Seismostratigraphy of the inner shelf adjacent to Suape Bay, Northeastern Brazil

ABSTRACT

Geotechnical and environmental studies widely use shallow geophysical imaging methods to indirectly acquire high-resolution subsurface data at a low cost for constructing three-dimensional models. Among these, seismic methods are especially valuable for investigating shallow submerged environments due to their capacity to produce detailed subsurface images. This study analyzes seismic facies patterns based on high-resolution shallow seismic profiles collected during a geotechnical investigation of the continental shelf offshore the Port of Suape, seeking to improve the understanding of the sedimentary and structural evolution of the transitional zone between the offshore and onshore regions of the Pernambuco Basin. The dataset comprises 14 multichannel 2D seismic sections, totaling 6.4 km of survey lines. Integrating sonographic data, borehole logs, sediment samples, and photographs enabled classifying three main types of seabed: (i) homogeneous mud seafloor; (ii) subaqueous dunes with gravel and sand; and (iii) irregular rocky substrate partially covered by sand. Interpretation of the seismic profiles identified five key reflections, including the present-day seabed and four major unconformities, And five seismic facies: (a) Facies I - unconsolidated sandy and muddy sediments (Quaternary); (b) Facies II - sandstones and shales of the Suape Formation (Lower-Middle Albian); (c) Facies III - basal deposits of the Cabo Formation (Barremian-Aptian); (d) Facies IV - carbonate mounds of the Estiva Formation (Cenomanian-Turonian); and (e) Facies V - crystalline basement (Ipojuca Magmatic Suite). Seismic and geotechnical data integrated allowed the reconstruction of stratigraphic layers associated with rift and post-rift phases of the basin. Additionally, a prominent positive seismic anomaly and normal faults trending NW-SE occurred at the basement top, suggesting extensional tectonic activity linked to the South Atlantic Rift.

Keywords:
Sub-bottom profiler; Side scan sonar; Pernambuco Sedimentary Basin; Port of Suape

INTRODUCTION

Seismic methods have long been employed in investigations of shallow underwater environments (Atherton, 2011; Barboza et al., 2021; Blondel, 2009; Fish and Carr, 1990; Jones, 1999; Mosher, 1999; Souza, 2006; Souza and Mahiques, 2013; Souza et al., 2013). High-resolution geophysics help to investigate subsurface environments using high-frequency spectrum, applying principles similar to those of conventional seismic reflection methods (Bataille and Chiu, 1991; Bruno, 2023; Kearey et al., 2009; Sieck and Sief, 1977). However, this approach differs from conventional techniques due to its specialized data acquisition systems, unique acoustic sources, and specific frequency spectra - variations essential for achieving higher resolution in complex subsurface investigations (Zhou, 2014). The demand for investigating subsurface sedimentary layers or acoustic basement parameters, such as contour and depth (rocky substrates), is met by applying acoustic systems that operate at low frequencies (<20 kHz) and high energy (100-300 J) (Souza, 2006).

High-frequency seismic sonographic patterns are interpreted in close relation to the physical characteristics of marine sedimentary materials, which allows identifying and classifying various seabed features, including morphology, sediment distribution, and benthic habitats (Bartholomä, 2006; Collier and Brown, 2005; Lathrop et al., 2006; Morang et al., 1997). Revealed reflection patterns correspond to the physical nature of the deposits and can be interpreted based on their continuity, frequency, and reflective properties (Fabin et al., 2019). Seismic facies patterns are characterized by their amplitude and continuity, which enable distinguishing seismic facies groups and defining three dimensional sedimentary successions and classifications (Mitchum et al., 1977a; Sheriff, 1980). The patterns interpreted from geophysical data, combined with the distribution of physical rock parameters, produce correlations that reflect types of deposits and sedimentary processes with similar characteristics (Ayres Neto, 2000; Belo et al., 2002; Catanzaro et al., 2004; Damuth, 1975, 1980; García-García et al., 2004; Morang et al., 1997; Quaresma et al., 2000; Souza, 2006).

Side-scan sonar is widely applied in seafloor mapping and seabed classification. Appropriate interpretation of acoustic data identifies sedimentary facies, subsurface stratified layers, and the associated geological processes (Barnhardt et al., 1998; Bartholomä, 2006; Gomes et al., 2015; Hogan et al., 2013). This approach is a valuable tool for integrating sequence stratigraphy studies and addressing questions regarding the evolution of sedimentary marginal basins and Quaternary events along the coastal zone, including tectonic influences and sedimentary reworking caused by successive sea-level variations (Cooper et al., 2002; Cunningham et al., 1998; Gomes et al., 2015; Işler et al., 2008).

The Southern Pernambuco Continental Shelf, part of the Brazilian Eastern Continental Shelf Margin, includes the Pernambuco Marginal Sedimentary Basin (PMSB), situated at the continent-marine interface (Figure 1). On land, the basin is narrow and elongated, structurally controlled by normal faults, and bounded by the Pernambuco Shear Zone to the north and a transform fault in the southernmost region. In the marine environment, the basin is wide, covering the entire SPCS (Barbosa et al., 2014). Its origin is linked to the final separation of the African and South American continents during the Aptian.

Figure 1
Location of the study area near the Suape Industrial Port Complex (d), on the coast of the State of Pernambuco (a), and within the coverage of Nautical Chart 906 (c) (DHN, 2014). The elongated red polygons indicate the position of the External Access Channel to the Port of Suape, where the shallow seismic survey was conducted. The white polygon on Cocaia Island (d) delineates the exposed portion of the Estiva Formation. The region is also marked by a positive gravimetric anomaly (Figure 1b), ranging from circular to elliptical in shape, aligned with the highlands of Cabo de Santo Agostinho and extending across both onshore and offshore sectors of the Pernambuco Marginal Sedimentary Basin (Correia Filho, 2017).

PMSB’s complex evolution is characterized by strong structural control and sea-level fluctuations which have influenced sedimentary deposits and seafloor morphology (Araújo Júnior et al., 2020; Macêdo et al., 2020; Tassinari et al., 2024). Neotectonic activity has affected PMSB via the reactivation of the basement rocks’ transcurrent regime and more recent faulting (Correia Filho et al., 2019). This mechanism has significantly deformed the sedimentary deposits of Northeastern Brazil marginal sedimentary basins, impacting sediment deposition and topography (Bezerra et al., 2014; Lima et al., 2017). Despite advances in understanding depositional processes, the relationship between PMSB onshore and offshore sedimentary deposits and the evolution of the continental shelf in this region remains poorly understood due to scarce data on the transition zone of the shallow marine platform, between the onshore and offshore areas.

Mapping and identifying the sedimentary facies that constitute the seafloor stratigraphy enable the correlation of sedimentation processes influenced by sea-level variations and the role of structural control in sediment deposition patterns on the continental shelf. This approach can provide important information for analyzing the sediment fill pattern related to tectonic reactivations, and establishing possible ages for the main pulses of reactivations and sedimentation of the shallow marine platform during the Cenozoic era.

Thus, this study performed a tectono-stratigraphic analysis and investigated the depositional architecture of the continental shelf based on shallow seismic surveys in the PMSB offshore region near Suape Bay. All 2D subsurface data were acquired using high-resolution shallow seismic profiling and integrated with surface information obtained from side scan sonar and a percussive drilling campaign, allowing for the identification of five seismic facies associated with the sedimentary evolution of PMSB.

STUDY AREA AND GEOLOGICAL SETTING

The study area is situated along the southern coast of the state of Pernambuco (Figure 1a), between the municipalities of Ipojuca and Cabo de Santo Agostinho. It is located near the Suape Industrial and Port Complex, approximately 40 km south of Recife (state capital). Additionally, the study area coincides with a prominent positive gravimetric anomaly (Figure 1b), ranging from circular to elliptical, which aligns with the highlands of Cabo de Santo Agostinho. This anomaly extends across both the onshore and offshore regions of the PMSB (Correia Filho, 2017).

The PMSB is associated with the fragmentation of the supercontinent Gondwana, based on the progradational rift model (Barbosa et al., 2014; Bueno, 2004; Lima Filho, 1998; Matos, 1999). This process unfolded in at least four stages, progressing from south to north, ultimately forming the Atlantic Ocean and the sedimentary basins along the Brazilian continental margin, as well as their counterparts on the African side.

The PMSB is bounded to the south by the Alagoas Basin, separated by the Maragogi High, and to the north by the Paraíba Basin through the Pernambuco Shear Zone (PESZ) (Figure 2). Offshore, the basin extends northward to the northern portion of the Pernambuco Plateau (Alves and Costa, 1986). It can be further divided into two sectors: the inner rift, which follows a narrow strip along the eastern coast of Northeastern Brazil, and a second rift located in deep and ultra-deep waters (Barbosa and Lima Filho, 2005, 1998; Morais, 2008). The Maracatu High marks the boundary between the internal basin and the plateau (Almeida et al., 2005).

Figure 2
Schematic map of the PMSB showing its structural domains. The upper image illustrates the PMSB domain, extending from the narrow onshore portion to the deep offshore waters. The lower image presents stratigraphic profiles along lines AA’ and BB’. Modified from Barbosa et al. (2014).

The stratigraphic framework proposed by Lima Filho (1998) for the PMSB comprised three lithostratigraphic units: the Cabo Formation (Aptian-Albian), the Estiva Formation (Cenomanian-Turonian), and the Algodoais Formation (Post-Turonian-Paleogene), in addition to the Ipojuca Magmatic Suite (IMS), which exhibits a primary magmatic pulse dated at 102 Ma and extends until 72 Ma (Nascimento, 2003, 2018). However, a subsequent revision of the basin’s stratigraphy retained the Cabo Formation as the basal unit while reclassifying the middle Albian succession into the Suape Formation and the Paraíso Formation (Maia et al., 2012; Maia, 2012). The Estiva Formation consists of carbonate deposits exhibiting a wide variation of facies (Barbosa et al., 2008; Menor and Boujo, 2002) and associated with three distinct transgressive pulses. Although carbonate facies dominate the sedimentation, interbedded layers of shales and calcareous sandstones are also present (Amaral and Menor, 1979; Lima Filho, 1998; Lima Filho and Santos, 2001).

The first transgressive pulse is defined by whitish-gray, fine-grained limestones overlying arkoses and shales, likely of Neo-Albian age, in the region of the Port of Suape. The second pulse is marked by marine carbonates with a strong terrigenous influence toward the continent, transitioning from marly limestones to siliciclastic limestones (Figure 1d). Finally, the last pulse consists of limestones identified in well cores, overlying the IMS rocks (also Neo-Albian in age) and capped by an erosional surface known as the Pré-Barreiras (Amaral and Menor, 1979) or Pré-Algodoais surface (Lima Filho, 1998).

MATERIALS AND METHODS

The data used in this research were collected for geotechnical studies in the Suape Port region along with bathymetric data obtained from the Bathymetry Project (Ladeira Neto and Roza, 2013), conducted by the (CPRM) Serviço Geológico do Brasil (SGB) in collaboration with the Agência Nacional de Petróleo (ANP).

The high-resolution shallow water seismic survey was conducted using a portable Sub-Bottom Profiling System model Edgetech 3100-P, equipped with an SB216S sensor. This sensor transmits linearly distributed wideband frequency-modulated pulses, sweeping across a full frequency spectrum of 2-16 kHz over a 20-millisecond duration. This technology, known as Compressed High-Intensity Radar Pulse (CHIRP), enables the individual interpretation of transmitted frequencies, resulting in the generation of higher-resolution subsurface images.

The high-resolution seismic data are generated from frequencies captured by hydrophones and processed through filtering techniques. This approach is particularly effective for areas with dredging debris, structural features, and consolidated subsurface formations. The signal emission source consists of an air gun with a central frequency, while the receiver is a hydrophone with a resolution compatible with the source’s frequency. To enhance the acoustic response, preliminary calibration tests were conducted before the survey to adjust the equipment settings and improve the quality of the data collected, enabling the generation of clearer images.

The side scan sonar survey was conducted using a frequency of 500 kHz, with a total swath width ranging from 100 to 150 meters, corresponding to 50 m and 75 m of lateral range on each side, respectively. The transducer was towed at an average layback distance of approximately 5 meters from the stern of the vessel. For the acquisition of sonographic profiles, a 560P digital acquisition system was used, operating with the Discover software, connected to an EdgeTech side scan sonar, model 4100. The system also included an EdgeTech ACI interface board and a TD-272 transducer.

SEISMIC DATA ACQUISITION

The seismic profiles in this study were divided into twelve sub-areas for profiling, consisting of a set of 35 longitudinal lines along the External Access Channel of the Port of Suape (EACPS), each approximately 530 meters long, with reference based on nautical chart number 906, provided by the Diretoria de Hidrografia e Navegação (DHN) of the Brazilian Navy. The seismic profile corresponds to a data set formed by fourteen planes of survey lines (Figure 6a).

The survey was conducted using a prospecting array composed of a platform with a computer, an amplifier, and a hydrodynamic vehicle, towed by a small boat and operated through the data acquisition and navigation software Hypack Survey and Hysweep Survey. The real-time positioning of the equipment in the operational area was achieved using a Smart Antenna DGPS receiver, configured to receive differential corrections via the OmniSTAR satellite-based augmentation system. This configuration ensured sub-meter accuracy, typically ranging between ±0.10 to ±0.50 meters, allowing precise determination of the dynamically occupied geographic positions of the survey boat. Such accuracy enabled systematic and homogeneous coverage of the study area. The transducer was towed at an average depth of 1.10 m above the estuarine bed, using cable out values of 9.0 m and 0.0 m (central axis of the vessel) to determine the layback.

The data acquisition system used was the Discover Sub-Bottom Full Spectrum Sonar Operation, 3200-XS system, which is employed exclusively for data acquisition, visualization, and pre-processing. The geographic projection used during the survey was WGS84, with the UTM coordinate system in zone 25S.

PRE-PROCESSING AND PROCESSING OF SHALLOW SEISMIC DATA

In the pre-processing of seismic data and throughout the processing workflow, the Reflex Win v.6.1 software was used to filter noise via the interactive 2D-Data-Analysis module, which is useful for the processing and interpretation of 2D seismic data and for defining the predominant structural units (Gomes, 2009).

The raw data were saved in the standard format recommended for acquisition, JSF (EdgeTech JSF Format). Subsequently, the seismic data were loaded and converted into the standard Seg-Y (SGY) format, which enables the visualization of acoustic signals, interpretation, and modeling.

For parameterization testing, the processing workflow was applied in the following sequence: (1) reading the seismic profile, including the import of raw data; (2) geometric analysis, involving the determination of the actual profile extent, removal of initial acquisition gain, and manual truncation of the two-way travel time at 100 ms; (3) spectral analysis, amplifying the seismic signal using the first derivative and exporting the frequency spectrum for spectral window extraction; (4) one-dimensional predictive deconvolution filtering to smooth double signals, followed by two-dimensional filtering along the X and Y directions to attenuate the effects of multiple reflections and noise, thereby improving the temporal resolution of the traces (Gadallah, 1994); (5) application of geometric divergence compensation gain, enhancing deep reflections; (6) enhancement of key reflections through the envelope detection method.

DETERMINATION AND INTERPRETATION OF THE SEQUENCE BOUNDARIES

The determination of the top and bottom sequence boundaries of the units interpreted from the seismic survey was performed using the Sub-bottom Processing tool in Hypack. Depth values were adjusted and referenced according to the tide gauge station at the Port of Suape (F-41).

The records were processed and interpreted to highlight features on the seafloor surface and in the subsurface, focusing on identifying the main seafloor morphologies and the structural arrangement of seismic reflections for the characterization of seismic facies.

RESULTS

Seismic data were correlated with sonographic patterns derived from mosaics produced by the Sub-Bottom Profiling System with lateral scanning, and with seabed samples collected across the EACPS area, where dredging operations were conducted.

SONOGRAPHIC PATTERNS OF SURFACE DEPOSITS

The correlation between geophysical patterns and sediment distribution helped to identify sonographic signatures that reflect sediments and sedimentary processes with similar characteristics (Belo et al., 2002; Catanzaro et al., 2004; Damuth, 1980; Flood, 1980; Hollister and Heezen, 1972; Morang et al., 1997; Quaresma et al., 2000). This enables the qualitative classification of sonographic reflections based on parameters such as contrast derived from grayscale gradients, backscatter intensity, acoustic impedance of the seafloor, and the texture and homogeneity of the records (Ayres Neto and Aguiar, 1993).

According to Figueiredo (2008), the analysis identified two types of seafloor substrates: consolidated and unconsolidated. These were further classified into three sonographic types (adapted from Microars, 2007), as illustrated in Figure 3, and described as follows: (I) low-intensity homogeneous - found at the beginning of the EACPS, it exhibits a smooth sonographic texture, light gray reflection pattern, uniform signal intensity, and a predominant grain size distribution; (II) subaqueous dunes - the most abundant feature in the area, occurring in both the Outer Harbor and the EACPS. They present a dark gray reflection pattern, with alternating high- and low-intensity signals; (III) irregular seabed - outcrops observed in four areas of the EACPS seafloor, corresponding to a moderately reflective substrate with alternating light and dark returns.

Figure 3
Shallow seismic surveys along the maneuvering basin of the External Port and EACPS. (A) Sonographic mosaic showing the main types of seabed patterns. (B) Interpretation of the primary sonographic patterns, with three types identified: a homogeneous, low-intensity pattern, a heterogeneous pattern associated with wave marks, and a heterogeneous/rough pattern with medium reflection. The black points indicate the locations of two boreholes, HDT 03 and HDT 06. The black line represents the seismic section, and the red polygons mark areas with competent material where underwater dismantling occurred.

CORRELATION BETWEEN SONOGRAPHIC DATA, SURFACE SAMPLES, AND BOREHOLE RECORDS

A correlation between sonographic patterns and the local stratigraphic material was established by selecting two boreholes (HDT 03 and HDT 06) within the EACPS region (Figure 3b), representing the study area (Figure 4). Borehole HDT 03 is located at a bathymetric depth of 17 m and comprises two distinct layers: the first is a 2.05 m-thick layer of unconsolidated sediments consisting of medium- to fine-grained sand with sparse shell fragments and fossil corals. Beneath this, a consolidated layer 1.95 m thick extends to a depth of 21.00 m, composed predominantly of sandstone with minor siltstone intercalations. Borehole HDT 06, at a depth of 18.10 m, presents a thin surface layer (0.25 m) of fine to medium-grained sand with occasional shell fragments and fossil corals. This layer overlies a 1.23 m-thick layer of gray limestone which, in turn, covers a final layer of gray mudstone with a thickness of 1.02 m. Both boreholes present a variable-thickness layer of unconsolidated sandy sediments deposited atop beds of chemical and clastic sedimentary rocks.

Figure 4
Borehole data from the EACPS. Boreholes HDT-03 and HDT-06 have thicknesses of 4.0 m and 2.5 m, respectively, with bathymetric depths of 17.00 m and 18.10 m. Both boreholes show unconsolidated sandy sediments of variable thickness forming the seafloor and overlying chemical (limestone) and clastic sedimentary rocks. Source: Modified from HDT, 2010.

Seabed surface samples and photographic images (Figure 5) allowed the identification of the various materials composing the seabed. The low-intensity homogeneous sonographic pattern (Figure 5A) predominantly consists of unconsolidated, brownish mud, primarily composed of clay. Locally, it varies from clayey mud (Figure 5B) to silty sand (Figure 5C) and is associated with sedimentation at the mouths of the Tatuoca and Massangana estuaries, driven by flocculation processes. The subaqueous dunes (Figure 5D) are associated with sand deposits of grain sizes ranging from fine to very coarse, along with gravel. The gravel layers consist primarily of quartz grains and bioclasts originating from reworked algal fragments, corals, foraminifera, and marine shell debris (Figure 5E). In contrast, the sandy sediments consist mainly of quartz sand, with little to no bioclastic influence (Figure 5F). These sediments are continuously mobilized by waves and currents, forming sand waves and mega-ripples. The irregular seabed (Figure 5G) consists of sand layers that partially cover the rocky substrate, identified in core samples as carbonates, sandstones, siltstones, and mudstones, correlated with PMSB geological units (Figures 5H and 5I). In addition to the core samples, analysis of the photographic records of materials dredged during underwater rock removal operations revealed the presence of massive, finely crystallized beige limestones (Figure 7). These irregular seabed areas occur on the shallow shelf of the sedimentary basin, between isobaths of 16 and 18 m depth, covering a surface area of 476,373.10 m².

Figure 5
Main sonographic patterns and surface sediment sampling of the seafloor in the study area (modified from Microars, 2007). (A) The homogeneous low-intensity pattern consists of a clayey and sandy-clayey substrate (B and C), characterized by a smooth seafloor. (D) The subaqueous dune pattern is composed of gravelly sand and bioclasts (E and F) (Eicomnor, 2013a, 2013b). (G) The irregular seafloor pattern consists of a rocky substrate partially covered by sandy sediments (H and I) (Eicomnor, 2012).

SEISMIC DATA INTERPRETATION

Seismic patterns were categorized based on the characteristics of the emitted signals, sediment properties, bed irregularity, and the presence or absence of sub-reflections. Seismic data analysis identified the acoustic responses of the substrates and classified them into five seismic reflections corresponding to stratigraphic boundaries - one representing the seafloor and the others indicating unconformities - and five seismic facies (Figure 6).

Figure 6
Seismic Interpretation of the EACPS. (A) Raw data and seismic interpretation of the stratigraphic arrangement related to the PMSB. (B) Raw and processed data from Line 2. Seismic facies I occur as an outcrop on the seafloor and consists of Quaternary sediments (reflection 1). Seismic facies II are bounded at both the top and base by unconformities (2 and 3, respectively) and appear from outcropping to sub-outcropping. It is composed of fluvio-lacustrine sandstones and mudstones and interpreted as strata of the Suape Formation. The basal deposits are not directly overlying the crystalline basement (reflection 4) and show a discordant contact (reflection 3). These deposits are interpreted as seismic facies III, consisting of conglomerates, coarse sandstones, and arkoses of the Cabo Formation. Seismic facies IV correspond to the crystalline basement, associated with rocks of the Ipojuca Magmatic Suite and characterized by acoustic transparency. (C) Interpretation of processed data from Line 8, where underwater dismantling occurred during dredging operations for the EACPS. Seismic facies V consist of isolated, non-continuous bodies with mound-shaped structures discordant with the Suape Formation (reflection 5). These are composed of carbonates like those outcropping on Cocaia Island and are interpreted as deposits of the Estiva Formation.

The parallel arrangement of reflections, along with the clear identification of lateral continuity, is a key characteristic for classifying Seismic Facies I, typically observed in sandbank deposits. In addition to the planar-parallel configuration, this unit can also be distinguished by the presence of isolated reflections with high lateral continuity, showing a slight dip and irregular deposition commonly associated with low-energy dynamic environments (e.g., muddy seafloors). Seismic Facies I are linked to the development of mega-ripple forms which often overlie larger scale bedforms. The top of this unit corresponds to the continental shelf’s seafloor (Reflection 1), while its base rests on a continuous, linear reflection identified as an erosional surface (Reflection 2).

In Seismic Facies II, the reflection arrangement is characterized by both high and low amplitudes, with a parallel to subparallel configuration and limited lateral continuity. It is bounded at the top by Reflection 2 and at the base by Reflection 3, both marked by unconformities. This is further corroborated by the loss of seismic signals in certain areas which leads to the attenuation of key reflections, while in other regions the signal shows high penetration with an immediate amplitude response. These characteristics reveal reflections with a predominantly subparallel internal arrangement and challenges in identifying lateral continuity.

Sand waves, the most common seafloor features, characterize Seismic Facies III. Their presence suggests higher current velocities required for wave formation and maintenance. Another characteristic of this unit is the low penetration capacity of the seismic signal, primarily limited by the sediment type and composition, which is predominantly sandy and/or shows a certain degree of compaction. The irregular reflection arrangement distribution within this unit, accompanied by translucent and irregular facies, defines Seismic Facies III. Despite the low seismic penetration, the reflections at depth present a pattern, with a slight dip towards the steeper slope, while most reflections are arranged chaotically across much of the section. Additionally, this unit exhibits a sigmoidal distribution pattern in the reflection arrangement, with tangential upper and lower terminations relative to a reflection, indicating the presence of ancient drainage systems. This is further supported by concave configurations followed by inclined, subparallel patterns towards the channel axis (incised channels). Seismic Facies III are further distinguished by two erosional surfaces (unconformities): one at the top (reflection 3) and a deeper one at the base (reflection 4).

Seismic Facies IV are located below Reflection 4 and shows acoustic transparency and the complete absence of horizontally arranged overlying reflections.

Finally, a more detailed analysis of regions exhibiting a rough sonographic pattern, which defines Seismic Facies V, reveals emergent to sub-emergent seismic patterns. These are positioned below Seismic Facies I and above Seismic Facies II, regions where the acoustic signal shows reduced penetration. According to Fabin et al. (2019), this suggests greater signal attenuation which may indicate a degree of lithification, possibly associated with cementation. These facies exhibit a sequence of high-amplitude, planar-parallel reflections that are stacked and found in isolated areas, forming a homogeneous low-intensity pattern consisting of deposits with horizontal boundaries. This will be further detailed in the discussion section.

DISCUSSION

The study area is situated within the southern portion of the Cupe Sub-basin, extending from the Santo Agostinho High to the Barreiros-Maragogi High (Lima Filho, 1998). It is positioned along the coastal zone of the PMSB and corresponds to the Aptian-Albian siliciclastic sequence, which represents the rift phase and comprises three distinct stratigraphic units: the Cabo Formation (Barremian-Aptian), the Suape Formation (Lower to Middle Albian) (Maia et al., 2012), and the Estiva Formation (Cenomanian-Turonian) (Lima Filho, 1998).

The sedimentary strata lie directly above the crystalline basement (reflection V), which is correlated with rocks of the Ipojuca Magmatic Suite (Cabo de Santo Agostinho Granite). This basement exhibits a strong positive magnetic anomaly, circular to elliptical in shape, coinciding with the Cabo de Santo Agostinho High and characterized by volcanic centers and the exposure of a granitic body along the coastline, forming a headland (Correia Filho, 2017). The anomaly is not related to the continental margin of the basin; rather, it occurs in isolation within the narrow rift that forms the internal basin, spanning the entire range of the seismic survey.

Faults related to extensional tectonics occur at the top of the basement. These structures are associated with the early evolution of the South Atlantic Rift in the onshore portion of the PMSB and correspond to normal faults formed during the initial stages of margin rifting. They exhibit a NW-SE orientation (Lima Filho, 1998; Polônia, 1997) with significant length and offset, typically on a metric scale, and dip angles varying from steep to shallow.

The basal deposits (reflection 5), which overlie the crystalline basement, lack direct sampling for detailed characterization. Among the identified seismic facies, this unit represents the thickest sedimentary package, with layers ranging from 5 to 8 meters. These deposits exhibit discordant contact (reflection 3) with the overlying units (seismic facies II). These interpretations are consistent with Cruz et al. (2003) and Fabin et al. (in press), who classify the basal interval as seismic facies III, composed of conglomerates, coarse sandstones, and arkosic sandstones from the Cabo Formation. Above these, strata are limited at the top (reflection 2) and base (reflection 3) by unconformities, with thicknesses varying from 0.5 m to 4.0 m. These strata occur in a sub-outcropping form at the start and end of the EACPS area and as partially exposed outcrops near the central portion of the seismic line. Seismic Facies II consist of fluvio-lacustrine sandstones and mudstones, interpreted as the Suape Formation, which corresponds to the second phase of the rift (Lower to Middle Albian) (Fabin et al., in press).

Analysis of samples obtained from blasting operations during the EACPS dredging project (Eicomnor, 2012) revealed the presence of finely crystallized, massive limestone (Figure 7) along with younger carbonate facies composed of a microbialite-encrusting-coral assemblage. Due to the unavailability of samples, the fossil content could not be characterized. These facies are similar to those outcropping on Cocaia Island and correlate with the descriptions by Maciel (1968). The carbonates sampled through drilling exhibit variable thicknesses, ranging from a few dozen centimeters (20 cm to 50 cm) to a few meters (1 m to 3 m). These seismic facies (V) appear in seismic lines as isolated, discontinuous bodies, taking the form of mound-like structures that are discordant with the Suape Formation (reflection 5). Due to its lack of representative thickness and width relative to the extent of the EACPS seismic line, this unit was analyzed separately.

Figure 7
Carbonate samples collected during dredging operations associated with rock removal in the EACPS. In (A) and (B), massive, finely crystalline beige limestones are observed. In (C) and (D), younger carbonate facies are encrusted on the surface of the massive limestone, composed of microbialites and fossil corals.

The Paraíso Formation could not be identified by seismic facies interpretation, although it would be expected to correspond to the first sequence of the basin’s post-rift phase (Maia, 2012; Maia et al., 2012). Given its proximity to the coastal zone, the formation may be absent in this area either due to a lack of depositional conditions or erosion.

Seismic Facies I are bounded at the top by the modern seafloor and at the base by a regional unconformity (reflection 2) across the PMSB. This surface coincides with the Last Glacial Maximum (LGM), dated to approximately 21 ka BP, which marks the lowest global sea-level stand (Clark et al., 2009). Following this event, early postglacial marine transgression began between ca. 20 and 19 ka BP, marking the onset of a relative sealevel rise. This transgressive phase is identified by the systematic coastal onlap of the regional reflection - first recognized between 20 and 19 ka - which aligns with chronostratigraphic markers in adjacent seismic lines and is positioned stratigraphically below the overlying facies (Correia Filho, 2017; Lima Filho, 1998; Mitchum et al., 1977b; Polônia, 1997; Wilgus et al., 1988). Its identification is based on the systematic alignment of the reflection with chronostratigraphic markers in adjacent seismic lines and its coherent stratigraphic position relative to the overlying facies. This regression exposed nearly the entire continental shelf during the Quaternary Period (Corrêa, 1996; Suguio and Tessler, 1984; Suguio et al., 2005), culminating in the last Holocene transgression. This transgressive event reached the Holocene relative sea-level highstand, which occurred approximately 5,000 years ago. During this period, the mean sea level (MSL) stood between 5 and 7 meters above present-day MSL (Dominguez et al., 1990), marking the maximum marine incursion of the Holocene along the Brazilian coast. Seismic Facies I consist of unconsolidated sandy deposits with grain sizes ranging from fine to very coarse, including gravel. Gravel layers are predominantly composed of reworked quartz grains and algal bioclasts, including corals, foraminifera, and marine shell fragments. In contrast, sandy sediments consist primarily of quartz sand, with minimal bioclastic content (Figure 5F). These sediments correlate with Facies 1, 2, and 3 identified by Melo (2019) and are associated with recent sedimentation along the marine shelf, controlled by Quaternary eustatic variations (Mabesoone, 1964). The predominance of sandy-gravel facies may indicate a moderately hydrodynamic environment (Coutinho and Farias, 1979). Terrigenous mud would be confined to river mouth regions like the Ipojuca River and to the infilling of paleochannels on the continental shelf (Gomes et al., 2011; Vital et al., 2008).

Deepening of nearshore areas can accelerate coastal erosion by altering local hydrodynamics (Simões, 2009). Dredged zones become dynamically unstable and tend to undergo re-siltation in the short to medium term, indicating that part of the sedimentary cover may result from post-dredging deposition.

CONCLUSION

Analysis of a dataset comprising shallow seismic and side-scan sonar surveys conducted in the EACPS, along with surface samples and geotechnical borehole profiles from the study area, identified sedimentary strata associated with both recent depositional processes on the marine shelf and older sequences correlated with PMSB. Three distinct identified sonographic patterns characterize the seafloor in the port region:

1. the Homogeneous Low-Intensity Pattern, composed of clayey to clay-sandy muds, interpreted as estuarine sediments;

2. he Subaqueous Dune Pattern, characterized by sand waves and mega-ripples consisting of sand and gravel, related to recent shelf sedimentation;

3. the Irregular Seafloor Pattern, observed in four EACPS sectors, corresponding to sandy layers partially covering consolidated sedimentary outcrops from the PMSB, between 16 and 18-m depth.

The five seismic facies identified correspond to recent sedimentary cover and older subsurface strata in the port channel region, associated with the rift and post-rift phases of the PMSB. These deposits overlie a prominent positive gravimetric anomaly in the crystalline basement, composed of rocks from the Ipojuca Magmatic Suite (IMS). The following interpretations stand out:

• Seismic Facies V enabled mapping isolated, mound-shaped, discontinuous carbonate structures, with signs of lithification and limited acoustic penetration. These are interpreted as carbonate deposits of the Estiva Formation;

• Seismic Facies IV, characterized by acoustic transparency and the absence of overlying reflections, corresponds to the crystalline basement, the top of which presents extensional faults related to the opening of the South Atlantic margin;

• Seismic Facies III consist of conglomerates, coarse sandstones, and arkosic sandstones from the Cabo Formation, overlying the basement with a discordant contact. These deposits show low signal penetration, irregular seismic patterns, and deformed translucent facies. The sigmoidal reflection geometry, with tangential upper and lower terminations, suggests the presence of paleodrainage systems.

• Seismic Facies II are interpreted as fluvio-lacustrine sandstones and mudstones of the Suape Formation, occurring in outcrop to sub-outcrop conditions and bounded at the top (reflection 2) and base (reflection 3) by regional unconformities;

• Seismic Facies I, exposed at the seafloor (reflection 1), are associated with the Holocene transgression controlled by Quaternary eustatic fluctuations. These are characterized by plano-parallel, laterally continuous, and gently inclined reflections, indicative of deposition in a low-energy muddy environment at the onset of the EACPS. Mega-ripples frequently appear superimposed on the sandy substrate.

Thus, the study area presents a stratigraphic sequence representative of the rift phase of PMSB, with key formations including the Cabo, Suape, and Estiva Formations. Seismic data also reveal normal faults related to extensional tectonics and a prominent positive anomaly in the basement. Facies analysis indicates sedimentary units such as conglomerates, sandstones, and carbonates, and highlights the absence of the Paraíso Formation in the coastal sector. Moreover, it recorded recent sedimentation linked to Quaternary sea-level oscillations.

Despite these significant findings, high-resolution seismic imaging has limited penetration which may hinder identifying deeper stratigraphic layers. Future studies should consider the use of higher-energy sources such as Boomer systems, capable of penetrating up to 200 meters in water-saturated sandy sediments. These would enhance the imaging of basement structures at the onshore-offshore transition and provide more detailed resolution of the pre-rift and rift stratigraphy of PMSB.

DATA AVAILABILITY STATEMENT

The data that support the findings of this study are private and were provided by the Port of Suape (Pernambuco, Brazil). Authorization for data processing, interpretation, and publication was formally granted by the Port of Suape via email communication to the authors. Due to confidentiality restrictions, the original datasets are not publicly available.

SUPPLEMENTARY MATERIAL

Supplementary figures and tables include high-resolution versions of the interpreted seismic profiles, additional stratigraphic cross-sections, and a workflow summary of data processing and interpretation. All supplementary materials were authorized for publication by the Port of Suape and are available as online supplementary files accompanying this article.

ACKNOWLEDGMENTS

The authors would like to thank the reviewers for their insightful comments and constructive suggestions, which significantly contributed to improving the quality of this manuscript. The authors also acknowledge the Federal University of Pernambuco (Universidade Federal de Pernambuco, UFPE) and the Marine Geology and Geophysics Laboratory (Laboratório de Geologia e Geofísica Marinha, LGGM) for their technical, logistical, and institutional support during the development of this research.

REFERENCES

• Alves, P. C. & Costa, M. P. A. 1986. Interpretação sismoestratigráfica da porção norte do platô de Pernambuco e suas possíveis correlações com a Bacia Pernambuco-Paraíba. In: Congresso Brasileiro de Geologia (34 ed., pp. 286-297).
• Almeida, C. B.; Cruz, L. R.; Sá, E. F. J.; Vasconcelos, P. M. P.; Medeiros, W. E. 2005. Tectônica e relações estratigráficas na Sub-Bacia de Pernambuco, NE do Brasil: contribuição ao conhecimento do Rifte Sul Atlântico. Boletim de Geociências da Petrobras, 13(2), 167-180.
• Amaral, A. J. R. & Menor, E. A. 1979. A seqüência Vulcano-sedimentar cretácea da região de Suape (PE): interpretação faciológica e considerações metalogenéticas. In: Simpósio de Geologia do Nordeste (9 ed., pp. 251-269).
• Araújo Júnior, J. C. M., Moura, W. A. L., Silva, I. M. G., Correia Filho, O. J., Souza Neto, J. A. 2020. Caracterização Estrutural da Região Central do Graben do Cupe, Bacia Sedimentar de Pernambuco: Implicações para o Padrão Atual da Rede de Drenagem. Revista Brasileira de Geografia Física, 13(05), 2355-2370. DOI: https://doi.org/10.26848/rbgf.v13.5.p2355-2370
  » https://doi.org/10.26848/rbgf.v13.5.p2355-2370
• Ayres Neto, A. 2000. Uso da sísmica de reflexão de alta resolução e da sonografia na exploração mineral submarina. Brazilian Journal of Geophysics, 18(3), 242-256. DOI: https://doi.org/10.1590/S0102-261X2000000300004
  » https://doi.org/10.1590/S0102-261X2000000300004
• Ayres Neto, A. & Aguiar, A. C. K. V. 1993. Interpretação de reflexões de Side Scan Sonar: uma proposta de nomenclatura e padronização de métodos. In: Congresso Internacional de Geofísica (1 ed., pp. 399-403).
• Atherton, M. W. 2011. Echoes and Images: The Encyclopedia of SideScan and Scanning Sonar Operations. Vancouver, OysterInk Publications.
• Barbosa, J. A. & Lima Filho, M. F. 2005. Os domínios da Bacia da Paraíba. In: Congresso Brasileiro de P&D em Petróleo e Gás (3 ed.). Available from: Available from: https://portalabpg.org.br/PDPetro/3/trabalhos/IBP0333_05.pdf Access date: 2025 Oct. 27.
  » https://portalabpg.org.br/PDPetro/3/trabalhos/IBP0333_05.pdf
• Barbosa, J. A., Ferreira, P. J., Lima Filho, M. 2008. Dente de um picnodontiforme (Actinopterygii, Neopterygii) da Formação Estiva, Cenomaniano-Turoniano da Bacia de Pernambuco, NE do Brasil. GAEA - Journal of Geoscience, 4(2), 43-48.
• Barbosa, J. A., Maia, M. F., Lima Filho, M., Magalhães, J. R. & Correia, O. J. 2014. Seismic Stratigraphy of the Onshore Portion of Pernambuco Basin: Evidence of Break-Up during Middle Albian for the South Atlantic Rift in Northeast Brazil. In: Annual Convention and Exhibition.
• Barboza, E. G., Dillenburg, S. R., Lopes, S. R., Rosa, M. L. C. C., Caron, F., Manzolli, R. P., Nunes, J. C. R., Weschenfelder, J. & Tomazelli, L. J. 2021. Geomorphological and stratigraphic evolution of a fluvial incision in the coastal plain and inner continental shelf in southern Brazil. Marine Geology, 437, 106514. DOI: https://doi.org/10.1016/j.margeo.2021.106514
  » https://doi.org/10.1016/j.margeo.2021.106514
• Barnhardt, W. A., Kelley, J. T., Dickson, S. M. & Belknap, D. F. 1998. Mapping the Gulf of Maine with Side-Scan Sonar: A New Bottom-Type Classification for Complex Seafloors. Journal of Coastal Research, 14(2), 646-659. Available from: Available from: https://journals.flvc.org/jcr/article/view/80648/77831 Access date: 2025 Oct. 27.
  » https://journals.flvc.org/jcr/article/view/80648/77831
• Bartholomä, A. 2006. Acoustic bottom detection and seabed classification in the German Bight, southern North Sea. Geo-Marine Letters, 26, 177-184. DOI: https://doi.org/10.1007/s00367-006-0030-6
  » https://doi.org/10.1007/s00367-006-0030-6
• Bataille, K. & Chiu, J. M. 1991. Polarization analysis of high-frequency, three-component seismic data. Bulletin of the Seismological Society of America, 81(2), 622-642. DOI: https://doi.org/10.1785/BSSA0810020622
  » https://doi.org/10.1785/BSSA0810020622
• Belo, W. C., Dias, G. T. M., Dias, M. S. 2002. O Fundo Marinho da Baía da Ilha Grande, RJ: O Relevo Submarino e a Sedimentação no Canal Central. Revista Brasileira de Geofísica, 20(1), 5-15. DOI: https://doi.org/10.1590/S0102-261X2002000100001
  » https://doi.org/10.1590/S0102-261X2002000100001
• Bezerra, F. H. R., Rossetti, D. F., Oliveira, R. G., Medeiros, W. E., Neves, B. B. B., Balsamo, F. Nogueira, F. C. C., Dantas, E. L., Andrades Filho, C. & Góes, A. M. 2014. Neotectonic reactivation of shear zones and implications for faulting style and geometry in the continental margin of NE Brazil. Tectonophysics, 614, 78-90. DOI: https://doi.org/10.1016/j.tecto.2013.12.021
  » https://doi.org/10.1016/j.tecto.2013.12.021
• Blondel, P. & Murton, B. J. (1997). Handbook of Seafloor Sonar Imagery. Chichester: John Wiley & Sons Ltd., 314p.
• Blondel, P. 2009. The handbook of sidescan sonar. Springer. DOI: https://doi.org/10.1007/978-3-540-49886-5
  » https://doi.org/10.1007/978-3-540-49886-5
• Bruno, P. P. 2023. Seismic Exploration Methods for Structural Studies and for Active Fault Characterization: A Review. Applied - Sciences, 2023, 13(16), 9473. DOI: https://doi.org/10.3390/app13169473.
  » https://doi.org/10.3390/app13169473.
• Bueno, G. V. 2004. Diacronismo no Rifte Sul-Atlântico. Boletim de Geociências da Petrobrás, 12, 203-229. Available from: Available from: https://bgp.petrobras.com.br/bgp/article/view/175/116 Access date: 2025 Oct. 27.
  » https://bgp.petrobras.com.br/bgp/article/view/175/116
• Catanzaro, L. F., Baptista Neto, J. A., Guimarães, M. S. D. & Silva, C. G. 2004. Distinctive Sedimentary Processes in Guanabara Bay - SE/Brazil, based on the Analysis of Echo-Character (7.0 kHz). Revista Brasileira de Geofísica, 22(1), 69-83. DOI: https://doi.org/10.1590/S0102-261X2004000100006
  » https://doi.org/10.1590/S0102-261X2004000100006
• Clark, P. U., Dyke, A. S., Shakun, J. D., Carlson, A. E., Clark, J., Wohlfarth, B., Mitrovica, J. X., Hostetler, S. W. & McCabe, A. M. 2009. The Last Glacial Maximum. Science, 325(5941), 710-714. DOI: https://doi.org/10.1126/science.1172873
  » https://doi.org/10.1126/science.1172873
• Collier, J. S. & Brown, C. J. 2005. Correlation of sidescan backscatter with grain size distribution of surficial seabed sediments. Marine Geology, 214(4), 431-449. https://doi.org/10.1016/j.margeo.2004.11.011
  » https://doi.org/10.1016/j.margeo.2004.11.011
• Cooper, J. A. G., Kelley, J. T., Belknap, D. F., Quinn, R. & McKenna, J. 2002. Inner shelf seismic stratigraphy off the north coast of Northern Ireland: new data on the depth of the Holocene lowstand. Marine Geology, 186(3-4), 369-387. DOI: https://doi.org/10.1016/S0025-3227(02)00311-0
  » https://doi.org/10.1016/S0025-3227(02)00311-0
• Corrêa, I. C. S. 1996. Les variations du niveau de la mer Durant les derniers 17.500 anos BP: l’exemple de la plate-forme continentale du Rio Grande do Sul-Brésil. Marine Geology, 130(1-2), 163-178. DOI: https://doi.org/10.1016/0025-3227(95)00126-3
  » https://doi.org/10.1016/0025-3227(95)00126-3
• Correia Filho, O. J. 2017. Análise de estruturas compressionais na região onshore da Bacia Pernambuco, NE do Brasil - possíveis influências no potencial petrolífero (Mestrado em Geociências). Recife: Universidade Federal de Pernambuco. Available from: Available from: https://repositorio.ufpe.br/handle/123456789/23738 Access date: 2025 Oct. 27.
  » https://repositorio.ufpe.br/handle/123456789/23738
• Correia Filho, O. J., Barbosa, J. A., Tavares, B., Silva, H. A., Monteiro, K. A., Fabin, C. E. G., Oliveira, J. T. C., Santana, F. R., Silva, S. M. 2019. Reativação Tectônica Quaternária no Domínio Sul da Província Borborema, NE do Brasil: Integração de Dados Morfométricos, Geológicos e Geofísicos da Bacia do Rio Una. Anuário do Instituto de Geociências, 42(4), 219-237. DOI: https://doi.org/10.11137/2019_4_219_237
  » https://doi.org/10.11137/2019_4_219_237
• Coutinho, P. N. & Farias, C. C. 1979. Contribuição à origem dos recifes do Nordeste. In: Simpósio de Geologia do Nordeste (9 ed., pp. 236).
• Cunningham, A. P., Barker, P. F., Tomlinson, J. S. 1998. Tectonics and sedimentary environment of the North Scotia Ridge region revealed by side-scan sonar. Journal of the Geological Society, 155, 941-956. DOI: https://doi.org/10.1144/gsjgs.155.6.0941
  » https://doi.org/10.1144/gsjgs.155.6.0941
• Cruz, R. L., Lima Filho, M. F., Neumann, V. H. M. L., Sá, E. F. J., Silva, F. C. A., Frutuoso Jr., L. J., Nascimento, M. A. L., Guedes, I. M. G., Antunes, A. F., Almeida, C. B. & Melo, K. J. V. 2003. As unidades siliciclásticas da Sub-bacia de Pernambuco: uma revisão lito-estratigráfica. In: Congresso Brasileiro de P&D em Petróleo e Gás (2 ed., pp. 50).
• Damuth, J. E. 1975. Echo character of the western Equatorial Atlantic floor and its relationship to the dispersal and distribution of terrigenous sediments. Marine Geology, 18(2), 17-45. DOI: https://doi.org/10.1016/0025-3227(75)90047-X
  » https://doi.org/10.1016/0025-3227(75)90047-X
• Damuth, J. E. 1980. Use of high-frequency (3.5-12 kHz) echograms in the study of near-bottom sedimentation processes in the deep-sea: a review. Marine Geology, 38(1-3), 51-75. DOI: https://doi.org/10.1016/0025-3227(80)90051-1
  » https://doi.org/10.1016/0025-3227(80)90051-1
• Damuth, J. E. & Hayes, D. E. (1977). Echo character of the east Brazilian continental margin and its relationship to sedimentary processes. Marine Geology, 24(2), 73-95. https://doi.org/10.1016/0025-3227(77)90002-0
  » https://doi.org/10.1016/0025-3227(77)90002-0
• DHN (Diretoria de Hidrografia e Navegação). 2014. Carta Náutica nº 906 - Abordagens ao Porto de Suape. Escala 1:25.000. Rio de Janeiro, Marinha do Brasil.
• Dominguez, J. M. L., Bittencourt, A. C. S. P., Leão, Z. M. A. N. & Azevedo, A. E. G. 1990. Geologia do quaternário costeiro do estado de Pernambuco. Revista Brasileira de Geociências, 20(1-4), 208-215. Available from: Available from: http://bjg.siteoficial.ws/1990/23.pdf Access date: 2025 Oct. 27.
  » http://bjg.siteoficial.ws/1990/23.pdf
• Eicomnor Engenharia. 2012. Relatório Analítico RE-SUA-11.16.0-330-EIC-001. Elaboração do Projeto Executivo e Supervisão da Dragagem do Canal de Acesso Externo de Suape.
• Eicomnor Engenharia. 2013a. Relatório de Estudo Geotécnico RE-SUA-11.16.0-331-EIC-001. Relátorio de Sondagens Jet-Prob e Rotativa no Canal de Acesso ao Porto de Suape.
• Eicomnor Engenharia. 2013b. Relatório de Batimetria RE-SUA-12.09.0-310-EIC-002. Serviços Técnicos de Engenharia para a Execução de Levantamento Topo-Batimétrico no Porto Interno e Externo de Suape.
• Fabin, C. E. G. S. O., Correia Filho, O. J., Alencar, M. L., Araújo, A. F. L., Ramos, G. M. S., Barbosa, J. A. 2019. Study of Recent Sedimentation in the Recife Port Based on Shallow Seismic Data. Anuário do Instituto de Geociências, 42(2), 19-31. DOI: https://doi.org/10.11137/2019_2_19_31
  » https://doi.org/10.11137/2019_2_19_31
• Fabin, C. E. G. S. de O., Arruda, S. D. d’A., Alencar, M. L., Manso, V. A. V., Almeida, N. M., Macêdo, R. J. A. & Soares Junior, C. F. A. (2025, submitted). New Lithostratigraphic Correlations of the Pernambuco Marginal Basin: Stratigraphic Reanalysis Based on Borehole Data. Submitted to Geosciences.
• Fish, J. P. & Carr, H. A. 1990. Sound Underwater Images: a guide to the generation and interpretation of side scan sonar data. Burlington, EG&G Marine Instruments.
• Figueiredo, T. S. 2008. Mapeamento batimétrico e sonográfico da plataforma Continental interna adjacente ao complexo industrial e portuário de Suape, Pernambuco-Brasil (Mestrado em Oceanografia). Recife: Universidade Federal de Pernambuco, 2008.
• Flood, R. D. 1980. Deep-sea sedimentary morphology: modelling and interpretation of echo-souding profiles. Marine Geology, 38(1-3), 77-92. DOI: https://doi.org/10.1016/0025-3227(80)90052-3
  » https://doi.org/10.1016/0025-3227(80)90052-3
• Gadallah, M. R. 1994. Reservoir Seismology: Geophysics in Nontechnical Language. Tulsa, Pennwell Corp.
• García-García, A.; García-Gil, S. & Vilas, F. 2004. Echo characters and recent sedimentary processes as indicated by high-resolution sub-bottom profiling in Ría de Vigo (NW Spain). Geo-Marine Letters, 24, 32-45. DOI: https://doi.org/10.1007/s00367-003-0156-8
  » https://doi.org/10.1007/s00367-003-0156-8
• Gomes, M. P. 2009. Aquisição, Processamento e Análise de Dados de Sísmica de Alta Resolução na Plataforma Continental Norte do Rio Grande do Norte: Vale Inciso do Rio Açu (Mestrado em Geodinâmica e Geofísica). Natal: Universidade do Rio Grande do Norte. Available from: Available from: https://repositorio.ufrn.br/handle/123456789/18767 Access date: 2025 Oct. 27.
  » https://repositorio.ufrn.br/handle/123456789/18767
• Gomes, M. P., Vital, H. & Macedo, J. W. P. 2011. Fluxo de processamento aplicado a dados de sísmica de alta resolução em ambiente de plataforma continental: exemplo: Macau-RN. Revista Brasileira de Geofísica, 29(1), 173-186. DOI: https://doi.org/10.1590/S0102-261X2011000100012
  » https://doi.org/10.1590/S0102-261X2011000100012
• Gomes, M. P., Vital, H., Eichler, P. P. B. & Sen Gupta, B. K. 2015. The investigation of a mixed carbonate-siliciclastic shelf, NE Brazil: side-scan sonar imagery, underwater photography, and surface-sediment data. Italian Journal of Geosciences, 134(1), 9-22. DOI: https://doi.org/10.3301/IJG.2014.08
  » https://doi.org/10.3301/IJG.2014.08
• HDT Drilling. 2010. Project Suape External Channel Dredging. HDT 01 to 06.
• Hogan, K. A., Dowdeswell, J. A. & Mienert, J. 2013. New insights into slide processes and seafloor geology revealed by side-scan imagery of the massive Hinlopen Slide, Arctic Ocean margin. Geo-Marine Letters, 33, 325-343. DOI: https://doi.org/10.1007/s00367-013-0330-6
  » https://doi.org/10.1007/s00367-013-0330-6
• Hollister, C. D. & Heezen, B. C. 1972. Geologic effects of ocean bottom currents: western North Atlantic. In: Gordon, A. L. (Ed.). Studies in Physical Oceanografy (pp. 37-66). New York: Routledge.
• Işler, E. B., Aksu, A. E., Yaltirak, C. & Hiscott, R. N. 2008. Seismic stratigraphy and Quaternary sedimentary history of the northeast Aegean Sea. Marine Geology, 254(1-2), 1-17. DOI: https://doi.org/10.1016/j.margeo.2008.04.003
  » https://doi.org/10.1016/j.margeo.2008.04.003
• Jones, E. J. W. 1999. Marine geophysics. Chichester, Willey.
• Kearey, P., Brooks, M. & Hill, I. 2009. Geofísica de Exploração. São Paulo, Oficina de Textos.
• Ladeira Neto, J. F. & Roza, J. B. 2013. Relatório de conclusão do Projeto Batimetria: Acordo de cooperação técnica entre a CPRM e ANP. Rio de Janeiro, CPRM, ANP. Escala 1: 300.000. Available from: Available from: https://rigeo.sgb.gov.br/handle/doc/18152 Access date: 2025 Oct. 27.
  » https://rigeo.sgb.gov.br/handle/doc/18152
• Lathrop, R. G., Cole, M., Senyk, N. & Butman, B. 2006. Seafloor habitat mapping of the New York Bight incorporating sidescan sonar data. Estuarine, Coastal and Shelf Science, 68(1-2), 221-230. DOI: https://doi.org/10.1016/j.ecss.2006.01.019
  » https://doi.org/10.1016/j.ecss.2006.01.019
• Lima, J. C. F., Bezerra, F. H. R., Rossetti, D. F., Barbosa, J. A., Medeiros, W. E., Castro, D. L. & Vasconcelos, D. L. 2017. Neogene-Quaternary fault reactivation influences coastal basin sedimentation and landform in the continental margin of NE Brazil. Quaternary International, 438, 92-107. DOI: http://dx.doi.org/10.1016/j.quaint.2016.03.026
  » http://dx.doi.org/10.1016/j.quaint.2016.03.026
• Lima Filho, M. F. 1998. Análise Estratigráfica e Estrutural da Bacia Pernambuco (Doutorado em Geoquímica e Geotectônica). São Paulo: Universidade de São Paulo.
• Lima Filho, M. F. & Santos, P. R. S. 2001. Biocronoestratigrafia da Bacia de Pernambuco: implicações ambientais e paleogeográficas. Revista Brasileira de Paleontologia, 2, 84.
• Mabesoone, J. M. 1964. Origin and age of the sandstone reefs of Pernambuco, Northeastern Brazil. Journal of Sedimentary Research, 34, 715-726. DOI: https://doi.org/10.1306/74D71177-2B21-11D7-8648000102C1865D
  » https://doi.org/10.1306/74D71177-2B21-11D7-8648000102C1865D
• Macêdo, R. J. A., Pereira, N. S. & Manso, V. A. V. 2020. Morphometric analysis of the Inner Continental Shelf in northeastern Brazil for seabed geomorphic classification. Journal of South American Earth Sciences, 104, 102847. DOI: https://doi.org/10.1016/j.jsames.2020.102847
  » https://doi.org/10.1016/j.jsames.2020.102847
• Maciel, E. 1968. Contribuição à geologia geral de Ipojuca, PE (Relatório de Graduação). Recife: Universidade Federal de Pernambuco.
• Maia, M. F. B. 2012. Revisão da estratigrafia do intervalo aptiano-albiano da bacia de Pernambuco, Nordeste do Brasil. (Mestrado em Geociências). Recife: Universidade Federal de Pernambuco. Available from: Available from: https://repositorio.ufpe.br/handle/123456789/12133 Access date: 2025 Oct 27.
  » https://repositorio.ufpe.br/handle/123456789/12133
• Maia, M. F. B., Barbosa, J. A., Lima Filho, M., Mort, H. P. & Santana, F. R. 2012. Características petrográficas e geoquímicas das formações siliciclásticas (aptiano-albiano) da Bacia de Pernambuco, NE do Brasil. Estudos Geológicos, 22, 55-75. Available from: Available from: https://periodicos.ufpe.br/revistas/index.php/estudosgeologicos/article/view/260933 Access date: 2025 Oct. 27.
  » https://periodicos.ufpe.br/revistas/index.php/estudosgeologicos/article/view/260933
• Matos, R. M. D. 1999. History of the northeast Brazilian rift system: kinematic implications for the break up between Brazil and west África. In: Cameron, N. R., Bate, R. H. & Clure, V. S. (Ed.). The oil and gas habitats of the South Atlantic (n. 153, pp. 55-73).
• Melo, M. C. S. S. 2019. Estudo Sedimentar Atual e Distribuição da Matéria Orgânica Sedimentar na Plataforma Interna e Média de Pernambuco (Doutorado em Oceanografia). Recife: Universidade Federal de Pernambuco. Available from: Available from: https://repositorio.ufpe.br/handle/123456789/38816 Access date: 2025 Oct. 27.
  » https://repositorio.ufpe.br/handle/123456789/38816
• Menor, E. A. & Boujo, A. 2002. A first approach to the marine sedimentary succession of the Estivas Formation, Pernambuco Basin, Northeastern Brazil. In: Congresso Brasileiro de Geologia (41 ed., pp. 315).
• Microars Engenharia. 2007. Relatório Final N° 01/07-SUAPE. Levantamentos Sismobatimétrico e Sonográfico no Canal de Acesso e Bacia de Evolução Externa do Porto de Suape (PE).
• Mitchum, J. R., Vail, P. R. & Sangree, J. B. 1977a. Stratigraphic interpretation of seismic reflec-tion pattern in depositional sequences. In: Payton, C. E. (Ed.). Seismic Stratigraphy - Applications to Hydrocarbon Exploration (pp. 117-134). Tulsa: American Association of Petroleum Geologists.
• Mitchum, R. M., Vail, P. R. & Thompson, S. 1977b. Seismic Stratigraphy and Global Changes of Sea Level, Part 2: The depositional sequence as a basic unit for stratigraphic analysis. In: Payton, C. E. (Ed.), Seismic Stratigraphy - Applications to Hydrocarbon Exploration (pp. 53-62). Tulsa: American Association of Petroleum Geologists.
• Morais, D. M. F. 2008. Sismoestratigafia do Cretáceo Superior/Neógeno nas Bacias de Pernambuco e da Paraíba NE do Brasil (Mestrado em Geociências). Recife: Universidade Federal de Pernambuco. Available from: Available from: https://repositorio.ufpe.br/handle/123456789/6319 Access date: 2025 Oct. 27.
  » https://repositorio.ufpe.br/handle/123456789/6319
• Morang, A., Larson, R. & Gorman, L. 1997. Monitoring the coastal environment; part III: geophysical and research methods. Journal of Coastal Research, 13(4), 1064-1085. Available from: Available from: https://www.jstor.org/stable/4298715 Access date: 2025 Oct. 27.
  » https://www.jstor.org/stable/4298715
• Mosher, D. C. 1999. Status and Trends of Marine High-resolution Seismic Reflection Profiling: data acquisition. Engineering, Environmental Science, Geology, 26, 174-188.
• Nascimento, M. A. L. 2003. Geologia, geocronologia, geoquímica e petrogênese das rochas ígneas cretácicas da província magmática do Cabo e suas relações com as unidades sedimentares da Bacia de Pernambuco, NE do Brasil (Doutorado em Geodinâmica e Geofísica). Natal: Universidade Federal do Rio Grande do Norte. Available from: Available from: https://repositorio.ufrn.br/jspui/handle/123456789/18361 Access date: 2025 Oct. 27.
  » https://repositorio.ufrn.br/jspui/handle/123456789/18361
• Nascimento, G. H. 2018. Estudo Geoquímico e Geocronológico de novas ocorrências das Rochas Vulcânicas da Suíte Magmática Ipojuca, Bacia de Pernambuco (Doutorado em Geociências). Recife: Universidade Federal de Pernambuco.
• Polônia, J. A. P. 1997. Geometria e cinemática do Rifte do Cabo, litoral Sul do Estado de Pernambuco (Mestrado em Geologia). Rio de Janeiro: Universidade Federal do Rio de Janeiro.
• Quaresma, V. S., Dias, G. T. M. & Baptista Neto, J. A. 2000. Caracterização da ocorrência de padrões de sonar de varredura lateral e sísmica de alta freqüência (3,5 e 7,0 kHz) na porção sul da Baía de Guanabara - RJ. Revista Brasileira de Geofísica, 18(2), 201-214. DOI: https://doi.org/10.1590/S0102-261X2000000200008
  » https://doi.org/10.1590/S0102-261X2000000200008
• Sheriff, R. E. 1980. Seismic Stratigraphy. Boston: International Human Resources Development Corporation. DOI: https://doi.org/10.1007/978-94-011-6395-8
  » https://doi.org/10.1007/978-94-011-6395-8
• Sieck, H. & Sief, G. W. 1977. Analysis of high resolution seismic data. In: Payton, C. E. (Ed.). Seismic Stratigraphy - Applications to Hydrocarbon Exploration (pp. 353-385). Tulsa: American Association of Petroleum Geologists.
• Silva, F. A., Marangoni, L. B. & Bassetti, M. A. (2021). Application of high-resolution seismic methods to characterize sedimentary structures on the Brazilian continental shelf. Marine Geology, 439, 106514. DOI: https://doi.org/10.1016/j.margeo.2021.106514
  » https://doi.org/10.1016/j.margeo.2021.106514
• Simões, M. H. 2009. Sistematização dos Aspectos Ambientais de Dragagens Portuárias Marítimas no Brasil (Mestrado em Engenharia Hidráulica). São Paulo: Universidade de São Paulo. DOI: https://doi.org/10.11606/D.3.2009.tde-21122009-160107
  » https://doi.org/10.11606/D.3.2009.tde-21122009-160107
• Souza, L. A. P. 2006. Revisão crítica da aplicabilidade dos métodos geofísicos na investigação de áreas submersas rasas (Doutorado em Oceanografia Química e Geológica). São Paulo: Universidade de São Paulo. DOI: https://doi.org/10.11606/T.21.2006.tde-30102006-171206
  » https://doi.org/10.11606/T.21.2006.tde-30102006-171206
• Souza, L. A. P. & Mahiques, M. M. (2013). II Manual de métodos en teledetección aplicada a la prevención de riesgos naturales en el litoral. In J. Alcántara-Carrió, I. Montoya-Montes & I. D. Correa-Arango (Eds.), Geofísica marina aplicada al estudio de los riesgos (pp. 133-158, Cap. 5). Barcelona: CYTED - Programa Iberoamericano de Ciencia y Tecnología para el Desarrollo. 438p
• Souza, L. A. P., Silva, M. & Ola, K. 2013. Why multi-frequency approach on shallow water seismic investigation? In: International Congress of the Brazilian Geophysical Society (13 ed., pp. 1-4). Available from: Available from: https://sbgf.org.br/mysbgf/eventos/expanded_abstracts/13th_CISBGf/Why%20multifrequency%20approach%20on%20shallow%20water%20seismic%20investigation Access date: 2025 Oct. 27.
  » https://sbgf.org.br/mysbgf/eventos/expanded_abstracts/13th_CISBGf/Why%20multifrequency%20approach%20on%20shallow%20water%20seismic%20investigation
• Suguio, K. & Tessler, M. G. 1984. Planície de cordões litorâneos quaternários do Brasil: origem e nomenclatura. In: Lacerda, L. D., Araújo, D. S. D. & Turcq, B. (Ed.). Restingas: Origem, Estrutura e Processos (pp. 15-25). Niterói: CEUFF.
• Suguio, K., Angulo, R. J. & Carvalho, A. M. 2005. Paleoníveis do mar e paleolinhas de costa. In: Congresso da Associação Brasileira de Estudos do Quaternário do Brasil (pp. 114-129).
• Tassinari, L. F. M., Araújo, T. C. M. & Barbosa, J. A. 2024. Neotectonic control of shelf valley formation on the southern Pernambuco continental shelf - Brazil. Ocean and Coastal Research, 72, e24002. DOI: http://doi.org/10.1590/2675-2824072.22151
  » http://doi.org/10.1590/2675-2824072.22151
• Vital, H., Stattegger, K., Amaro, V. E., Schwarzer, K., Frazão, E. P., Tabosa, W. F. & Silveira, I. M. 2008. A Modem High-Energy Siliciclastic-Carbonate Platform: Continental Shelf Adjacent to Northern Rio Grande do Norte State, NE Brazil. In: Hampson, G. J., Steel, R. J., Burgess, P. M. & Dalrymple, R. W. (Ed.). Recent advances in models of siliciclastic shallow-marine stratigraphy: introduction and perspectives (pp. 177-190). Claremore: Society for Sedimentary Geology.
• Vital, H., Gomes, M. P., Tabosa, W. F., Frazão, E. P., Santos, C. L. A. & Plácido Jr., J. S. (2010). Characterization of the Brazilian continental shelf adjacent to Rio Grande do Norte State, NE Brazil. Brazilian Journal of Oceanography, 58(spe1), 43-54. https://www.scielo.br/j/bjoce/a/fGXsDMsp7cQGRZnbhZHBXhc
  » https://www.scielo.br/j/bjoce/a/fGXsDMsp7cQGRZnbhZHBXhc
• Zhou, H.-W. 2014. Practical Seismic Data Analysis. Cambridge, Cambridge University.

• AI USE DISCLOSURE
  Artificial intelligence (AI) tools, including language models, were used solely to enhance the linguistic clarity and technical consistency of this manuscript. The scientific content, data interpretation, and conclusions are entirely the responsibility of the authors. No AI system contributed to the generation, modification, or validation of the scientific results or analytical procedures described herein.
• FUNDING
  The offshore data used in this study were acquired during geotechnical investigations and construction activities in the port area, with consent and authorization from the Port of Suape for their processing, interpretation, and publication. This research was supported by CAPES (Coordenação de Aperfeiçoamento de Pessoal de Nível Superior, Brazil) through a scholarship grant. Apart from that, this research did not receive financial support from funding agencies in the public, commercial, or not-for-profit sectors. Technical and logistical support, including data processing infrastructure and workspace, was provided by the Marine Geology and Geophysics Laboratory (LGGM) at the Federal University of Pernambuco (UFPE), Brazil.

Edited by

• Associate Editor:
  Nils Asp.

Publication Dates

• Publication in this collection
  30 Jan 2026
• Date of issue
  2026

History

• Received
  07 May 2025
• Accepted
  23 Oct 2025