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Ethiopia): Findings from a DEM Michal Kusák1,*, Vít Vilímek2, Jozef Minár3

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Ethiopia): Findings from a DEM Michal Kusák1,*, Vít Vilímek2, Jozef Minár3 Original Article 129 Influence of neotectonics on land surface evolution in the upper part of the Blue Nile Basin (Ethiopia): findings from a DEM Michal Kusák1,*, Vít Vilímek2, Jozef Minár3 1 Institute of Rock Structure and Mechanics of the Czech Academy of Sciences, Czech Republic 2 Charles University, Faculty of Science, Department of Physical Geography and Geoecology, Czech Republic 3 Comenius University in Bratislava, Faculty of Natural Sciences, Department of Physical Geography and Geoecology, Slovak Republic * Corresponding author: [email protected] ABSTRACT The morphometric analysis of lineaments, valleys and signs of erosion taken from a digital elevation model (DEM) made it possible to not only confirm most of the conclusions of the morphotectonic development of the Blue Nile Basin from the previously pub- lished results of structural, petrological, tectonic and geochronological analyses, but also to expand our knowledge by applying several new hypotheses. The relative age of the morpholineaments of particular directions was estimated from the character of topographic profiles. Faults, lineaments and valleys are predominantly oriented in a direction compatible to the published concepts of the tectonic development of the area. Overall, the most abundant NE-SW and NNE-SSW lines reflect a change of extension from a NW-SE to WNW-ESE direction during the Pliocene, in relation to the creation and development of the Main Ethiopian Rift (MER). This is confirmed by a more developed character of the valleys and less pronounced erosion activity of the NE-SW oriented valleys contrary to the deeper narrower NNE-SSW valleys characterised by downward and headward erosion in the second direction. The most pronounced morphological manifestations of the E-W extension of the MER and western Afar during the Quaternary are confined to the borders of the MER. The directions of the Pre-Neogene rift structures to the NW-SE and WNW-ESE are compatible with the oldest elements of the current landscape and with the relict fragments of the valley network on the SE boundary of the upper Blue Nile Basin, which could have been drained across current shoulders of the MER to the S and E before the Late Miocene. KEYWORDS landscape evolution; neotectonics; river piracy; lineaments; DEM; Main Ethiopian Rift; Ethiopian Highlands Received: 17 April 2019 Accepted: 28 June 2019 Published online: 26 August 2019 Kusák, M., Vilímek, V., Minár, J. (2019): Influence of neotectonics on land surface evolution in the upper part of the Blue Nile Basin (Ethiopia): findings from a DEM. AUC Geographica 54(2), 129–151 https://doi.org/10.14712/23361980.2019.13 © 2019 The Authors. This is an open-access article distributed under the terms of the Creative Commons Attribution License (http://creativecommons.org/licenses/by/4.0). 130 Michal Kusák, Vít Vilímek, Jozef Minár 1. Introduction the upper part of the Blue Nile Basin. Lineaments are linearly arranged elements of the GaniThe et al. main 2007, objectives 2009; ofWolela this work 2010). are We to: focused 1) analyse on the morpholineaments, faults and valley networks of the Blue Nile Basin and their interrelationships; alandscape – linear potential zone of brittlesections fractures of a valley, of bedrock ridges and/ or orstraight the concentration sections of slopes – should of erosion processes be considered with anas and the geomorphological evolution, in order to determine2) study the which relation elements between are thepotential morpholineaments zones of brit- - tle fractures of bedrock and serve as concentrations mentsinfluence can on give the an geomorphological insight into landscape evolution evolution, of an for erosion processes; 3) identify areas with the most thusarea (Abdullahproviding informationet al. 2010). onAn tectonicanalysis activityof the linea over dynamic changes of valley networks. large areas, which is particularly useful for areas with Several works deal with the tectonic and volca- nic history of the upper part of the Blue Nile Basin Highlands. Recently, the lineaments are increasingly usedlimited not field only access as a surface(Ehlen 2004),expression like theof individualEthiopian faults (fracture zones) but their statistics is used also (Abebe et al. 1998; Chorowicz et al. 1998; Wolfenden paidet al. to2004; the Pikrelated et al. geomorphic 1998, 2003; development. Kieffer et al. 2004;Local morphotectonicGani et al. 2009); and however, morphodynamic less attention aspects has beenhave to define/confirm the character (directions) of the mainly been investigated (Ayalew and Yamagishi palaeomorphotectonicIn this paper we aim stress to fields understand (Minár and relations Sládek between2008; Koronovskya landforms andet al. the 2014; tectonic Šilhavý structures et al. 2016). of the - 2018).2003; Ismail Works and by Abdelsalam Gani and Abdelsalam 2012; Kusák (2006) et al. 2016; and - Mäerker et al 2016; Kycl et al. 2017; Gani and Neupne eneEthiopian and Abdelsalam Highlands, 2005; as the Gani region and Abdelsalam is strongly 2006;influ the selected aspects of geomorphic development. enced by tectonics (Kazmin 1975; Pik et al. 2003; Bey Gani et al. (2007) deal most comprehensively with Fig. 1 Map of the Blue Nile basin and adjacent area, Ethiopian Highlands. Subregions particularly analyzed in the following text: 1 – the Jemma River; 2 – Beshlo Wenz River; 3 – Volcanoes Mt. Choke and Mt. Gish; 4 – Lake Tana; 5 – Didessa River and Baro River; A – Guder River and Muger River. Influence of neotectonics on land surface evolution 131 They refuse the older idea that present physiography landscape area at a lower elevation and with gentle of the elevated plateau exists since the Oligocene (e.g. valley slopes is situated in the western part of the of incision rate of the Blue Nile initiates ca. 10 Ma ago. with a low vertical division (Figure 1). ThisPik et al. paper 2003) presents and they evidence argue from that thesatellite rapid data increase that studyThe area modern and thetopography Blue Nile of flows the area through formed the Tertia basin- - ry and Quaternary volcanism and tectonics. The uplift ing morphotectonic activity of the territory, specifying directionssupport young and space (Late impactMiocene – Quaternary) of palaeomorphotectonic increas ledof the to Ethiopianthe formation Highlands of faults (during and cracksthe last (Kazmin 29 Ma) and opening of the MER (during the last 18 Ma) has fields on the land surface development. 2. The study area: geomorphological and1975; Abdelsalam Pik et al. 2003; 2012). Beyene and Abdelsalam 2006; and geological settings GaniThe et al. plateau 2007; in Gani the easternet al. 2009; part Wolela of the study2010; areaIsmail is built by various types of Cenozoic volcanic rocks and The study area includes the Blue Nile Basin between several Cenozoic volcanoes tower above it. Erosion Lake Tana and the Roseires water reservoir by the Blue Nile and its tributaries exposed Jurassic 2) and the adjacent area (Figure 1). The and Crateceous sedimentary complexes in the valleys Blue Nile Basin consists of a large plateau that is incised into the plateau. The western part of the study inclined(175,400 km from the border of Afar and the MER (more area is built by a Precambrian crystalline complex and volcanics (Figure 2; Mangesha et al. 1996). The Ethiopian Highlands are marked by a num- than 3,000 m a.s.l.) to the W and NW (approximately- ber of faults increasing from the west to the east, bolian2,000 m Quaternary a.s.l.). Huge volcanoes Neogene areshield concentrated volcanoes towerto the SSWup to of 2,000 m Lake Tana above reach the severalplateau, hundreds and smaller of metersstrom Rift (Chorowitz 2005). The oldest Permo-Trias and Crateceous-Palaeogenewhere they border the MER – part rift systems of in the the East study African area tectono-thermal uplift of the rift shoulders and a swell - centredat most (Kiefferon the Lake et al. Tana 2004). basin Pliocene are responsible and Quaternary for the gor 2015). The main phase of extension in the MER have a NW-SE orientation (Gani et al. 2009; MacGre Ismail and Abdelsalam 2012; MacGregor 2015; Gani and the majority of fault activity occurred in the last andrecent Neupne elevation 2018). of the Uplift plateau caused (Chorowicz the rivers et al. to cut 1998; into started approximately 11 Ma (Ukstins et al. 2002)- the bedrock and divide the area by canyons and deep gor 2015). The NW-SE Late Miocene extension formed valleys with steep slopes linked to faults in the east- 5–9 Ma, and particularly in the last 1–2 Ma (MacGre NE(NNE)-trending faults (Wolfenden et al. 2004; Gani ern part of the study area (Gani et al. 2009). An older et al. 2009). E-W and NNE-SSW Quaternary extensions Fig. 2 Geological map of the Blue Nile basin and adjacent area, Ethiopian Highlands (scale 1 : 250,000; after Mangesha et al. 1996). 132 Michal Kusák, Vít Vilímek, Jozef Minár opening the MER are related to the development of mega-lineamentsand lineaments) for an analysis of the E-trending transverse faults. N-ESE- and NW-trending main directions of the landscape forming processes. extensional structures are connected with the NE-SW The faults in the Ethiopian Highlands were taken from Quaternary extension in southern Afar and the E-W the geological map of Ethiopia (scale 1 : 250,000; west of Addis Ababa, an elongated Yerer-Tullu Wellel A valley network model for the Ethiopian High- volcano-tectonicextension in western lineament Afar (Gani is probably et al. 2009). an inherent To the landsMangesha was et al.extracted 1996). from SRTM DEM by following structure, which has decoupled the Northern Ethiopi- method of Jenson and Domingue (1988) and using an Plateau and the MER as a transtensional dominant- ArcHydro tools in ArcGIS 10.2.: Fill Flow Direction ly oblique E-W to ENE-WSW structure since the Late Flow accumulation (ESRI 2015), i.e. the valley net- - Miocene (Abebe et al. 1998). sink-likework was artefacts identified caused by analysing by noise the and flow inaccuracies accumula 3.
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