Finisterra, LXI(131), 2026, e42870  
ISSN: 0430-5027  
doi: 10.18055/Finis42870  
Artigo de Investigação  
FLUVIAL TYPOLOGIES IN THE BRAZILIAN DRYLANDS:  
A STUDY ON THE APPLICATION OF THE METHODOLOGICAL PROPOSAL OF RIVER  
STYLES  
1
JOANA D’ARC MATIAS DE ALMEIDA  
1
ANTONIO CARLOS DE BARROS CORRÊA  
2
CARLA SUELANIA DA SILVA  
WEMERSON FLÁVIO DA SILVA  
1
ABSTRACT – In light of the increasing demand for methodological frameworks that underpin the conservation of  
landscape diversity, particularly within physiographic contexts that have been historically undervalued, such as tropical  
drylands, the River Styles methodology emerges as a significant approach. This methodology aims to generate a comprehensive  
set of spatialized information that addresses the systemic interplay of regional and local controls in shaping processual and  
morphological responses across drainage systems. Furthermore, it facilitates a deeper understanding of the functionality,  
maintenance, preservation, and sustainable management of fluvial environments. This study applies the River Styles  
methodology to a semi-arid basin in Northeastern Brazil, where the relationships between channel patterns and the formation  
of aggradation landforms is still poorly explored by the geomorphological literature. Seven distinct fluvial typologies were  
identified, grounded in the predominant physiographical, environmental, and processual characteristics of the area. The river  
styles delineated herein can serve as a valuable reference for the assessment and classification of other basins within the  
Brazilian semi-arid domain, as well as for comparative analysis with other semi-arid tropical regions situated in similar passive  
continental margin contexts.  
Keywords: River compartmentation; river styles; drylands; landscape units; hydrographic basin.  
RESUMO – TIPOLOGIAS FLUVIAIS NAS TERRAS SECAS BRASILEIRAS: UM ESTUDO SOBRE A  
APLICAÇÃO DA PROPOSTA METODOLÓGICA DE ESTILOS FLUVIAIS. Considerando a crescente demanda por  
propostas metodológicas que forneçam bases para a conservação da diversidade paisagística, sobretudo em contextos  
fisiográficos subestimados para esses fins como as terras secas tropicais, destaca-se a dos Estilos Fluviais, voltada à produção  
de um conjunto de informações espacializadas de caráter sistêmico acerca dos controles regionais e locais responsáveis por  
produzir características morfológicas e processuais ao longo das drenagens. Ademais, a metodologia aporta informações  
fundamentais para o reconhecimento da funcionalidade, manutenção, preservação e gestão sustentável dos ambientes fluviais.  
O presente trabalho aplicou a proposta metodológica de Estilos Fluviais a uma bacia semiárida do Nordeste do Brasil, onde as  
relações entre os padrões de canal e a criação de formas de agradação são ainda pouco enfocadas pela literatura geomorfológica.  
Foram identificadas sete tipologias fluviais com base nas características físicas, ambientais e processuais predominantes. Os  
estilos fluviais estabelecidos para a área podem servir de referência para o levantamento e classificação de outras bacias no  
domínio semiárido brasileiro, bem como para comparação com outras áreas tropicais semiáridas em contextos plataformais e  
de margem continental passiva.  
Palavras-chave: Compartimentação fluvial; estilos fluviais; terras secas; unidades de paisagem; bacia hidrográfica.  
HIGHLIGHTS  
●
●
The compatibility of application of river styles to Brazilian drylands.  
To understand river typologies for environmental conservation and water resources in a semi-  
arid context.  
●
River Styles in Brazilian drylands are constantly associated with structural and landscape  
controls.  
Recebido: 13/04/2025. Aceite: 10/01/2026. Publicado: 11/05/2026.  
Joana D'arc Matias de Almeida: joana.matias@ufpe.br  
1 Federal University of Pernambuco, Cidade Universitária, 50670-901, Recife, Brasil.  
2 Federal University of Amapá, Oiapoque, 68980-000, Brasil.  
Published under the terms and conditions of an Attribution-NonCommercial-NoDerivatives 4.0 International license.  
   
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
1.  
INTRODUCTION  
Irregular and concentrated precipitation, year-round high temperatures, and high evapotranspiration  
rates characterize the drylands of the Brazilian Northeast. The irregularity of rainfall produces long periods  
of drought interspersed with occasional peaks of significant rainfall, resulting in a particular  
geomorphological dynamic associated with the semi-arid river environment (Almeida, 2021; Bracken &  
Wainright, 2008; Souza et al., 2016). In addition to the surface processes peculiar to this type of environment,  
in its tropical variety, there are impacts on land use since European colonization, with more than 400 years  
of pastoral activities and traditional dry farming. These transformations have been producing complex  
responses in the landscape, especially regarding the fluvial morphological units, altering channel character  
and stability, and creating particular sets of morphologies (Almeida, 2021; Lima et al., 2021; Souza et al.,  
2016).  
Considering the diversity of river environments, proposals aimed at understanding these  
geomorphological systems in their varied spatial arrangements are necessary to obtain effective responses to  
water resource planning and management programs. In this sense, studies focused on the classification of  
river morphology have been widely disseminated in geomorphology. Many authors have suggested  
geomorphological schemes for classifying rivers, whether considering their landscape, morphological, or  
hydrosedimentological aspects, such as those of Miall (1996), Nanson and Croke (1992), Whiting and  
Bradley (1993) and Woolfe and Balzary (1996). Nonetheless, most studies dealing with river style  
classification have bypassed the drainage systems of the semi-arid Northeast of Brazil, remaining among the  
least known regions regarding their fluvial characteristics among the drylands of the world.  
In recent decades, innovative methodologies have emerged to develop river typologies that are  
grounded in realistic ecological and geomorphological settings. These approaches prioritize areal  
requalification and the comprehensive management of river environments.  
Within this framework, the River Styles theoretical-methodological model offers a nuanced  
geomorphological framework aimed at elucidating the behavior and evolution of rivers on a localized scale.  
This model places particular emphasis on channel dynamics and the structural characteristics of valley  
bottoms (Brierley et al., 2002; Fryirs & Brierley, 2009; Souza, 2014). Its primary objective is to  
systematically classify river segments by characterizing them based on a standardized set of  
geomorphological and hydrodynamic attributes. This classification allows for a clear differentiation of the  
behaviors and characteristics inherent to various river types (Brierley & Fryirs, 2005; Lima & Marçal, 2013).  
The River Styles proposal allows us to identify the relationships between processes and forms along  
rivers, in their different segments, based on the perspective that these occupy a place within the landscape  
context of the watershed, in such a way that a river can present different styles, according to the particular  
interaction of each segment with the landscape in its surroundings (Brierley & Fryirs, 2005).  
In this way, the methodology offers a comprehensive overview of the river landscape's structure,  
which can record the character and behavior of a river and offer a geomorphic assessment of its spatial and  
evolutionary patterns. The proposed analysis focuses on the drainage basin, considered as a set of attributes,  
which includes the morphostructural compartmentalization of the relief, the characteristics of the valley, the  
plan shape and geometry of the channel, the geomorphic units of the basin and the texture of the river bed  
(Brierley & Fryirs, 2005; Corrêa et al., 2009; Lima & Marçal, 2013).  
In the drylands of Northeastern Brazil, the methodology was applied by Almeida et al. (2016), Corrêa  
et al. (2009), Franco et al. (2022), Lima et al. (2021), Rodrigues and Souza (2020b), Rodrigues et al. (2023),  
Santos et al. (2023), Souza et al. (2016). The authors focused on a morphoclimatic context, whose fluvial  
landscapes have been largely overlooked. They pioneered addressing the existence of ephemeral basins  
characterized by sui generis aggradational forms in this Brazilian region, differentiated from intermittent  
rivers.  
The concept of River Styles offers a versatile framework for understanding the dynamics of rivers and  
landscapes, yet its application in semi-arid basins remains underexplored. This is notable given the potential  
benefits that its outcomes could yield for territorial planning. In this context, the present study seeks to apply  
the River Styles methodology within a semi-arid basin in the Brazilian Northeast.  
The primary objective is to establish a new typological framework for the identification of  
aggradational units. This framework aims to provide a more robust characterization that could serve as a  
foundation for the conservation and rehabilitation of ephemeral river channels. Such an approach is crucial,  
considering the diverse uses and environmental services these river systems offer to the region.  
2
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
2.  
METHODOLOGY  
The application of the River Styles methodology requires the creation of a database composed of a list  
of integrated geospatial attributes concerning the river forms, processes, and connections established between  
channels. This spatialized information on the morphological and structural aspects of the channels and their  
segments constitutes the basis for the four-tiered River Styles analysis and provides a basis for predictions  
on river behavior (Brierley & Fryirs, 2005).  
The first stage of the method involves the identification, interpretation, and mapping of river styles in  
a river basin. These procedures are the basis for characterizing the river behavior. The second stage consists  
of conducting assessments of river character and behavior from a dynamic perspective, where forms and  
processes are evaluated from an evolutionary standpoint. The third stage corresponds to evaluating the future  
trajectory of changes and the recovery potential of the river channel. Finally, the fourth stage focuses on river  
management applications by constructing qualitative and prognostic scenarios (Almeida, 2017; Brierley &  
Fryirs, 2005).  
In this work, the methodology proposed by Brierley and Fryirs (2005) was adapted, based on its first  
two stages, to provide a detailed geomorphological model to understand the behavior and evolution of the  
river system up to its current spatial arrangement. This work adapted the River Styles methodology with  
emphasis on the interaction between structural and anthropogenic conditions, in order to complete the  
definitions for the semi-arid region proposed by Lima et al. (2021), Souza (2014) and Souza et al. (2016).  
The identification of River Styles is based on the analysis of river sections, for which the degree of  
valley confinement, the number of channels, and the condition of channels' lateral stability are defined. The  
confinement classification aims to establish whether or not the flow overflows beyond the limits of the  
channel, and it is possible to identify three classes. The confined valley corresponds to the sectors that present  
floodplains in less than 10% of the river section; the partially confined valley occurs when 10 to 90% of the  
analyzed segment presents a discontinuous alluvial plain; while in the unconfined pattern, more than 90% of  
the section presents a continuous floodplain (Brierley & Fryirs, 2005; Souza, 2014).  
In this stage, orthophotomaps from the Pernambuco 3D Project, at a scale of 1:5 000, were used to  
identify current drainage patterns and fluvial deposits. As a result, the approach sought to build an  
information framework presenting the river's characteristics, behavior, and controls. At this stage,  
representative channel sections were identified. Next, the adjustment capacity of each section was analyzed.  
To assess the processual state of a river in relation to its surrounding landscape, it is essential to  
determine the adjustment capacity of each river segment and establish its specific morphology. The  
evolutionary trajectory of each segment must be analyzed to identify any irreversible changes and to pinpoint  
reference sections that facilitate a more in-depth interpretation of the prevailing geomorphological conditions  
(Almeida, 2017; Brierley & Fryirs, 2005). Fieldwork was conducted to substantiate the typologies identified,  
following a comprehensive geomorphological mapping of representative areas.  
To construct the river typologies, it was necessary to compartmentalize the landscape units that make  
up the watershed. To this end, primary data, such as the Digital Terrain Model (MDT) from the Pernambuco  
3D Project (Pernambuco, 2013), were used on a scale of 1:5 000 with an altimetric precision of 25cm. These  
data served as a basis for updating the landscape compartmentalization map proposed in Almeida (2021) for  
the basin and generating topographic profiles.  
Secondary data from other cartographic bases were also used, including geology (Serviço Geológico  
do Brasil [SGB], 2005a, 2005b, 2005c), geomorphology (Almeida, 2017), and pedology (Oliveira, 2016).  
Land cover and land use data were obtained from Almeida et al. (2016), which generated a mapping based  
on the legend proposed by Food and Agriculture Organization of the United Nations [FAO], (2014).  
2.1. Study area  
The Riacho Grande Basin (fig. 1), with an area of 316km², is located in the center of the state of  
Pernambuco, encompassing parts of the municipalities of Serra Talhada, Calumbi, and Flores, delimited by  
the geographic coordinates of 7°55' S / 37°55' W and 8°08' S / 38°12' W (Almeida, 2017; Almeida et al.,  
2016). The watershed constitutes a sub-basin of the Pajeú River, a tributary of the São Francisco River, the  
largest exotic river in South America, and the only perennial course to cross the semi-arid Northeast of Brazil.  
3
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
Fig. 1 – Location and hypsometry of the Riacho Grande basin.  
Fig. 1 – Localização e hipsometria da bacia do Riacho Grande.  
Source: Almeida (2021) and Almeida et al. (2025)  
Regarding the climatic context, the Riacho Grande basin is located in the semi-arid tropical domain of  
the interior of the Brazilian Northeast, with average monthly temperatures ranging from 22 to 26°C, total  
annual precipitation of less than 800mm, and an irregular interannual regime controlled by global-scale  
phenomena. The area is prone to prolonged droughts or torrential rains concentrated over short periods, even  
in unlikely times, which favors the occurrence of floods and inundations (Almeida et al., 2012; Alves et al.,  
2017; Aragão, 1998; Barros, 2018; Freire et al., 2011).  
Identifying landscape physiographic elements allowed the definition of the spatial controls operating  
over the fluvial domain. Relief morphostructural units were identified by analyzing the different classes of  
terrain roughness, which led to the basin's subdivision into three larger sectors (table 1 and fig. 2): the Pajeú  
Interplanaltic Depression, Structural Ridge Massifs, and the Betânia Sedimentary Plateau.  
Table I – Summary of the lithological framework of the study area.  
Quadro I – Síntese dos dados litológicos da área de estudo.  
Morphostructural Unit  
Lithological Framework  
Landscape setting  
São Caetano Complex Afogados da Ingazeira Complex  
Floresta Complex Indiscriminated granitoids Recanto - Riacho do Forno  
Suite  
Vegetated or unvegetated dissected  
pediments  
Pajeú intermontane  
depression  
Alluvial deposits  
Alluvial plains  
Structural ridge massifs  
Prata Intrusive Suite Terra Nova Intrusive Itaporanga Intrusive Suite  
NE-SW / E-W trending elongated ridges  
Homoclinal sedimentary plateau  
Betânia sedimentary plateau  
Tacaratu Formation  
Source: Serviço Geológico do Brasil (2014)  
4
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
The Pajeú Intermontane Depression corresponds to a strip of NE-SW elongated lowlands, confined  
between the Remobilized Massifs of the Transversal Zone Domain and the Western Escarpment of the  
Borborema Highlands (Corrêa et al., 2010). The Riacho Grande basin is installed on this low-lying flat  
compartment, structured in metamorphic complexes and Neoproterozoic granite plutons, mostly covered by  
the xerophytic thorn-scrub vegetation of the caatinga. The lowlands are transversed by mylonitic ridges  
subordinated to the structural controls of the NE-SW and E-W trending Neoproterozoic Shear Zones, where  
some sections of the larger channels are superimposed (Almeida et al., 1967; Sial, 1984; Silva Filho et al.,  
1987; Silva Filho e Guimarães, 1990).  
Fig. 2 – Geology of the Riacho Grande basin and its surroundings.  
Fig. 2 – Geologia da bacia do Riacho Grande e arredores.  
Source: Serviço Geológico do Brasil (2014)  
The climatic and geological characteristics of the region significantly influence soil development, as  
highlighted by Corrêa et al. (2014). In the semi-arid Northeast of Brazil, the soils demonstrate a denudational  
balance that tends to prioritize erosion over pedogenesis. This process results in a distribution of soil classes  
that is primarily governed by lithological controls, geomorphic compartmentalization, and land use types.  
Within this framework, the Fluvisols present in the Riacho Grande basin are noteworthy; these soils are  
formed from recent alluvial deposits found in river plains and their associated terraces.  
Additionally, the presence of Leptosols, which are shallow soils containing gravel, and Arenosols,  
characterized by sandy textures that are highly susceptible to erosion, is significant. The Arenosols exhibit a  
high infiltration capacity and notably low clay content.  
Planosols are another class of greater recurrence in the Riacho Grande basin. They exhibit light-  
colored horizons and abrupt changes in texture, are shallow, have low permeability, and are more susceptible  
to erosion processes (Almeida, 2015; FAO, 2014; Oliveira, 2016), especially when related to the intensity of  
human activities in the sectors close to the terraces and riverbeds.  
In these regions, Fluvisols and Planosols are the dominant types found at the interface between the  
alluvial plains and the adjacent rocky pediments, which delineate the lateral boundaries of the alluvial  
domain. Within this geoenvironmental unit, a range of agricultural practices is undertaken, including cattle  
ranching and dryland farming, particularly by smallholder farmers.  
The pediments cover a large part of the Riacho Grande basin, alternating areas with preserved  
vegetation cover and areas under agricultural activities closer to the main channel. These are overall level  
5
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
surfaces with a ramp morphology, occurring between 450 and 550 meters (Almeida et al., 2016). These  
compartments are primarily structured in the sequences of metamorphosed metasedimentary rocks of the São  
Caetano Complex (SGB, 2001) to the north of the Afogados da Ingazeira Shear Zone and in the orthogneisses  
of the Floresta Complex. Leptosols and Luvisols predominate on the pediment ramps, while Planosols occur  
in the fluvial plains.  
The agricultural activities carried out in the areas of contact between the pediment and the alluvial  
plains are those aimed at subsistence, carried out on small family properties, which take advantage of areas  
capable of holding soil moisture even after the short rainy season to grow short-cycle crops.  
The semi-arid nature of the region significantly influences agricultural development, necessitating the  
construction of small-scale dams and the drilling of shallow wells. The prevalence of these rudimentary dams  
is closely associated with the Fissural Hydrogeological Domain, characterized by crystalline rock formations.  
In this domain, water storage is primarily dictated by secondary porosity, which is manifested through  
fractures and fissures. This results in underground reservoirs that are often spatially limited, discontinuous,  
and unpredictably distributed. Consequently, the wells in this region typically exhibit low flow rates.  
Furthermore, due to inadequate water circulation, elevated rates of evapotranspiration, and the specific  
characteristics of the bedrock, the water is frequently prone to salinization (Ministério de Minas e Energia  
[MME], 2009).  
The Betânia homoclinal sedimentary plateau is characterized by a continuous cover of caatinga  
vegetation, which marks its distinctive landscape unit within the basin. This region is notable for its  
asymmetric ridges, featuring slopes exceeding 15°, and is further defined by dip-slip slopes that are dissected  
by canyons and steep valleys. The morphological characteristics observed in the area are largely attributed  
to the adaptation of the drainage network to the predominant psammite-psephitic lithotypes, which exhibit  
significant diagenesis and sub-vertical fracturing.  
In this landscape unit (fig. 3), aggradational areas are characterized by alluvial plains presenting  
sediments of sandy, clayey, and gravelly textures. In contrast, sandy eluvial-colluvial sediments occur at the  
foot of the elevations. Prevailing soil classes in this landscape unit are Leptosols, rocky outcrops on the higher  
hillslopes, and Arenosols at the foot of the slopes. Associations with Acrisols were also observed to a lesser  
extent.  
Fig. 3 – Landscape units of Riacho Grande basin  
Fig. 3 – Unidades de Paisagem da bacia do Riacho Grande.  
Source: Almeida et al. (2025)  
6
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
3.  
FLUVIAL COMPARTIMENTS AND TYPOLOGIES  
To comprehend the fluvial dynamics within a semi-arid environment, a detailed analysis of the  
channels in the Riacho Grande basin was conducted, employing the River Styles framework established by  
Brierley and Fryirs (2005). The analysis commenced with an exploration of fluvial compartmentalization, a  
concept that reflects the regional influences on channel morphology and highlights the prevailing surface  
processes within the landscape framework.  
This approach categorizes the channels based on the degree of valley confinement, further subdividing  
them according to shared characteristics regarding the distribution of floodplain deposits along their lengths.  
Specifically, confined valleys are identified as those that either lack floodplains entirely or exhibit them  
sporadically, characterized by unilateral overflow. In contrast, partially confined valleys display  
discontinuous floodplains throughout the majority of their stretches. Finally, laterally unconfined valleys are  
distinguished by the presence of bilateral overflow deposits and the continuous development of alluvial  
plains.  
A longitudinal profile of the main channel has been constructed (fig. 4), delineating the various river  
compartments within the Riacho Grande Basin. In the section of the profile up to an elevation of 530 meters,  
a predominantly erosive behavior is observed, which is characteristic of confined valley systems.  
Conversely, downstream of this elevation, the profile becomes increasingly smoother, indicating a  
transition to depositional processes. This shift is reflected in the landscape through laterally unconfined  
valleys, which are influenced by features that disrupt sediment transfer within the channel. These disruptions  
may be attributed to both geological structures and anthropogenic interventions, leading to the formation of  
zones of sediment storage.  
Between 500 and 450 meters, the river dynamics combine erosive and depositional processes. In this  
section, the channel is partially confined and is characterized as a sediment transfer zone. In this segment,  
the knickpoints record the existence of structural controls on the geometry of the channel, characterized by a  
sequence of rocky sills along the riverbed. Then, the profile becomes smoother again, evidencing a  
resumption of depositional processes close to its mouth.  
Fig. 4 – Longitudinal profile of the Riacho Grande (A). Main channel of the Riacho Grande and its compartmentalization (B).  
Fig. 4 – Perfil longitudinal do Riacho Grande (A). Canal principal do Riacho Grande e a sua compartimentação (B).  
Source: Authors  
7
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
In order to elucidate aspects of the drainage dynamics and behavior, the channels were subdivided into  
segments, defining typologies that translate the landscape context in which they are inserted on a local scale.  
Thus, considering the landscape units, the river compartmentalization, and the local geomorphological  
characteristics, seven channel typologies were defined in the Riacho Grande Basin (fig. 5): rocky confined  
channels; rocky confined channels with discontinuous floodplains; sandy confined channels with  
discontinuous floodplains; low sinuosity channels with discontinuous floodplains; channeled valley with  
filling; filled valleys; and filled valleys in homoclinal morphostructure.  
Fig. 5 – Fluvial typologies in the Riacho Grande basin.  
Fig. 5 – Tipologias fluviais na bacia do Riacho Grande.  
Source: Opentopography, Copernicus (2025)  
3.1. Confined pattern  
The confined valleys within the Riacho Grande Basin are generally devoid of floodplains, or, when  
present, these features are limited in both spatial extent and frequency. Lithological and structural controls,  
including fractures and mylonitic foliation, significantly influence the morphological characteristics of these  
valleys. The topography leads to the formation of single, continuous, low-order channels predominantly  
shaped by erosional processes. These channels exhibit low sinuosity and medium to high slopes in  
longitudinal and lateral profiles. Based on their distinct characteristics and behavior, these channels can be  
classified into three primary typologies: rocky confined channels, rocky confined channels with  
discontinuous floodplains, and sandy confined channels with discontinuous floodplains.  
With low incidence in the Riacho Grande basin, channels of this type have stable banks and steep  
slopes, with direct contact between the bed and the rocky substrate (fig. 6). Erosion and transport predominate  
in their evolution. They are located over sediment source and transfer areas, with punctual deposition  
characterized by the development of small pockets of sediment retained upstream of rocky sills or at the  
confluence of tributaries. These deposits are subject to reworking and evacuation during high-magnitude  
rainfall events. The distribution of artificial dams also contributes to the genesis of these depositional features  
8
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
During extended drought periods, river channels exhibit a lack of flow, which unveils the presence of  
gradient disruptions and a sequence of rifles and pools. Upon the resumption of flow, the ensuing torrents  
exhibit both high capacity and competence, serving as a source area for the downstream segments. This  
particular typology is characterized by minimal anthropogenic influence along its course, featuring dense  
shrubby caatinga vegetation. In this context, human interventions are typically localized, manifesting as the  
construction of rustic dams and the intersection of channels by unpaved roads.  
Fig. 6 – (A) Segment of a rocky confined channel, (B) land use, (C) lateral and longitudinal profiles highlighted (point 1), (D)  
the upper detail on the right refers to sediments trapped near the confluence, where (A) represents the flow direction and (A)  
the confluence.  
Fig. 6 – Segmento de canal confinado rochoso, (B) uso da terra, (C) destaque para perfis longitudinal e lateral (ponto 1),  
(D) o detalhe superior à direita refere-se aos sedimentos aprisionados perto da confluência, onde (A) representa a direção  
do fluxo e (B) a confluência.  
Source: Authors. Photography: Joana Almeida, 2019.  
In the Riacho Grande basin, rocky confined channels with discontinuous floodplains are prominent  
features characterized by single, continuous channels that exhibit rocky beds, with floodplains typically  
confined to one side. These channels are situated in transitional zones where there is a gradient in sediment  
transfer capacity, ranging from high to low.  
The channels are typically entrenched and possess asymmetric margins, which display varying degrees  
of resistance that influence their lateral adjustment. This category of confined channels is widespread  
throughout the Riacho Grande basin, distinguished by an average sinuosity in regions that are predominantly  
subject to erosion and sediment transport. In certain wider segments, occasional floodplains develop in  
response to episodic flash floods (fig. 7).  
Among the geomorphic units in this typology, lateral bars, floodplains, and riffle-and-pool sequences  
predominate. Depositional processes occur through flooding on gentle convex banks, while concave and  
steep banks remain controlled by lithology. In planform, these channels become wider downstream,  
evidencing a transitional behavior towards a predominance of depositional features. These, in turn, occur as  
temporary accumulation zones, composed mainly of gravelly- sandy sediments, reworked during high-flow  
episodes.  
9
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
In the Riacho Grande basin, this typology is mainly associated with the dissected pediments landscape  
compartment. In addition to structural controls, human interventions influence river behavior in this sector.  
Small rural settlements are located directly around the channels, with short- cycle crops and animal husbandry  
on slopes with eluvial cover. Due to the traditional agricultural activities, the presence and construction of  
dams and rustic reservoirs temporarily interrupt the longitudinal connection along the channels. The same  
occurs with the interposition of unpaved rural roads and the Transnordestina railway works, which remobilize  
sediments from the hillsides to the channels. During the long dry season, sediments remain trapped until the  
arrival of the first torrential episodes in late summer.  
Fig. 7 – (A) Rocky confined channel with discontinuous floodplain, (B) land use, (C) longitudinal and lateral profiles  
highlighted (Point 2). (D) The image in the upper right corner refers to the deposition of a pocket plain in a bedrock channel,  
where (A) represents rupture and (B) pocket-plain sediment deposition, while the red arrow indicates flow direction.  
Fig. 7 – (A) Canal rochoso confinado com planície de inundação descontínua, (B) uso da terra, (C) perfis longitudinais e  
laterais destacados (Ponto 2). (D) A imagem no canto superior direito refere-se à deposição de uma planície de inundação  
em um canal rochoso, onde (A) representa a ruptura e (B) a deposição de sedimentos na planície de inundação, enquanto a  
seta vermelha indica a direção do fluxo.  
Source: Authors. Photography: Joana Almeida, 2014  
The sandy confined channels with discontinuous floodplains represent the most prevalent subtype  
within the confined channels category (fig. 8). These channels are characterized by single, continuous  
channels, with a substrate formed by alluvial deposits that overlay the dissected surface of rocky pediments.  
Rocky outcrops are frequently found within the channel, contributing to the banks' structural resistance.  
These outcrops are linked to more resistant lithologies that influence the flow dynamics.  
As a result, sediment deposition occurs upstream of these rocky formations, forming pocket plains  
embedded within alveoli, which are separated by segments of straight, confined channels. The banks exhibit  
asymmetry, characterized by the accumulation of lateral bars, shallow floodplains on one side, and steep,  
more resistant rocky banks on the other.  
The segments under analysis stand out due to the predominance of bed incision and thalweg  
entrenchment over erosion processes on the banks, as observed in the cross-section profiles. The greater  
resistance of the banks limits the adjustment capacity and lateral migration of the channel, restricting the  
sediment accommodation spaces to specific sectors of the river where structural controls, such as the  
10  
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
intersections of fractures of different directions, allow the widening of the valley (alveoli), as verified in  
planform through the arrangement of depositional features in sections where the channel presents inflections.  
Longitudinally, these segments occur adjacent to partially confined channels, contributing as source  
and transfer areas for sediments during high-magnitude torrential events. Regarding land use and land cover,  
the sectors of the Riacho Grande basin under this typology present low levels of human intervention, except  
for rustic dams and unpaved roads.  
Fig. 8 – (A) Sandy confined channel with discontinuous floodplain, (B) land use, (C) highlighting longitudinal and lateral  
profiles (Point 3). In the below right corner, an entrenched channel in sandy bed, where (D) represents channel incision in  
2014 and channel filling in 2019. The red marker indicates a rocky sill.  
Fig. 8 – (A) Canal confinado arenoso com planície de inundação descontínua, (B) uso da terra, (C) destacando perfis  
longitudinais e laterais (Ponto 3). No canto inferior direito, um canal entrincheirado em leito arenoso, onde (D) representa a  
incisão do canal em 2014 e o preenchimento do canal em 2019. O marcador vermelho indica uma soleira rochosa.  
Source: Authors. Photography: Joana Almeida, 2014; 2019.  
3.2. Partially confined  
Partially confined valleys were identified according to their character and fluvial behavior, with low  
sinuosity channels and discontinuous floodplains. They are commonly located downstream of confined  
valleys and stand out as sediment transfer zones. In general, they are quite representative in the study area,  
especially along the main channel of the Riacho Grande. They constitute transitional typologies characterized  
by a combination of erosion and depositional processes.  
In specific segments, depositional dynamics dominate (fig. 9), leading to pronounced accumulation  
morphologies, such as point bars and floodplains. The valleys formed in this context tend to be broad and  
contain discontinuous channels that operate under low energy conditions, displaying reduced competence.  
The deposition of silty-sandy materials prevails both in the channel bed and along the banks. This  
geomorphological section demonstrates a moderate to high capacity for adjustment, as lateral channel  
migration occurs due to erosional processes impacting the concave banks and sediment accumulation over  
the convex banks. Additionally, the influence of overflow deposition during flooding events further  
contributes to accretional physiognomies.  
11  
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
Fig. 9 – (A) Low sinuosity channel with discontinuous floodplain, (B) land use, (C) the longitudinal and lateral profiles of the  
section (Point 4), (D) in the upper right corner, a low sinuosity channel, where (A) represents the lateral deposition of  
sediments on the convex bank, with adjacent overflow, while (B) represents a pool adjacent to the rocky sill (indicated by the  
red marker) and a longitudinal bar downstream.  
Fig. 9 – (A) Canal de baixa sinuosidade com planície de inundação descontínua, (B) uso da terra, (C) perfis longitudinal e  
lateral da seção (Ponto 4), (D) no canto superior direito, um canal de baixa sinuosidade, onde (A) representa a deposição  
lateral de sedimentos na margem convexa, com transbordamento adjacente, enquanto (B) representa uma poça adjacente à  
soleira rochosa (indicada pelo marcador vermelho) e uma barra longitudinal a jusante.  
Source: Authors. Photography: Joana Almeida, 2015.  
The upstream sectors of the laterally unconfined channels are located on hillslopes with eluvial cover,  
where agricultural activities intensify human interventions in sediment pockets and flat floodplain areas.  
Agricultural practices also contribute to sediment remobilization from the banks to the channel bed. The most  
representative stretch of this typology refers to the main channel of the Riacho Grande, which is especially  
impacted by the construction of dams for water impoundment. Human aggradational morphologies develop  
upstream of such dams.  
3.3. Laterally unconfined  
Laterally unconfined valleys are prevalent in the low-slope sectors of the Riacho Grande Basin,  
characterized by a predominance of aggradational forms. Channels in this typology exhibit significant  
capacity for both lateral and vertical adjustment, resulting in broad, shallow, and bilaterally symmetrical  
floodplains.  
In many instances, the landscape features discontinuous incisions of single or multiple shallow  
channels; however, in most scenarios’ channels are frequently absent. This cut-and-fill channel pattern is a  
defining characteristic of the alluvial river segments found in the semi-arid Northeast (Lima et al., 2021;  
Mabesoone, 1981). As a result, the fluvial landscape is dominated by unchanneled depositional sectors,  
particularly observed in the vicinity of confluences.  
These segments have a high incidence of human interventions, mainly focused on agricultural  
activities, in addition to the implementation of dams for flow containment and water storage. These dams,  
typical of the drylands of the Northeast, influence the distribution of sediments along the channel, establishing  
12  
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
upstream, extensive floodplains. Considering these local particularities of each planform section, the laterally  
unconfined valleys were subdivided into channeled-filled valleys, filled valleys, and filled valleys in  
homoclinal morphostructure.  
The segment depicted in figure 10 pertains to Varzinha Creek, which exhibits gentle slopes and a  
longitudinal equilibrium profile. This indicates significant energy dissipation and highlights the prevalence  
of depositional processes within the creek's dynamics.  
Fig. 10 – (A) Channeled filled valley, (B) land use, (C) lateral and longitudinal profiles of the section (Point 6), (D) in the  
upper right corner, a section of channeled filling in the Varzinha Creek, where (A) represents the Flood Plain and (B) the  
Sandy Lateral Bar, while the red arrow represents the flow direction.  
Fig. 10 – (A) Vale preenchido canalizado, (B) uso da terra, (C) perfis lateral e longitudinal da seção (Ponto 6), (D) no canto  
superior direito, uma secção de preenchimento canalizado no Riacho Varzinha, onde (A) representa a Planície de Inundação  
e (B) a Barra Lateral Arenosa, enquanto a seta vermelha representa a direção do fluxo.  
Source: Authors. Photography: Joana Almeida, 2019.  
As a result, the formation of point bars and adjacent marginal dikes along the alluvial plain is evident.  
Point bars develop as sandy sediments accumulate on banks that flank rocky outcrops and boulders. These  
formations are closely associated with litho-structural controls, which are influenced by the intersection of  
NE-SW and NW-SE lineaments, as illustrated in figure 11.  
These controls are manifest in the planform through abrupt inflections in the drainage pattern. Notably,  
during the dry season, certain areas within this section remain inundated, while in the rainy season, the flow  
reaches elevations that surpass the level of the alluvial plain, resulting in the reworking and deposition of  
sediments throughout the valley  
This section is approximately 8.5km long, with erosive process predominating up to an elevation of  
445km. This behavior is associated with the interposition of an artificial base level resulting from a dam built  
upstream of the segment. The difference in altitude between the base levels causes the erosive processes to  
recur and channel dissection to resume. As the flow progress, aggradational morphologies appear in the  
middle of the channel.  
13  
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
Fig. 11 – Point bar adjacent to a rock outcrop. A – sandy point bar.  
Fig. 11 – Barra em pontal adjacente a soleira rochosa. A – barra em pontal arenosa.  
Source: Authors. Photography: Joana Almeida, 2019.  
The sections classified as filled valleys (fig. 12) are wide, flat, low-sinuosity, sediment-filled, and  
preserved alluvial valleys with no channeled flow. They are located at the valley bottoms with low lateral  
and longitudinal slopes, reflected in the flow's low capacity and competence, with a predominance of  
aggradational processes. They are configured as low-energy fluvial units, with a predominance of  
depositional morphologies, especially in the middle of the channel, associated with spasmodic overflow  
events, which, according to Brierley and Fryirs (2005), construct temporary morphologies within the bed  
materials.  
Fig. 12 – (A) Unchanneled filled valley, (B) land use, (C) longitudinal and lateral profiles of the section (Point 5). (D) In the  
upper right corner is a mid-channel morphology, where (A) refers to the longitudinal bar, and the red arrow indicates the flow  
direction.  
Fig. 12 – (A) Vale preenchido não canalizado, (B) uso da terra, (C) os perfis longitudinal e lateral da seção (Ponto 5). (D)  
No canto superior direito, há uma morfologia do meio do canal, onde (A) se refere à barra longitudinal e a seta vermelha  
indica a direção do fluxo.  
Source: Authors. Photography: Joana Almeida, 2019.  
14  
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
In this typology, discontinuous ravines and small ponds may be frequent, which are associated with  
low-flow stages, where the flow is limited to depressions or small incisions in the alluvial surface, with the  
accumulation of suspended sediments. During periods of higher flow, the valley is entirely covered by a sheet  
of water. At this time, sediments are remobilized and rapidly deposited as the flow energy is dissipated  
downstream (fig. 13), resulting in the formation of floodouts.  
Fig. 13 – Filled valley. A – Dry period (2015). B – Following the rainny season (2019).  
Fig. 13 – Vale preenchido. A – Período de seca (2015). B – Após o período chuvoso (2019).  
Source: Authors. Photography: Joana Almeida. A) 2015 B) 2019.  
Brierley and Fryirs (2013) define floodouts as geomorphic units that are associated with depositional  
sectors within flood-prone areas. These features arise from the intersection of a discontinuous channel that,  
influenced by changes in base level, transports sediments downstream into a valley surface that shows little  
to no incision. The resulting sedimentary deposits typically exhibit a fan-like morphology, primarily  
composed of bedload materials. However, the low gradient of the channeled flow allows for the deposition  
of finer materials as well, due to the dissipation of energy.  
According to the authors, these sedimentary flood lobes, referred to as floodouts, distribute themselves  
over a relatively flat surface characterized by slightly convex edges, predominantly filling the lower  
elevations of the valley bottom.The filled valleys are located in different sectors of the Riacho Grande Basin,  
usually adjacent to partially confined sections or filled valleys with dominant structural controls.  
These areas function as storage basins (sinks) for sediments from the main channel and tributaries,  
trapping sediments between confluences and promoting river disconnection in the channel-channel and  
channel-tributary relationship. In these areas, there is an intensification of human activities, both on the banks  
and in the middle of the channel, with the practice of agriculture, which intensifies erosion processes.  
Installing open wells (locally known as cacimbas) is common to take advantage of the water storage in the  
alluvial aquifers.  
Also noteworthy in the Riacho Grande Basin are the filled valleys under the morphostructural  
influence of the Betânia homoclinal plateau (Corrêa et al., 2024), located on the dip-slip slope of the residual  
landforms, here named "filled valley in homoclinal structure".  
These valleys have hollow-shaped headwaters, where surface flows converge, filling the adjacent  
accommodation spaces with sandy sediments from the weathering of the Tacaratu Formation (Siluro-  
Devonian), forming extensive alluvial plains (fig. 14). This configuration is evident in the analysis of the  
longitudinal profile of the highlighted section, where the river presents erosive behavior above 700m under  
a high gradient, with the gradual smoothing of the longitudinal profile below 650m, indicating the beginning  
of the accumulation zone.  
This typology is characterized by irregular valleys with asymmetrical cross-sectional profiles that  
widen downstream. Their capacity for lateral adjustment is limited due to the lithostructural controls of the  
silicified sandstones of the Tacaratu Formation. The alluvial plains differ from the other typologies by the  
abundance of gravel and coarse sand, which attest to the proximity and control of the source area (fig. 15).  
15  
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
Fig. 14 – Drainage headwaters (Point 7 in Fig. 5). A – Sediment storage in adjacent alluvial plain.  
Fig. 14 – Cabeceiras de drenagem (Ponto 7 na Fig. 5). A – Estocagem de sedimentos em planície aluvial adjacente.  
Source: Authors. Photography: Joana Almeida, 2019.  
Fig. 15 – (A) Valley filled in Homoclinal Morphostructure, (B) land use, (C) the lateral and longitudinal profiles of the  
section (Point 7), (D) in the upper right corner, there is an alluvial plain, while the red arrow indicates the flow direction.  
Fig. 15 – (A) Vale preenchido em Morfoestrutura Homoclinal, (B) uso da terra, (C) perfis lateral e longitudinal da secção  
(Ponto 7), (D) no canto superior direito, há uma planície aluvial, enquanto a seta vermelha indica a direção do fluxo.  
Source: Authors. Photography: Joana Almeida, 2019.  
These segments are characterized, in terms of land use and land cover, by the low incidence of human  
activities, with interventions restricted to the channel through extensive goat farming. In contrast, the  
hillslopes are covered by preserved shrubby caatinga. The thick layers of sand that fill the accommodation  
spaces of the valley bottoms concentrate most of the open wells (cacimbas), with depths that vary between 3  
and 7 meters, helping to maintain traditional agricultural practices.  
The analysis of landscape compartments and river typologies enabled us to establish a preliminary  
understanding of the river dynamics in the Riacho Grande Basin, resulting in an initial guide to the diversity  
16  
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
of semi-arid river systems in Northeastern Brazil and their relationship with the surrounding landscape  
context. This type of morphological integration approach facilitates the interpretation of sediment production  
and accumulation processes in the various sectors of a basin. Table II presents a summary of the  
characteristics and behavior of the river typologies identified in the Riacho Grande Basin.  
Table II – Fluvial Typologies in the Riacho Grande basin.  
Quadro II – Tipologias Fluviais na bacia do Riacho Grande.  
Characteristics  
River Style  
Adjustment capacity  
Bed  
material  
Channel in Planform  
Geomorphic Units  
Land use  
Limited. Coarse  
sediments  
remobilization during  
floods  
Single, straight,  
continuous, confined  
Gravelly-sandy side bar  
and pocket floodplain  
Native vegetation  
(shrubby caatinga)  
Rocky confined  
Rocky  
Rocky  
Native vegetation  
Rocky confined with  
Single, continuous, low  
discontinuous floodplain sinuosity, confined  
Side bar, discontinuous  
pocket floodplain  
(shrubby caatinga), bare Limited to depositional  
soil and urban  
aglomerate  
sectors  
Sandy side bar,  
discontinuous pocket  
floodplain  
Native vegetation  
(shrubby caatinga), bare limited to punctual  
soil  
Channel incision,  
Sandy confined with  
discontinuous floodplain sinuosity, confined  
Single, continuous, low  
Sandy  
Sandy  
sectors.  
Low sinuosity channel  
with discontinuous  
floodplain  
Single, continuous, low  
sinuosity, partly  
confined  
Point bar, sequence of  
rocky rifles and pools,  
discontinuous floodplains  
Native vegetation  
(shrubby caatinga), bare  
soil  
Moderate to high,  
overflow.  
Filled valley with  
continuous channelized  
flow, laterally  
Native vegetation  
(shrubby caatinga), bare High, cut and fill  
soil  
Continuous floodplain,  
point bar, marginal dyke  
Sandy and  
silty-sandy  
Filled channelized  
unconfined  
Alluvial plain,  
Native vegetation  
Filled valley, laterally  
unconfined  
Filled Valley  
longitudinal bar, rifle and Silty-sandy (shrubby caatinga), bare High, cut and fill  
pool sequences, floodout  
Alluvial plain, side bar  
Source: Authors  
soil  
Filled valley in  
homoclinal  
morphostructure  
Filled unchanneled  
valley, laterally  
unconfined  
Native vegetation  
(shrubby caatinga), bare  
soil  
Limited by structural  
controls  
Sandy  
Anthropogenic changes generate direct or indirect impacts on river configuration, altering flow  
interactions between slopes and the channel itself and tributaries, promoting the development of pleasant  
features. Thus, areas of preserved native vegetation predominate in the Riacho Grande basin. Areas under  
dense shrubby caatinga, located on slopes and dissected fronts with detrital cover, occupy the largest area of  
the basin, playing a significant role in soil stabilization against erosion.  
4.  
FINAL CONSIDERATIONS  
The recognition of regional controls affecting the physical characteristics and geomorphological  
processes in small river basins has led to the development of models that yield efficient and viable systemic  
products for environmental and territorial planning and management, particularly in the context of the  
complexity of landscapes in dryland regions. From this perspective, the theoretical-methodological proposal  
of River Styles provided the basis for the compartmentalization and definition of fluvial typologies,  
considering the dominant processes and associated morphologies in order to understand their evolution.  
To apply the methodology, it was necessary to understand the interactions between water flow,  
sediments, and vegetation cover, as well as the behavior of the climate and the anthropogenic impacts that  
shape these interactions. Thus, the study of the fluvial configuration of a low-order ephemeral basin in the  
semi-arid Northeast of Brazil, the Riacho Grande basin, allowed for the identification of seven typologies,  
which highlighted the role of structural controls as a fundamental element in establishing the geometry of the  
channels and the distribution of sediment storage zones. However, the forms of land use, with a predominance  
of artificial dam construction, intensify the genesis of depositional alluvial features.  
Thus, it was possible to determine that in the semi-arid region of Northeast Brazil, as exemplified in  
the Riacho Grande Basin, compartmentalization and river typologies are direct products of the interaction  
between primary regional landscape controls (structure and lithology) and anthropic interferences, which,  
acting in consortium, promote local river diversity.  
17  
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
In short, the application of the established typological model is of great importance, as it offers a  
valuable reference for the survey, classification, and evaluation of other hydrographic basins in the Brazilian  
semi-arid domain and for comparison with other semi-arid tropical areas, where the analysis of typologies  
and their evolutionary trajectory are fundamental for recognizing the functionality of aggradational  
environments and their sustainable management.  
ACKNOWLEDGMENTS  
To the Foundation for Science and Technology Support of the State of Pernambuco – FACEPE and the  
National Council for Scientific and Technological Development – CNPq.  
ORCID  
Joana D’arc Matias de Almeida  
Antonio Carlos de Barros Corrêa  
https://orcid.org/0000-0003-0936-0451  
https://orcid.org/0000-0001-9578-7501  
Carla Suelania da Silva  
Wemerson Flávio da Silva  
https://orcid.org/0000-0002-5920-867X  
https://orcid.org/0000-0002-7439-9443  
AUTHOR’S CONTRIBUTIONS  
Joana D’arc Matias de Almeida: Conceptualization, Methodology, Validation, Investigation, Resources,  
Writing – original draft preparation, Visualization, Project administration, Funding acquisition. Antonio Carlos  
de Barros Corrêa: Conceptualization, Methodology, Validation, Investigation, Resources, Writing – review and  
editing, Supervision, Project administration, Funding acquisition. Carla Suelania da Silva: Validation,  
Investigation, Writing – original draft preparation. Wemerson Flávio da Silva: Validation, Investigation.  
Writing - review and editing.  
REFERENCES  
Almeida, F. F. M., Leonardos, O. H., & Valença, J. (1967). Review on granitic rocks of Northeast South America. IUGS.  
Almeida, J. D. M. (2021). Dinâmica Fluvial no sertão central pernambucano: morfogênese dos plainos aluviais na bacia do  
Riacho Grande [Fluvial Dynamics in the central sertão of pernambuco: morphogenesis of the alluvial plains in the  
Riacho Grande basin]. [Tese de doutoramento, Universidade Federal de Pernambuco]. Repositório Digital da  
Universidade Federal de Pernambuco. https://repositorio.ufpe.br/handle/123456789/40448  
Almeida, J. D. M. (2017). (Des)conectividade da paisagem e compartimentação fluvial na Bacia do Riacho Grande, Sertão  
Central pernambucano [(Dis)connectivity of the landscape and fluvial compartmentalization in the Riacho Grande  
Basin, Central Sertão of Pernambuco]. [Dissertação de mestrado, Universidade Federal de Pernambuco]. Repositório  
Digital da Universidade Federal de Pernambuco. https://repositorio.ufpe.br/handle/123456789/28988  
Almeida, J. D. M. (2015) Dinâmica e Caracterização Fluvial da Bacia do Riacho Grande: Abordagem da Conectividade da  
Paisagem [Fluvial Dynamics and Characterization of the Riacho Grande Basin: A Landscape Connectivity  
Approach]. [Monografia de graduação, Universidade Federal de Pernambuco]  
Almeida, J. D. M., Corrêa, A. C. B., & Souza, J. O. P. (2016). (Des)Conectividade da Paisagem em Ambiente Semiárido:  
Bacia do Riacho Grande, Sertão Central Pernambucano [(Dis)Connectivity of the Landscape in a Semi-arid  
Environment: Riacho Grande Basin, Central Sertão of Pernambuco]. In F. L. R. Listo, D. Mützenberg, & B. A. C.  
Tavares (Eds.), E-book do I Workshop de Geomorfologia e Geoarqueologia do Nordeste (pp. 9-18). GEQUA.  
Almeida, J. D. M., Lima, D., Franzen, M., Lima, E. A. M., & Costa, F. A. (2012, outubro). Abastecimento público de água no  
Sertão de Alagoas e Pernambuco. [Poster] [Public water supply in the Sertão region of Alagoas and Pernambuco]. IV  
Workshop de Mudanças Climáticas e Recursos Hídricos do Estado de Pernambuco [IV Workshop on Climate Change  
and Water Resources in the State of Pernambuco], Recife, Brasil.  
Almeida, J. D. M., Corrêa, A. C. de B., & Barros, A. C. M. (2025). Semi-arid river dynamics from the internal geometry of  
river deposits. Geographical Research, 63(4), 553-572. https://doi.org/10.1111/1745-5871.70027  
Alves, J. M. B., Silva, E. M., Sombra, S. S., Barbosa, A. C. B., Santos, A. C. S., & Lira, M. A. T. (2017). Eventos Extremos  
Diários de Chuva no Nordeste do Brasil e Características Atmosféricas [Extreme Daily Rainfall Events in Northeast  
Brazil and Atmospheric Characteristics]. Revista Brasileira de Meteorologia, 32(2), 227-233.  
https://doi.org/10.1590/0102-77863220012  
18  
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
Aragão, J. O. R. (1998, outubro). A previsão da precipitação no norte do Nordeste do Brasil para o período chuvoso de  
fevereiro a maio: os anos 1997/98. [Poster] [Precipitation forecast for the northern Northeast of Brazil for the rainy  
season from February to May: the years 1997/98]. 10º Congresso Brasileiro de Meteorologia e 8º Congresso da  
Flismet [10th Brazilian Congress of Meteorology and 8th FLISMET Congress], Brasília, Brasil.  
Barros, A. C. M. (2018). Tipologia e dinâmica de paisagens não canalizadas no nordeste semiárido. [Typology and  
dynamics of unchanneled landscapes in the semi-arid northeast]. [Tese de doutoramento, Universidade Federal de  
Pernambuco]. Repositório Digital da Universidade Federal de Pernambuco.  
https://repositorio.ufpe.br/handle/123456789/33415  
Bracken, L. J., & Wainwright, J. (2008). Equilibrium in the balance? Implications for landscape evolution from dryland  
environments. In K. Gallagher, S. Jones, & J. Wainwright (Eds.), Landscape Evolution: Temporal and Spatial Scales  
of Denudation, Climate and Tectonics (pp. 29-46). Geological Society.  
Brierley, G. J., & Fryirs, K. (2013). Geomorphic Analysis of River Systems: An Approach to Reading the Landscape.  
Wiley- Blackwell. https://doi.org/10.1002/9781118305454  
Brierley, G., & Fryirs, K. (2005). Geomorphology and River Management: Applications of the River Styles Framework.  
Blackwell. https://doi.org/10.1002/9780470751367  
Brierley, G., Fryirs, K., Outhet, D., & Massey, C. (2002). Application of the River Styles framework as a basis for river  
management in New South Wales, Australia. Applied Geography, 22(1), 91-122. https://doi.org/10.1016/S0143-  
6228(01)00016-9  
Corrêa, A. C. B., Maciel, F., Souza, J. O. P., Azambuja, R. N., & Araújo, M. S. B. (2009). Estilos fluviais de uma bacia de  
drenagem no submédio São Francisco [River styles of a drainage basin in the lower-middle São Francisco river].  
Revista de Geografia, 26(1), 181-215.  
https://www.researchgate.net/publication/291035783_Estilos_fluviais_de_uma_bacia_de_drenagem_no_submedio_S  
ao_francisco  
Corrêa, A. C. B., Souza, J. O. P., & Cavalcanti, L. C. S. (2014). Solos do ambiente semiárido brasileiro: erosão e degradação  
a partir de uma perspectiva geomorfológica [Soils of the Brazilian semi-arid environment: erosion and degradation  
from a geomorphological perspective]. In A. J. T. Guerra, & M. C. O. Jorge (Eds.), Degradação dos solos no Brasil  
[Soil degradation in Brazil] (pp. 127-169). Bertrand Brasil.  
Corrêa, A. C. B., Tavares, B. A. C., Monteiro, K. A., Cavalcanti, L. C. S., & Lira, D. R. (2010). Megageomorfologia e  
morfoestrutura do Planalto da Borborema [Megageomorphology and morphostructure of the Borborema Plateau].  
Revista do Instituto Geológico, 31(1-2), 35-52. https://doi.org/10.5935/0100-929X.20100003  
Corrêa, A. C. B., Tavares, B. A. C., Silva, D. N. F., & Lira, D. R. (2024). Geomorphology of Pernambuco State. In V.  
Claudino-Sales, & J. F. Sobrinho (Eds.), Geomorphology of the Northeast Region of Brazil (pp. 175-204). Springer.  
https://link.springer.com/content/pdf/10.1007/978-3-031-58874-7.pdf  
Food and Agriculture Organization of the United Nations. (2015). World reference base for soil resources 2014: International  
soil classification system for naming soils and creating legends for soil maps. World Soil Resources Reports, 106.  
FAO. https://openknowledge.fao.org/server/api/core/bitstreams/bcdecec7-f45f-4dc5-beb1-97022d29fab4/content  
Franco, V. V., Lima, V. F., & Souza, J. O. P. (2022). Caracterização de Estilos Fluviais no alto e médio curso da bacia  
hidrográfica do rio Piancó, ambiente semiárido da Paraíba [Characterization of River Styles in the upper and middle  
course of the Piancó River basin, semi-arid environment of Paraíba]. Caderno de Geociências, 15, e-221506  
https://doi.org/10.9771/geocad.v15i0.44394  
Freire, J. L. M., Lima, J. R. A., & Cavalcanti, E. P. (2011). Análise de Aspectos Meteorológicos Sobre o Nordeste do Brasil  
em Anos de El Niño e La Niña [Analysis of Meteorological Aspects on the Northeast of Brazil in El Niño and La  
Niña Years]. Revista Brasileira de Geografia Física, 4(3), 429-444. https://doi.org/10.26848/rbgf.v4i3.232719  
Fryirs, K., & Brierley, G. (2009). Naturalness and place in river rehabilitation. Ecology and Society, 14(1), 20  
https://doi.org/10.5751/ES-02789-140120  
Lima, G. G., Marçal, M., Corrêa, A. C. B., & Lima, F. J. (2021). Landscape evolution of the Salamanca watershed, Araripe  
Plateau: Insights from a river channel morphological classification. Journal of South American Earth Sciences, 107.  
103013. https://doi.org/10.1016/j.jsames.2020.103013  
Lima, R. N. S., & Marçal, M. S. (2013). Avaliação da condição geomorfológica da bacia do Rio Macaé – RJ a partir da  
metodologia de classificação de Estilos Fluviais [Assessment of the geomorphological condition of the Macaé River  
basin – RJ using the River Styles classification methodology]. Revista Brasileira de Geomorfologia, 14(2), 171-179  
https://doi.org/10.20502/rbg.v14i2.317  
Mabesoone, J. M., Lobo, H. R. C., & Rolim, J. L. (1981). Ambiente semiárido do nordeste brasileiro: os rios efêmeros [The  
semi-arid environment of northeastern Brazil: the ephemeral rivers.]. Estudos Pesquisas, 4, 83-91.  
Miall, A. D. (1996). The Geology of Fluvial Deposits: Sedimentary Facies, Basin Analysis and Petroleum Geology. Springer.  
19  
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
Ministério de Minas e Energia. (2009). Relatório Técnico: análise das informações sobre os recursos hídricos subterrâneos  
no país. [Technical Report: Analysis of information on groundwater resources in the country]. Governo Federal do  
Brasil. https://www.gov.br/mme/pt-br/  
Nanson, G. C., & Croke, J. C. (1992). A genetic classification of floodplains. Geomorphology, 4(6), 459-486.  
https://doi.org/10.1016/0169-555X(92)90039-Q  
Oliveira, D. C. (2016). Detalhamento de mapeamento de solos em ambientes semiáridos. [Detailed soil mapping in semi-arid  
environments]. [Monografia de graduação, Universidade Federal da Paraíba]. Repositório Institucional da  
Universidade Federal da Paraíba. http://plone.ufpb.br/ccblg/contents/documentos/bacharelado/trabalhos-de-  
conclusao-de-curso-2016.2/diego-corte-de-oliveira.pdf/view  
Pernambuco. Secretaria de Recursos Hídricos e Saneamento. (2013). PE3D - Projeto Pernambuco Tridimensional.  
[Pernambuco Tridimensional Project]. Mapeamento do Território Pernambucano. Recife.  
PE3D:http://www.pe3d.pe.gov.br/mapa.php.  
Rodrigues, J. F., & Souza, J. O. P. (2020a). Parâmetros de controles de estilos fluviais na bacia do rio Piranhas, semiárido  
paraibano [Parameters for controlling river flow patterns in the Piranhas river basin, Paraíba semi-arid region].  
Caderno de Geografia, 30(62), 650-667. https://doi.org/10.5752/P.2318-2962.2020v30n62p650  
Rodrigues, J. F., & Souza, J. O. P. (2020b). Tipologia de canais fluviais como mecanismo de identificação da sensitividade e  
potencial de recuperação em uma bacia de drenagem no semiárido paraibano, município de São João do Tigre (PB)  
[River channel typologies as a mechanism for identifying sensitivity and recovery potential in a drainage basin in the  
semi-arid region of Paraíba, municipality of São João do Tigre (PB)]. Revista de Geociências do Nordeste, 6(2), 266-  
275. https://doi.org/10.21680/2447-3359.2020v6n2ID19772  
Rodrigues, J. M., Souza, J. O. P., Xavier, R. A., Santos, C. A. G., & Silva, R. M. (2023). Geomorphic changes in river styles  
in a typical catchment of the Brazilian semiarid region. CATENA, 232, 107423.  
https://doi.org/10.1016/j.catena.2023.107423  
Santos, W. V., Nascimento, M. C., & Barros, A. C. M. (2023). Estilos Fluviais da Bacia Hidrográfica Riacho Talhada:  
contribuições a gestão hidrogeomorfológica no semiárido alagoano [River Styles of the Talhada Stream  
Hydrographic Basin: contributions to hydrogeomorphological management in the semi-arid region of Alagoas].  
Geoambiente On-line, 47, 108-131. https://revistas.ufj.edu.br/geoambiente/article/view/75977  
Serviço Geológico do Brasil. (2014). Mapa geodiversidade do estado de Pernambuco [Geodiversity map of the state of  
Pernambuco]. SGB. https://rigeo.sgb.gov.br/handle/doc/14707  
Serviço Geológico do Brasil. (2005c). Projeto cadastro de fontes de abastecimento por água subterrânea: diagnóstico do  
município de Serra Talhada, estado de Pernambuco [Project for registering groundwater supply sources: diagnosis of  
the municipality of Serra Talhada, state of Pernambuco]. SGB/PRODEEM.  
.https://rigeo.sgb.gov.br/handle/doc/16837  
Serviço Geológico do Brasil. (2005b). Projeto cadastro de fontes de abastecimento por água subterrânea: diagnóstico do  
município de Calumbi, estado de Pernambuco [Project for registering groundwater supply sources: diagnosis of the  
municipality of Calumbi, state of Pernambuco]. SGB/PRODEEM. https://rigeo.sgb.gov.br/handle/doc/15735  
Serviço Geológico do Brasil. (2005a). Projeto cadastro de fontes de abastecimento por água subterrânea: diagnóstico do  
município de Flores, estado de Pernambuco [Project for registering groundwater supply sources: diagnosis of the  
municipality of Flores, state of Pernambuco]. SGB/PRODEEM. https://rigeo.sgb.gov.br/handle/doc/15944  
Serviço Geológico do Brasil. (2001). Programas levantamentos geológicos do Brasil: Serra Talhada, Folha SB. 24-Z-C.  
Estados de Pernambuco, Paraíba e Ceará. Escala 1:250 000 [Geological survey programs of Brazil: Serra Talhada,  
Sheet SB. 24-Z-C. States of Pernambuco, Paraíba and Ceará. Scale 1:250 000] SGB.  
https://rigeo.sgb.gov.br/handle/doc/9043  
Sial, A. N. (1984). Litogeoquímica de elementos terras raras na caracterização de granitoides no espaço Cachoeirinha,  
Nordeste do Brasil. [Lithogeochemistry of rare earth elements in the characterization of granitoids in the  
Cachoeirinha area, Northeast Brazil]. In Congresso Brasileiro de Geologia (Ed.), Anais do XXXIII Congresso  
Brasileiro de Geologia [Proceedings of the XXXIII Brazilian Congress of Geology] (pp. 2697-2709). Sociedade  
Brasileira de Geologia.  
Silva-Filho, A. F., & Guimarães, I. P. (1990). Geologia das rochas ultrapotássicas da região de Salgueiro, PE [Geology of the  
ultrapotassic rocks of the Salgueiro region, PE]. Congresso Brasileiro de Geologia (Ed.), Anais do XXXVI Congresso  
Brasileiro de Geologia [Proceedings of the XXXVI Brazilian Congress of Geology] (pp. 1752-1763). Sociedade  
Brasileira de Geologia.  
Silva-Filho, A. F., Thompson, R. N., & Leat, P. T. (1987). Petrology of Terra Nova pluton, Brazil, and associated  
ultrapotassic dykes. Revista Brasileira de Geociências.,17 (4), 481-487.  
Souza, J. O. P. (2014). Modelos de evolução da dinâmica fluvial em ambiente semiárido: bacia do açude do saco, Serra  
Talhada, Pernambuco [Models of fluvial dynamics evolution in a semi-arid environment: açude do saco basin, Serra  
Talhada, Pernambuco]. [Tese de doutorado, Universidade Federal de Pernambuco]. Repositório Digital da  
Universidade Federal de Pernambuco https://repositorio.ufpe.br/handle/123456789/11117  
20  
Almeida, J. D. M., Côrrea, A. C. B., Silva, C. S., Silva, W. F. Finisterra, LXI(131), 2026, e42870  
Souza, J. O. P., Barros A. C. M., & Corrêa, A. C. B. (2016). Estilos Fluviais num Ambiente Semiárido, Bacia do Riacho do  
Saco, Pernambuco [River Styles in a Semi-arid Environment, Riacho do Saco Basin, Pernambuco]. Finisterra –  
Revista Portuguesa de Geografia, LI (102), 3-23. https://doi.org/10.18055/Finis3737  
Whiting, P. J., & Bradley, J. B. (1993). A process-based classification system for headwater streams. Earth Surface  
Processes and Landforms, 18(7), 603-612. https://doi.org/10.1002/esp.3290180704  
Woolfe, K. J., & Balzary, J. R. (1996). Fields in the Spectrum of Channel Style. Sedimentology, 43(5), 797-805.  
https://doi.org/10.1111/j.1365-3091.1996.tb01503.x  
21