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Article

Geomorphological Analysis of Xilokastro Fault, Central Gulf of Corinth, Greece

by
Sotirios Verroios
and
Vasiliki Zygouri
*
Department of Geology, University of Patras, 26504 Rion, Greece
*
Author to whom correspondence should be addressed.
Geosciences 2021, 11(12), 516; https://doi.org/10.3390/geosciences11120516
Submission received: 20 November 2021 / Revised: 7 December 2021 / Accepted: 13 December 2021 / Published: 16 December 2021
(This article belongs to the Special Issue Morphogenic Faulting: Current Practices and Future Challenges)
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Abstract

:
The Gulf of Corinth is a rapidly opening area with high seismicity associated with extensive building collapses, destruction of cities, and even the deaths of inhabitants. Rapid residential development, especially in the southern part of the Gulf of Corinth, and the construction of crucial technical infrastructures necessitate understanding the activity across crustal-scale faults that host devastating earthquakes. The evolution of landforms affected by fault action is a dominant issue in geological science. In the present study, was selected the 20 km long Xilokastro pure normal fault. In this fault, we apply eight geomorphological indices in footwall catchments that drain perpendicular to its trace. In total, more than 5000 measurements were made in 102 catchments. The determination of geomorphological indices requires the construction of morphological profiles either perpendicular to the faults or perpendicular to the main tributaries of the drainage basins under consideration through the use of the geographical information systems (ArcGIS platform). Τhe application of these indices along catchments draining the Xilokastro fault scarp show high active tectonics. Its high activity is evidenced by the high values of the length-slope index near the fault trace, the low values of the width to height ratio index, the strong asymmetry of the drainage basins, especially in the overlapping zones between its segments, and the elongated shape of the drainage basins. This study supports the idea that the application of a single morphometric index is unable to reflect the distribution of active tectonics across faults, which makes inevitable the systematic comparison of a series of tectonic morphometric indices from which a new combined index emerges (Iat). The Iat classifies the Xilokastro fault in the high degree of activity at a rate of 75% of its length.

1. Introduction

The evolution of tectonically controlled landforms and the way active tectonics of an area are imprinted has caused a great deal of research by and discussion among the scientific community [1]. Understanding the geometry of faults, the interaction between faults, and the sensitivity of river systems to tectonic movements becomes extremely important in determining the active tectonics of an area [2,3,4,5,6]. Therefore, its associated hazards, such as tectonic movements, liquefactions, and floods can be predicted as well. Fault growth, whether achieved by the joining of smaller cracks or by radial widening of a pre-existing fault, is a process with numerous stages of development, most of which cannot be detected. However, the use of geomorphological methods in areas of active tectonics, which are associated to strong seismicity, leads to conclusions and quantifies the changes in the terrain along a fault, and it can be an indication of the slip rate in an active fault.
The Gulf of Corinth (Figure 1) is a basin with the fastest extension rate in Europe [7,8,9]. The existence of many faults of normal geometry in its southern margin is “responsible” for the impressive topography in the gulf [10,11,12]. Deltaic sediments, which are currently uplifted, located on the footwall of normal faults, imply the continuous supply of the bay with sediments. The intense tectonic activity ensures conditions required for capturing tectonic movements in landforms. By this way the landforms become “able” to provide data on the tectonic evolution of an area for both short-term and long-term observation periods.
Extensive research has been conducted in the Gulf of Corinth in recent decades, covering different geological activities (e.g., [13,15,16,17,18,19,20]). Active faults in the southern margin of the Gulf of Corinth causes a combination of movements that vary from west to east [19,21]. This combination of movements consists of N-S maximum extension of 16 mm/yr and increasing elevation towards the west [19,22,23,24], reaching 1.85 mm/yr in the southwest margin [25] as is expressed by the occurrence of strong seismic events in the area [26,27,28,29,30,31,32]. The intense tectonic activity, which is concentrated mainly in the southern part of the bay, results in the creation of a high relief in the area. The stratigraphy of the Gulf consists mainly of geological formations of the Mesozoic that belong to the units of Olonos—Pindos, Tripoli, and Sub-Pelagonic. The orogenetic processes began in the Eocene [33], resulting in the creation of the Greek orogenic belt. During the final stages of orogeny, during the Neogene, several processes began, such as the formation of river basins, the accumulation of sedimentary deposits such as clays and conglomerates that gradually turn into marls [16,34,35,36,37,38,39], and submarine fans in the bottom of the Gulf [40,41,42,43]. In addition, fault activity in the southern margin of the basin raised these deposits more than 400 m above sea level, forming a succession of marine terraces that are quite extensive in the southeastern part of the Gulf [15,16,44,45,46]. The evolution of the Gulf highlights a dynamic process that changes over time [47,48,49]. The majority of researchers distinguish two stages of development. At first the Gulf formed a shallow basin where terrestrial sediments were deposited, while gradually in the second stage the Gulf achieved its current geometry by developing delta ridges within the Gulf of Corinth depocentres [13,15,16,17,18,50,51,52]. However, [53] and later [45] claim that during glacial periods the sea level decreased, resulting in the isolation of the bay and the change of sedimentation rates. The tectonic-stratigraphic evolution of the Gulf of Corinth represents the complexity of the processes found in other rift basins such as the Gulf of Suez, and for this reason despite the abundance of research work the Gulf of Corinth continues to attract the interest of geoscientists despite its age as relatively new (< 5 million years) compared to other rifts.
Tectonic geomorphology is a relatively new tool at the disposal of geoscientists, which, although initially showing only qualitative estimates, the use of innovative observation instruments gave accurate observations and the necessary quantification for modern society. It serves multiple temporal and spatial scales by examining how the horizontal and vertical deformation of the earth surface can affect the shape of hills or streams in an effort to better understand the distribution of stresses along active faults [2,6,54,55]. In Greece, systematic research in the field of tectonic geomorphology is rather limited [56,57,58,59], and the river network response associated with high tectonic activity is poorly understood [60,61,62,63]. Therefore, the question arises whether landforms that are subject to the action of both external and internal processes can evidence tectonic activity and describe the fault evolution (Figure 1). In addition, the Gulf of Corinth, showing a dense network of active normal faults that host a large number of landforms, constitutes a prominent study area as it is rather easily assessable and the structures are newly formed and thus not eroded.
The aim of this study is the detailed geomorphological analysis of the evolution of landforms in the area of Xilokastro fault, located in the central part of the Gulf of Corinth. The Xilokastro fault dominates the seismic activity of the Corinthian and is representative example of morphogenic fault associated with high slip rates. Its morphology and geometry are analyzed using geomorphic indices that indicate the influence of active tectonics in river drainage orientation and sediment distribution.

2. Geological Setting

Detailed tectonostratigraphy studies show that extensional basins are not simple geometrical structures, but evolve over time. Observations of geometry as well as the evolution of the structure of an extensional basin provide important information on large-scale lithospheric processes and the mechanical properties of faults. Despite their scientific, social, and economic significance, understanding of how extension begins and how it progresses remains limited mainly due to the few examples of active extensional basins. These are the Red Sea or the Gulf of Aden. A typical example of active extension in Europe is the Gulf of Corinth, which is an extremely new structure with a large volume of sediments and, at the same time, high seismicity rates. The Gulf of Corinth with a general orientation WNW-ESE separates the Peloponnese from central mainland Greece (Figure 1). Geodetic extension over the last 20 years shows an increase from 6 mm/yr in the east to 16 mm/yr in the west [7,24,31].
The northward movement of the African plate results in its subsidence below the Eurasian plate, with a convergence rate of 1 cm/yr [47]. The movement of the Arabian plate to the north has caused compression around the Black Sea [64], resulting in a western extrusion of Turkey in relation to the Eurasian plate. This movement is currently taking place along the dextral transfer fault of the North Anatolia, and leads gradually to the southwest movement of the East and Aegean microplate, relative to the Eurasian plate [65,66]. The modern convergence with NE-SW direction was measured to be achieved at rates of 3–5 cm/yr in the Hellenic arc ([23]; Figure 1 inset). In addition, micro-seismic studies [67] and geophysical seismic wave tomographies [68], in an attempt to trace the subsidence of the African plate, showed that the subduction angle changes gradually from mild to abrupt subsidence below the Gulf. The Gulf of Corinth is regarded to be the most active graben within the Aegean microplate (Figure 2) between the SW end of the North Anatolian fault and the dextral strike slip fault of Kefalonia [8,69,70]. It extends more than 100 km in WNW—ESE direction [19,34] while it grows at an angle in relation to the NNW extending Hellenides (Figure 1 and Figure 2), occupying a maximum width of 30 km.
The geomorphological structure between Corinth and Xilokastro is characterized as relatively mild as it forms rivers and marine terraces [16]. In this area there are no densely ruptured slopes resulting in the mild morphology of the relief [8,16,21]. These terraces cover a large area and are limited to the west by the impressive ruptured slope formed by the action of the Xilokastro fault. Its trace is located in the area southwest of the coastal city of Xilokastro. Its length reaches almost 20 km but its most impressive slope is set at 11.6 km, where in this area the fault scarp is impressive and is estimated at 0.8–1 km (Figure 2a). It is characterized by normal sense of movement in an almost W-E orientation, dipping to the north. It is composed of an onshore and an offshore part [71,72]. The offshore part, which does not exceed 6 km in length, shows, according to underwater geophysical surveys, a slope height of 580 m ([50]; Figure 2b) and is related to the deposition of modern turbidites towards the centre of the trench of The Gulf of Corinth that come from high sediment supply of rivers draining the area east of Xilokastro [71]. Its onshore part is not uniform but shows high segmentation (Figure 2b). According to [73], the Xilokastro fault is probably the boundary between the deformation that diffuses into several faults in the western part of the Gulf of Corinth and the eastern one in which the deformation is now hosted in a small number of faults that are mainly located within the offshore part of the gulf. The main phase of its activity is occurred approximately 1.5–0.7 million years ago [20,52]. Its surface trace based on extensive field work showed the existence of segments with length 500–2500 m. The western end of the fault shows larger sections of faults than the eastern one. In addition, its topographic detection (Figure 2b) decreases dramatically at the eastern end of the fault. The value of maximum topographic elevation reaches 1180 m, while the separation between the eastern and western part is evident, accompanied by a corresponding reduction in displacement. The Fonissa River flows in between the two prominent segments of the fault (Figure 2 and Figure 3). The maximum visible displacement along the fault is approximately 900 m and is located in the western part (Figure 2b). The fault footwall consists of Mesozoic limestones [74,75] in its western part, whereas in the eastern part there are elevated marine terraces (Figure 3). Surface scarps appear in the western part of the fault (Figure 3b,c,e). Curvatures are identified on these surfaces, whereas slip lines are compatible with the normal sense of motion of the fault (stereographic projections in Figure 3). The footwall of the fault is bounded by colluvial deposits that include clay formations with scattered conglomerates (Figure 3f,g). Towards the east, in its footwall Pleistocene marls and conglomerates are exposed (Figure 3h).

3. Materials and Methods

Geomorphological indices have been used systematically to evaluate active tectonic structures in various parts of the world ([58] and references therein). The structures primarily used in the geomorphological analysis are the active slopes, the river basins, and the drainage networks. Internal tectonic processes deform the Earth’s surface, whereas external processes shape the final morphological expression. Any disturbance caused by these processes alters the dynamic equilibrium of the system, which can be observed in the properties of river networks that drain tectonically active slopes [6,76,77]. In particular, river basins represent dynamic systems that can provide evidence of the formation and evolution of a tectonic structure [78,79]. The numerical representation of the topographic features is implemented through mathematical relations that can be divided into two sections (spatial and tectonic geomorphological indices), depending on the parameters of each index [80,81,82,83].
Across the orientation of the Xilokastro fault, 102 catchments were identified that dissect the fault almost perpendicularly. The main morphotectonic indices were calculated (Table 1). The runoff direction of each basin is considered to be the same as the general N-S orientation of the extension. However, there is a change in the lithology that is eroded between the eastern and western part of the fault, whereas the effect of climate is considered similar along the entire fault. The drainage network is characterized from parallel to sub-parallel, attributing its formation mainly to the fault evolution. The catchments show a variety of sizes and shapes (Figure 4). The fault is also drained from the four major catchments of the rivers Skoupeikos, Fonissa, Trikalitikos, and Katharoneri of general direction N-S whose runoff has also been affected by the action of the Xilokastro fault according to [37], forming wind and water gaps in the past.

4. Results

We examined the spatial distribution of the catchment shape factor Bs based on the calculation of the length to the width of the catchment and not its surface. The catchments can be separated in more detail, into very long ones that have values higher than 4 and are connected to high percentages of active tectonics. A second class of basins are classified as elongated with values in the interval 3–4, which indicate active tectonics, and others that are less elongated and have values lower than 3. These less elongated basins are characterized by lower active tectonics. According to this classification of [89], approximately 60% of the catchments along the Xilokastro fault (Figure 5a) show evidence of active tectonics based on their shape, which in most of them is characterized as elongated. In addition, both the catchment area elongation index RL and the circularity index of the catchment area RC prove that almost all the basins along the Xilokastro fault can be characterized as elongated to very elongated (Figure 5b,c). Therefore, the drainage of the fault footwall is mainly formed from the main branches of the basins by direct discharge of the secondary branches to the main branches, which will show high erosion capacity.
The AF catchment asymmetry index calculated at 102 catchments along the Xilokastro fault indicates a wide range of values, and for this reason its values were grouped at specified numerical intervals (Figure 6a). The classification of [89] regards values between 45 and 55 that do not show any preferred slope and are considered to grow in stable geological conditions. Values above or below this range indicate basin asymmetry either to the west (values > 55) or to the east (values < 45). Along the Xilokastro fault, the catchments are mostly considered asymmetric (Figure 6a) without, however, a uniform general tendency, a fact that is probably related to the fault segmentation. However, there are sub-trends that highlight a westward turn of the catchments located in the western part of the fault, which become even stronger towards its western boundary and obviously affects the catchments just east of Skoupeikos that are tilted to the east. Exactly the same phenomenon is observed at the natural border between the western and eastern part of the fault, Fonissa.
Therefore, both areas around the river systems of Fonissa and Skoupeikos are affected by the fault’s activity. Τhe analysis of the transverse topographic symmetry index T for all catchments along the Xilokastro fault includes the calculation of a vector that has size and orientation. The spatial distribution of these values is shown in Figure 6b, which also shows the orientation of the mean vector with a yellow arrow. As can be seen, the individual trends shown by the AF basin asymmetry index are also confirmed by the orientation of the mean vectors determined for the transverse topographic symmetry index T (Figure 6b). A characteristic example is the area around the Skoupeikos River, where strong values of asymmetric slope according to the asymmetry index AF and similar orientation of the mean vector of the index of transverse topographic symmetry T (Figure 6).
For the SL length-slope index, a density map was constructed with the aim of distinguishing the areas of the basins that show higher values of the index and therefore correspond to areas of high anomaly from the ideal elongated topographic profile of the riverbed. Areas of high anomaly in the index values are associated with high tectonic activity. According to the map of Figure 7a, the areas of high anomaly and therefore of high tectonic activity are located in the western part of the fault, mainly along its trail. Respectively, in the eastern part of the fault in the area between Fonissa and Trikalitikos there are no correspondingly high irregularities except for the fault trace that is located very close to Fonissa and showed signs of high tectonic activity and the asymmetry indices of the basin topographic symmetry T. In addition, the distribution of the high values of the index in the area near Katharoneri should be noted, in which smaller ruptured structures are observed. A corresponding density map was constructed for the values of the ratio valley floor to valley height Vf. Index values are grouped into three classes [80,84,88,90,91]. This grouping correlates the index values with active tectonics classes. In this way, high values of the index (>1) correspond to low active tectonics, whereas low values of the index (<0.5) indicate high uplift rates. According to this separation and the measurements in the present analysis, the majority of the values of the geomorphic indices along the Xilokastro fault fall within the field of high uplift rates at the footwall of the fault (Figure 7). However, it seems that the lithology also plays a very important role as the largest cluster of low values is located in the area between Fonissa and Trikalitikos in the eastern part of the fault (Figure 7). The small size of these values is related to lithology, as in this area the streams flow in deltaic deposits forming high deep erosion and therefore relatively small widths in the active riverbed. However, a general observation that is easily deduced is that low values of the index are observed almost along the entire length of the fault trace.
Finally, for the Hypsometric integral index as shown in Figure 7c, it is striking that several basins in the western part of the fault are in a young stage. The remaining basins along the fault are placed in a mature stage, with only three basins being in an aged stage. The catchments classified in an aged stage are located in both parts of the fault. They are characterized by their size, which is impressive. One of them is the largest basin, which, as shown in Figure 7c, is less elongated and therefore is expected to be classified as old. However, the same basin exhibits low values of valley floor to width ratio due to its lithology. The other two basins are extremely small in size, which would be expected to be associated with earlier stages of erosion. Probably, their classification in the old stage is due to the “effort” of the catchments to increase their hydrodynamic capacity by attracting adjacent basins or to be a non-ruptured point in the fault (persistent segment barrier).

5. Discussion

For the overall assessment of the active tectonics in the whole area of the Xilokastro fault, the geomorphological indices were joined in a combined index Iat. These are the basin-shaped coefficient indices of the catchment area Bs and the tectonic morphometric indicators except the index of the transverse topographic symmetry T. The index distribution identifies the most active sections of the fault via ArcGIS by presenting a rather simplified map of tectonic activity along the fault (Figure 8). Based on the distribution of the combined index Iat, its values that are less than 2 represent high tectonic activity. Areas with high tectonic activity occur in both the western and eastern part of the fault, although the steepest slopes in the topographic profile are observed in the west. However, both the findings from the SL stream length-slope index for the western part and those of the valley floor-to-height ratio for the eastern part are compatible with the distribution of the combined index. In addition, special note should be made of the areas that flow through the rivers Skoupeikos, Fonissa, Trikalitikos, and Katharoneri. Except for the area of Skoupeikos, where high tectonic activity occurs in other areas, the active tectonics is clearly lower. Considering the AF basin asymmetry index, the creation of an overlap zone is evident, especially in the area of Fonissa, and is also seen in the Skoupeikos area. As for the eastern and western boundary of the fault, they seem to disappear in the area and therefore the results of the geomorphological analysis do not support either the merging with the submarine part of the fault to the east or the westward propagation of the fault. Similar observations were made for the Xilokastro submarine fault by [41,50] and for the western part of Xilokastro and its possible merge with the Valimi fault by [20,52].
Based on the combined index (Iat) (Figure 8) that resulted from the detailed morphotectonic analysis of Xilokastro fault, the fault slip rate was calculated. According to [92] the slip rate at highly active fault scarps corresponds to 0.08 mm/yr, whereas according to [93], it was found to be 0.4–0.5 mm/yr. The distribution of the combined index showed that along the Xilokastro fault the largest percentage of runoffs belongs to the order of highly active tectonics (Figure 8) with almost straight foothills, main runoff channels of deep erosion, elongated runoff basins, and changes in the topographic profiles of the streams that develop at the fault footwall. All these results derived from the morphotectonic analysis of the faults demonstrate rapid rates of vertical erosion and tectonic slip. In addition, the data are compatible with the morphometric analysis of [94], who applied morphometric measurements across ten pre-existing river systems along the south coast of the Gulf of Corinth.

6. Conclusions

The variability in the distribution of the values of the geomorphological indices significantly influences the classification of the whole fault and its segments into classes of tectonic activity. The application of geomorphological indices seems to be extremely useful in areas that are not dominated by very high activity that, although they have clear evidence of tectonic activity—such as the Xilokastro fault, with its impressive fault scarp—do not record recent incidents of seismic activity. The conclusions from the present study are:
  • The application of the geomorphological indices along 102 small basins along the Xilokastro fault proposes high fault activity.
  • Although the fault shows high activity, the prominent segment linkage is not achieved. These segments are defined by the Skoupeikos, Fonissa, and Trikalitikos antecedent rivers.
  • Its high degree of tectonic activity is certified by the high values of the length-slope index near its trace, by the low values of the valley floor-to-height ratio index, the strong asymmetry of the catchments, especially in between overlapping segments, and from the elongated shape of its catchments.
  • Its morphotectonic impact according to the index of hypsometric integral is in a young stage, especially in the western part of the fault, which shows the steepest relief, but no signs of fault propagation are recognized either to the west or to the east.
Therefore, for active faults whose paleoseismological history is unknown, morphotectonic analysis can help estimate key variables such as slip rate and recurrence time interval that are considered important elements for a seismic hazard analysis across a fault. Moreover, considering the possibilities provided by modern technology and the easily and economically feasible access to high-precision digital products, it seems that geomorphological indices contribute to the determination of fault activity.

Author Contributions

Conceptualization, S.V.; methodology, S.V. and V.Z.; software, S.V.; validation, S.V.; formal analysis, S.V. and V.Z.; investigation, S.V.; resources, S.V.; data curation, S.V.; writing—original draft preparation, S.V. and V.Z.; writing—review and editing, S.V. and V.Z.; visualization, S.V. and V.Z.; supervision, V.Z.; project administration, S.V. and V.Z. All authors have read and agreed to the published version of the manuscript.

Funding

This research received no external funding.

Institutional Review Board Statement

Not applicable.

Informed Consent Statement

Not applicable.

Data Availability Statement

Not applicable.

Acknowledgments

The authors are grateful to the referees for their constructive and positive comments and to all editors for the excellent managing and suggestions on the manuscript.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. Simplified map of the Gulf of Corinth (modified by [13,14]). The inset figure shows the geological setting of the study area.
Figure 1. Simplified map of the Gulf of Corinth (modified by [13,14]). The inset figure shows the geological setting of the study area.
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Figure 2. (inset) Geological setting of Greek peninsula; (a) 3D model of the Xilokastro fault constructed through the ArcScene platform. The red line is the trace of the rift as mapped during field work. (b) Topographic profile of the displacement of the hanging wall (line 1) and the footwall (line 2) of the fault. Line 3 illustrates the normalized topography of the individual ruptures along the fault section, and line 4 illustrates the overall topographic representation of the two main sections of the fault.
Figure 2. (inset) Geological setting of Greek peninsula; (a) 3D model of the Xilokastro fault constructed through the ArcScene platform. The red line is the trace of the rift as mapped during field work. (b) Topographic profile of the displacement of the hanging wall (line 1) and the footwall (line 2) of the fault. Line 3 illustrates the normalized topography of the individual ruptures along the fault section, and line 4 illustrates the overall topographic representation of the two main sections of the fault.
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Figure 3. Simplified map of the Xilokastro fault showing stereographic projections of the polished surfaces and the sliding lines of the main scarps whose position is marked with a white dashed line. In addition, photos taken during field work are displayed, the locations of which are symbolized by the image of the camera. The yellow box marks parts of the photos that are presented in a larger scale. (a) Panoramic view of the western part of the Xilokastro fault (its exact location is marked with a black box on the map). (b) Photomosaic of the scarp derived that appears on Ano Loutro–Kato Loutro road. (c) Detail view of the same surface. (d) Panoramic view of the eastern part of the fault. The hill is known as “Panagia Korifis”. (e) Photomosaic of a fault surface marked in the yellow frame of the photo in (a). (f) Colluvial deposits accumulating at the base of the fault. (g) Detailed geometry of the background with the Neogene formations. (h) Successive sea terraces at the eastern end of the fault.
Figure 3. Simplified map of the Xilokastro fault showing stereographic projections of the polished surfaces and the sliding lines of the main scarps whose position is marked with a white dashed line. In addition, photos taken during field work are displayed, the locations of which are symbolized by the image of the camera. The yellow box marks parts of the photos that are presented in a larger scale. (a) Panoramic view of the western part of the Xilokastro fault (its exact location is marked with a black box on the map). (b) Photomosaic of the scarp derived that appears on Ano Loutro–Kato Loutro road. (c) Detail view of the same surface. (d) Panoramic view of the eastern part of the fault. The hill is known as “Panagia Korifis”. (e) Photomosaic of a fault surface marked in the yellow frame of the photo in (a). (f) Colluvial deposits accumulating at the base of the fault. (g) Detailed geometry of the background with the Neogene formations. (h) Successive sea terraces at the eastern end of the fault.
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Figure 4. A 3D relief model of the hydrographic network that develops along the orientation of the Xilokastro fault. The catchments highlighted in bright pink intersect its trace and are numbered from the west to the east end of the fault.
Figure 4. A 3D relief model of the hydrographic network that develops along the orientation of the Xilokastro fault. The catchments highlighted in bright pink intersect its trace and are numbered from the west to the east end of the fault.
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Figure 5. (a) Spatial distribution of the drainage basin index Βs. The red line symbolizes the trace of the Xilokastro fault. Smaller sedimentary faults in the area have been projected between the rivers Trikalitikos and Katharoneri. (b) Spatial distribution of the RL elongation basin index. (c) Spatial distribution of the RC circularity basin index.
Figure 5. (a) Spatial distribution of the drainage basin index Βs. The red line symbolizes the trace of the Xilokastro fault. Smaller sedimentary faults in the area have been projected between the rivers Trikalitikos and Katharoneri. (b) Spatial distribution of the RL elongation basin index. (c) Spatial distribution of the RC circularity basin index.
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Figure 6. (a) Spatial distribution of the AF basin asymmetry index. (b) Spatial distribution of the transverse topographic index T. The colours in the catchments along the fault correspond to the average size calculated for each basin and the yellow arrows in the middle show displacement direction of the main branch of each basin.
Figure 6. (a) Spatial distribution of the AF basin asymmetry index. (b) Spatial distribution of the transverse topographic index T. The colours in the catchments along the fault correspond to the average size calculated for each basin and the yellow arrows in the middle show displacement direction of the main branch of each basin.
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Figure 7. (a) Spatial distribution of SL length-slope value values. The green to yellow areas indicate areas where the values of the index show from no to small anomaly, whereas the red areas indicate the areas that are dominated by very high anomalies. (b) Spatial distribution of values of the ratio of valley floor to valley height Vf. The red areas correspond to high tectonic activity, whereas the yellow areas indicate the moderate tectonic activity sites, and the green areas highlight low tectonic activity areas. (c) Spatial distribution of the hypsometric integral Hi.
Figure 7. (a) Spatial distribution of SL length-slope value values. The green to yellow areas indicate areas where the values of the index show from no to small anomaly, whereas the red areas indicate the areas that are dominated by very high anomalies. (b) Spatial distribution of values of the ratio of valley floor to valley height Vf. The red areas correspond to high tectonic activity, whereas the yellow areas indicate the moderate tectonic activity sites, and the green areas highlight low tectonic activity areas. (c) Spatial distribution of the hypsometric integral Hi.
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Figure 8. Spatial distribution of the combined index Iat.
Figure 8. Spatial distribution of the combined index Iat.
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Table
Table 1. Main morphometric indices calculated for the drainage basins along the Xilokastro fault front.
Table 1. Main morphometric indices calculated for the drainage basins along the Xilokastro fault front.
Geomorphic IndicesMathematical FormulaXilokastro Fault
Number of Calculations for Each Index
Number of valleys 102
Drainage basin shape Bs (1, 2) Bs = BL/Bw102
Elongation Basin Index RL (1, 2)RL = 2√(A/π)/L102
CircularityBasin IndexRc(1, 2) Rc = 4πA/P2102
Asymmetry Factor AF (1, 3)AF = 100(Ar/At)102
Transverse Topographic Symmetry Factor T (1, 3)T = Da/Dd881
Stream length-gradient index SL (1, 4)SL = (ΔH/ΔL)L845
Valley Floor Width–Valley Height Ratio Vf (1, 5)Vf = 2Vfw/[(Eld − Esc) + (Erd − Esc)]1673
Hypsometric integral Hi (1, 6)Hi = (hmid − hmin)/(hmax−hmin)1859
(1) = For the definition and calculation of the geomorphic indices described in the current analysis see [58,59,84] and references therein. (2) = Elongated catchments (tectonically active) usually have a small secondary network compared to circular catchments (inactive tectonics), which have a network with branches of many orders [85]. (3) = The development of a river basin network in stable geological conditions results in absolute symmetry for basin and river characteristics. Any tectonic force affects this ideal symmetry [86]. (4) = When the elongated profile of a riverbed differs from the typical profile, then the differentiation reveals changes in the lithology and the tectonics of the area [87]. (5) = Streams with a narrow riverbed and steep banks show V-shaped river valleys characterized by deep erosion, whereas a wide riverbed with gentle banks forms a U-shaped river valley showing the prevail of erosion against tectonic forcing [88]. (6) = The Hypsometric Integral index marks the stage of evolution in which the catchment is in relation to the erosion cycle [1,69].
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Verroios, S.; Zygouri, V. Geomorphological Analysis of Xilokastro Fault, Central Gulf of Corinth, Greece. Geosciences 2021, 11, 516. https://doi.org/10.3390/geosciences11120516

AMA Style

Verroios S, Zygouri V. Geomorphological Analysis of Xilokastro Fault, Central Gulf of Corinth, Greece. Geosciences. 2021; 11(12):516. https://doi.org/10.3390/geosciences11120516

Chicago/Turabian Style

Verroios, Sotirios, and Vasiliki Zygouri. 2021. "Geomorphological Analysis of Xilokastro Fault, Central Gulf of Corinth, Greece" Geosciences 11, no. 12: 516. https://doi.org/10.3390/geosciences11120516

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