but overlies the hummocky structures (Unit V)and the incised valley deposits (Unit VI) (Figure 7). This unit isonly observed in profile III (11030201). Elsewhere, lagoonaldeposits are characterised by their seismic transparency andpoor internal stratification arising from their very high contentof silt, clay and organic material. The location of Unit III and itsseismic characteristics are thus consistent with early Holocenedeposition in a low energy environment sheltered byembankments or ridges.
Sigmoidal structures characterise Unit II, at the transitionbetween horizon I and the overlying sub-horizontal layers ofUnit I. (1977) noted that a similar configurationof seismic reflectors is indicative of sea level rise combinedwith low sediment supply, which permits topset beds toaggregate simultaneously with foreset progradation. In thiscase, such structures would develop during sea level riseaccompanied by a prograding shoreline. The observedstructures do not allow a distinction between these scenarios ifthe sigmoidal structures are arranged within topset layering.However, the slight offshore increase in depth of Unit IIindicates no topset layering but may be evidence of formationduring an interval of either sea level fall or stagnation, oralternatively a periodic increase in sediment supply. Such amodel fits well with our interpretation of Unit III, which alsosuggests an interval of sea level stagnation.
The tableau-like structure (Unit VI) indicates recent tectonicactivity has occurred, and this is interpreted as uplift from thesymmetry of the Unit I layers on the western and eastern flanksof the tableau. These layers are not interrupted on the flanks, and
MITCHUM et al.
Figure 5. Incised valley and a cut and fill structure in profile III(11030201b).
Figure 6.Young Holocene sediments thin over a buried "tableau-like" structure of more solid material.
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143Holocene Coastal Evolution
their thickness decreases towards the top. As Unit VI is buriedby Unit I, the uplift must have occurred during the Pleist
Seismic data (boomer profiles) were acquired and used toinvestigate the subsurface geology and structure of the RioGrande do Norte coastal shelf, NE Brazil. The investigationfocussed on the interpretation of seismostratigraphic units, andunits attributed to both Pleistocene regression and Holocenetransgression were identified. The incised valley of the ancientriver is preserved as a channel extending from the present-dayriver mouth to the shelf edge. A continuous strong reflector,identified in all profiles, represents the sea level lowstandsurface. This reflector separates the Pleistocene deposits fromthe early Holocene deposits.
A regression phase, or at least stagnation, is indicated byoffshore dipping, sigmoidal structures in re-worked fluvialmaterial. Evidence of late Pleistocene / early Holocene tectonicactivity was also discovered.
We thank the German Research Foundation (DFG) forfunding this project, "Holocene Coastal Development andRecent Sediment Dynamics in Rio Grande do Norte (north-east
Brazil)", grant no.: STA 401/712. We are also grateful toHelmut Beese for outstanding technical support and fieldassistance under sometimes difficult environmental conditions,and to Eugênio Pires Frazão for supplying us withbathymetrical data and logistical support.
and , 1997. The acoustic turbidlayer in muddy sediments of Eckernförde Bay, WesternBaltic: methane concentration, saturation and bubblecharacteristics. , 137 147.
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2003. Sedimentological and SeismicInvestigations in the River Mouth Area of the Rio Açu, RioGrande do Norte, (NE-Brazil). Kiel, Germany: KielUniverity, Institute of Geosciences; Master´s thesis, 66p.
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oceneor early Holocene. A compilation of all profiles demonstratesthat this tectonic activity was not restricted to profile III, butextends over a distance of at least 10 km in a N-S direction.
In localised areas of the channel, acoustic turbiditypenetrates the sediment layers from below. In most cases the gaseffect stops ~15 m below the sediment surface. However, onprofile V where the channel narrows to an 1100 m-wide trench,the effect is apparent close to the sediment surface. TheBrazilian oil company PETROBAS is extracting oil ~25 km tothe east of our investigation area. While acoustic turbidity inmuddy sediments is mostly related to the decomposition oforganic material (Abegg and Anderson, 1997), the nearby oildeposits may also be contributing gas to the sediments.
CONCLUSIONS
ACKNOWLEDGEMENTS
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