Content area
The neotectonic processes are crucial for identification of active faults in a seismic unstable area. The Aїn Smara active fault runs along the Middle Rhumel Valley located in Constantine area of Algerian Eastern Tell Atlas mountain chain and it emerges in the south‒western part of the epicentral zone of the earthquake occurred on October 27, 1985 (Mw = 5.8) within a corridor displaying morphological features and deformed Pliocene‒Quaternary layers, which are the consequence of transpressive tectonic regime. In our study the morpho-tectonic and structural research supported by the fieldwork, was performed. The thick fault gouge indicating simple shear deformation, fault breccias and minor faults affecting the Pliocene limestone and Quaternary alluvial terraces, were found. The active fault splits into northern and southern segments. The northern segment corresponds to the El Aria Fault that ruptured during the earthquake in 1985 and the southern segment with the studied Aĭn Smara Fault. Our research showed the significant extent of the active fault and including its parameters for improved seismic hazard assessment of the Constantine area.
INTRODUCTION
The kinematics of many active faults located along the Algerian Tell Atlas has researched nowadays to the extent that isn’t enough to allow identifying their geometry and neotectonic regime (Fig. 1).
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Fig. 1.
Map of active faults of Algerian Tell Atlas (after [106], modified). The identified: active faults (after [44, 64, 106]; the large earthquakes (Mw ≥ 4.5) for the period 858 BC‒2008 (after [58, 112]); the focal mechanisms of the main strong earthquakes (after [113]), except for Mila-2020 (after [17]). The earthquakes (numbers): (1) Constantine-October 27, 1985 (Mw = 5.8); (2) Mila-2020 (Mw = 4.8); (3) Béjaia-2021 (Mw = 6.0); (4) Boumerdes-2003 (Mw = 6.8); (5) Algiers-2014 (Mw = 5.6); (6) Asnam-1980 (Mw = 7.1); (7) Oran-2008 (Mw = 5.5); (8) Aїn Timouchent-1999 (Mw = 5.6).
There is opportunity for observing outcrops that prove brittle deformation. These outcrops were the subject of previous studies [1, 6, 13, 21, 31, 33, 36, 56, 57, 66, 74, 101].
On basis of the data of historical strong earthquakes and using instrumental seismicity measurements the seismic hazard maps of Northern Algeria were created [10, 18, 19, 24, 58, 81, 84].
The areas where strong earthquakes happened, showed systematically the significant hazard while whereas in regions with moderate seismicity; the role of active faults is underrating. However, the recent geodetic studies have supported the larger seismic hazard in areas of strain accumulation close to certain faults, either inland or offshore [25]. As well as they suggested the fault zone accommodating ~2 mm/year of slip in the Tell Atlas wither the Constantine region as a zone of high strain accumulation. The region belongs to the Eastern Tell range, seismically active domain of the Northern Algeria. At the margin of the Tellian massifs with the Pliocene‒Quaternary Rhumel basin, where evidences of neotectonic activity associated to Aїn Smara active fault, are discernible.
The transpressive tectonics date back to the Eocene has engendered major strike-slip faults; situated along the Tell range similar to the Algerian margin a transpressional structure [12, 39, 91]. Moreover, large strike-slip faults identified within the Western Mediterranean, as well, along the Moroccan Rif, Tunisian Atlas, Betic and the South Alps, Pliocene strike-slip faults were recognized [11, 15, 16, 30, 32, 34, 35, 51, 70, 79, 80, 82, 86, 89, 90, 93, 95‒97].
This has motivated our interest on the transpressive tectonics observed inside a fault corridor along the Rhumel Valley located in south‒west of the epicentrale zone of October 27, 1985 Constantine earthquake (Mw = 5.8) [59].
The aim of our study is evaluating the neotectonic framework of the 1985 Constantine earthquake by:
(i) combining the alpine tectonic structures with the recorded seismicity in Constantine region;
(ii) examining the morphological expressions and indications related to the Pliocene tectonics within the Rhumel Fault corridor;
(iii) discussing the fault implications in the seismic hazard assessment of Constantine area.
TECTONIC FRAMEWORK
The Constantine has area been shaken frequently by earthquakes, including three major events in 1908, 1947 and 1985, marked by the instrumental measurements [61]. The last earthquake (Mw = 5.8) occurred in October 27th 1985 is so far the strongest earthquake recorded. Its epicentre was located in El Aria, ~20 km to east of Constantine city [28] (Fig. 2).
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Fig. 2.
(a) Geological setting of the study area within the Tell Atlas mountain chain. The topographic relief (after [114]); tectonic limits of Northern Algeria (after [45, 91]). The active domain tectonic boundaries (from north to south): SK—South Kabyle Fault; FN—Miocene frontal thrust corresponding to the southern border of the Tell Atlas; ANA—North Atlasic Accident—the supposed tectonic boundary of Maghrebides chain of the Atlas chain; ASA—South Atlasic Accident (or South Atlas Front, or Sahara Flexure)—the front marks the end of active domain: a structural feature that extends from Morocco to Tunisia (after [50]), the South Atlas Front marks the transition from the relatively undeformed Sahara Platform to the deformed Atlasic domain to the north. (b) Shaded map of the Constantine–October 27, 1985 earthquake epicentral area. The DEM [108] is based on Shuttle Radar Topography Missions (SRTM1) data with 1 arc-second resolution [115]; the focal mechanisms of earthquakes within the study area are from GCMT [113]. Indicated: the azimuths of P-axis of the focal mechanism and sinistral strike-slip on NE‒SW trending fault, the nodal planes oriented N213E and N117E (black lines); Middle Rhumel Valley (black rectangle); the El Aria area (white square) (after [5]).
Its focal mechanism showed the left lateral fault oriented N217°‒84°NW [40]. The aftershock distribution displays the NE‒SW “cloud” of 14 km length, 10 km wide and 15 km in depth [83]. The main shock caused many landslides and rock falls, as well as cracks in soft ground oriented NE‒SW, similar to the strike of the fault derived from the focal mechanism.
According to seismological studies, the Aїn Smara Fault is the seismic source associated to the earthquake occurred on October 27, 1985 although; the earthquake location coincides with the El Aria Fault [26‒28]. The crucial geological fault was observed in the epicentre area [5]. As soon as the epicentre area of occurred earthquake was located northeastward of Aїn Smara fault, thus, the active fault is a system composed of Aїn Smara and El Aria NE‒SW sinistral strike-slip faults (Fig. 2b). These are faults forming tectonic framework of Constantine range, effect of influence of the Middle–Upper Eocene and Lower Miocene phases [29, 68].
The Constantine range belongs to Tell Atlas mountain chain is an allochthonous domain of the Maghrebian orogen which results from Cenozoic slow convergence involving the closure of the Tethyian basin [53, 70, 103].
The Neotectonics outsets were synchronous with the West Mediterranean opening and prolonged during the Pliocene by transpressive tectonics [46, 48, 54, 55, 63, 73].
The stress field remained relatively steady during the Pliocene‒Quaternary with shortening and extensional episodes interrelated under the regional compressive field [3, 41, 42, 72, 76].
With the geodynamic process, the formation of Tell Atlas occurred during two paroxysmal phases spaced by a quiet extensive phase [12, 91]:
— the 1st initial phase took place under transpressive tectonic process from the Middle to Late Eocene organized the different geological units of Tell Atlas;
— the 2nd compressive phase started largely in the Lower Miocene generating in the main EW thrust-nappe and two transverse strike-slip faults networks (dextral NE‒SW, sinistral faults and NW‒SE dextral faults).
The post-nappe basins establishment followed in the Middle Miocene. That event marked the outset of the neotectonic period in Tell Atlas which took place in two compressive phases:
— the Upper Miocene‒Pliocene;
— the Late Pliocene to the Present.
Structural indications are observed occasionally near alpine faults, at the edges of basins with the Tell massifs [2, 22, 23].
It was demonstrated the inversion of strain field and the reactivation, for example, of some old normal faults and thrust faults in orogenic belts [62].
In Constantine region, the Neotectonics is evidenced by brittle deformations.
It was reported mainly, reverse faults affecting the upper Miocene, strike slip faults in the Pliocene and fractures in the Quaternary [13, 60, 101].
In [78] was confirmed the existence of N‒S Quaternary normal faults within the epicentre zone.
Moreover, the brittle deformation is reported in the Center Tell Atlas. For example, [33] identified the N‒S Quaternary normal faults in the Babors Mountains, the seismically active zone belonging to the Kabylian domain.
It was reported N‒S normal faults affecting the Sahel and the Mitidja Basin which are two confirmed active structures in Algiers region [56, 92].
These identified neotectonic structures were resulting of converge forces exerted at the African and Eurasian plates, which have been moved since the Lower Miocene to Quaternary from N‒S to NNW‒SSE involving the Atlas in continued seismic activity [8, 9, 37, 38, 87].
The current convergence occurs at rate of 2–3 mm/year along the Algerian transverse where the Tell Atlas is the most seismically active domain in northern Algeria [77].
Along this domain, a number of faults predominantly (NE‒SW sinistral strike-slip faults and E–W dextral strike-slip faults) has an important seismic role in Eastern Tell that encompasses the Constantine region [4, 75].
DATA AND METHODS
We carried out the morphotectonic and structural analyses on a corridor along the Middle Rhumel Valley where runs Aїn Smara active fault [20, 23, 65, 67, 85, 94, 98, 99, 104, 105].
The method combines the morphotectonic examination and structural analysis. We used tools from spatial resources DEM (ASTER GDEM v.3, SRTM1 data with 1 arc-second resolution) [108], the catalogs of historical seismicity [60, 110] and the geological maps of Oued Athmania, Constantine, El Khroub areas at map scale 1 : 50 000 [116]. We exploit the GIS software (MapInfo) [109] for mapping.
We support the assessment by field investigations. The analysis of fault traces and its recent activity is based on:
(i) Geomorphic and morphotectonic examination via satellites imagery and digital elevation models (DEMS) [110] displaying landform, topography and shape of the Constantine massifs.
(ii) Trace of paleo-earthquakes recognized overall by the presence of the raised alluvial terraces and the fault escarpments corresponding to surface ground rupturing; as indirect indicators of earthquakes during the Quaternary [15].
(iii) Deformation expression near and far from the Aїn Smara fault (Rhumel faults in this study), are documented from Geological Map [116].
(iv) Faulting and microstructural (C/S) affecting the Pliocene strata, revealed in the field and on digital elevation models (DEMS) [108], are organized to transpressive tectonics under simple shear.
(v) Drawn-out the first steps of seismic hazard assessment by integrating the cartographic parameters of the considered active fault, to estimate the maximum magnitude that could have been generated.
We used the empirical relationships linking the magnitude of the seismic moment Mw to the length, width of the failure plane [102].
RESULTS
Seismicity Analysis and Characterization Seismic Sources
The Constantine area being the seismically active area has seen moderate earthquakes (4.0 < Mw < 5.8) and shows evidence of active tectonic. There is a significant correlation between seismicity and its tectonic framework. The combination delineates two seismotectonic zones, as shown in Fig. 3.
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Fig. 3.
Map of seismic zoning of Constantine area. The seismicity recorded with the structural sets: Tellian tectonic units and their adjacent Pliocene‒Quaternary basins of the Constantine range (after [101]), the earthquakes (after [112]).
The northern zone has recorded from low to moderate seismicity (magnitudes Mw ≤ 4.5). However, it experienced destructive earthquakes, among them the Jijel (Djidjeli) earthquake on August 22, 1856, with an intensity of I0 = X MSK and the Skikda earthquake on September 19, 1935, with an intensity of I0 = VI EMS [61].
In the southern zone during the instrumental period with intensities I0 = VII EMS there were three strong earthquakes recorded with magnitudes [60, 61]:
— Mw = 5.2 (August 4, 1908);
— Mw = 5.3 (August 6, 1947);
— Mw = 5.8 (October 27, 1985).
Recently in the area occurred two moderate earthquakes with magnitudes [17]:
— Mw = 4.6 (July 17, 2020);
— Mw = 4.8 (August 7, 2020).
More than 30 low-magnitude earthquakes (with magnitudes fM l ≤ 4) were localized within the Middle Rhumel Valley [112].
Geomorphological Analysis
We investigated the fault corridor underlined the limits the foot of the Constantine area-foothills from the southern edge of the Middle Rhumel basin. This corridor exhibits geomorphic features of the young relief and paleo-earthquakes forewarning.
The hydrographic network marks the direction of the main Alpine faults. Streams flow mainly in NW‒SE or N‒S directions, for example the two main tributaries of the rivers Oued Rhumel, the Oued Seguen and Oued Athmania (Oued means river and also valley in Arabic of North Africa, Oued Athmania, Oued Seguen are the names of areas contiguous to the Rhumel Valley).
The Oued Rhumel River (~250 km-long) drains the plains of the Great Constantine region and crosses the Plateau of Constantine through gorges. Its U-shape inside the Middle Rhumel Valley (MRV) is probably the result of fault-controlled changes in flow direction (Fig. 4a).
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Fig. 4.
(a) Morphologic setting—the map displays the hydrographic network [111] and the elongated shape of the Middle Rhumel Valley (MRV) massifs, the west and east deflections of the Rhumel River (white circles); (b) profiles within the MRV massifs: longitudinal profile A—length of MRV, profiles B, C and D—asymmetric slopes of the MRV massifs, cross-sections II, III and IV—width of MRV massifs, profiles P1, P2 and P3—steep topography on the Pliocene slopes (which we associated with fault scarps), morphotectonic lineaments (dashed black lines); (c) arrangement of the Pleistocene and Quaternary alluvial terraces along the Djebel Felten.
Two main deflections are discernible:
— in the western part at the entrance of the MRV, where the Rhumel bypasses the side of the Tellian massif in Oued Athmania area (Fig. 4a, D1);
— in the eastern part, to the north of Aїn Smara (Fig. 4a, D2).
In fact, from the source to the Constantine area, the Oued Rhumel River flows NW‒SE, then WSW‒ENE within the Middle Rhumel Valley. It becomes considerably narrower near Aїn Smara and forms the almost complete oxbow. Further, in its down-stream, the Oued Rhumel River flows SSW‒NNE.
The shape of Djebel Chettabah (1266 m), Djebel Felten (1097 m), and Djebel Sekoum-Sellam mountains that are Tellian massifs bounded the Rhumel Valley in the north and the south, are shown in Fig. 4b (profiles A‒D).
These massifs have trend NE‒SW and display elongate shapes and asymmetric flanks. Their topography is steep in front of the north Rhumel fault (NRF) and the south Rhumel fault (SRF). In contrast, the north slope of Djebel Chettabah mountain shows flat surfaces and the south slope of Djebel Felten mountain shows gentle slopes.
The faults Escarpments of the Rhumel faults are observable in the landscape and on satellite imagery [110] along the south flank of Djebel Chettabah mountain and along the northern slope of Djebel Felten mountain (Fig. 4, I‒IV).
The most remarkable case is the Djebel Felten cumulative escarpment. At its summit, we observed the main scarp, which is more than 4 m high, pronounced by break in slope and by interruption of the stream system. At low altitudes, the slope is incised by numerous streams and along natural sections.
Secondary escarpments are also apparent. Here, we observed dislocated Quaternary terraces affected by normal faults (Fig. 4c).
It is shown the suspended Pleistocene terraces dislocated by N‒S and E‒W trending normal faults (Fig. 4c). The terraces can be grouped into:
— alluvium of the Rhumel;
— Ancient- alluvium;
— Quaternary terrace (between 15‒25 m);
— Pleistocene terrace (between 30‒50 m elevation).
We interpret the scarps inside the corridor that is bordering the Djebel Chettabah to the south and the Djebel Felten mountains to the north, as expression of earthquakes during the late Quaternary of Aїn Smara fault.
Neotectonic Analysis
Structural Analysis. Existing geological data confirmed that Aїn Smara Active Fault is the NE‒SW left strike-slip oriented N060E with sub-vertical component, brings Cretaceous of Tellian nappes into contact with Pliocene formations over the length of 30 km long.
Its neotectonic activity is established since it affects the Plio‒Quaternary deposits of the Rhumel Valley. Certainty, this is a system fault divided into the northern and southern segments (Fig. 5):
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Fig. 5.
(a) Geological map of the Rhumel Valley (after [101], modified). Geological units: (i) Ante-Neogene (assembles Tellian units, flysch units); (ii) Pliocene (corresponding to the continental deposits characterized by clays, conglomerates and thick lacustrine limestones); (iii) Quaternary deposits; (b) geological cross-sections showing the neotectonic setting near the Rhumel Fault: (1) Quaternary, (2) Pliocene, (3) Peni Tellian nappe Cretaceous, (4) Tellian nappe Cretaceous, (5) Neritic Cretaceous.
— North Rhumel Fault (NRF) affecting the south slope of Djebel Chettabah mountain;
— South Rhumel fault (SRF) affecting the north slope of Djebel Felten mountain.
Within the zone delimited by the NRF and SRF, we have identified brittle deformation in the Pliocene and Quaternary units:
— The Pliocene layers show mainly the south plunging monoclinal structure ( < 20°), sometimes with steeper dips 30°‒40°. The Pliocene is inclined towards the S‒E at the western edge of Djebel Felten mountain. Outside the corridor, the Pliocene layers show a slightly inclined monoclinal structure and minor fractures affect the southern slope of Djebel Chettabah mountain (Fig. 5C). We emphasized the Aїn Smara bulge that we interpreted as a NE‒SW flexure fold or drag fold associated with the South Rhumel Fault represented by blue rectangle as showing in Fig. 5(a).
— The Quaternary layers are sub-horizontal. N‒S and E‒W trending normal faults in the Quaternary terraces are marked on the geological maps (Figs. 4, 5).
Field Investigations. We highlighted microstructures (C/S) related to transpressive tectonics discovered in the field and on digital elevation models (DEMS) [108]. Evidence are observed on the two Rhumel River banks. These are mainly fault gouges, faults planes with slip sense criteria (slickensides) and kinematic data from microtectonic figures at outcrop scale and regional scale [5].
On the left bank of the Rhumel River, the first site shows deformation related to the north Rhumel fault is apparent on the slope of Djebel Chettabah mountain.
The site S1 displays minor (metric to hectometres) normal faults in Pliocene limestone (Fig. 6).
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Fig. 6.
Photos through section S1, piedmont of Djebel Chettabah massif, SW Constantine. (a) Pliocene bulge: from bottom to top, we distinguish soil, the fault gouge with clays, and the soft limestone with fractures; (b) cross section inside the Pliocene bulge showing E‒W and N‒S metric normal faults.
The site S2 shows an intra-Pliocene brittle deformation zone with an ENE‒WSW trending strike-slip fault with sinistral motion (Fig. 7).
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Fig. 7.
Photos through section S2, southern slope of Djebel Chettabah massif, intra-Pliocene strike-slip fault. (a) Lateral extension of the fault gouge: (a1) Fault plane showing horizontal striation, (a2) zoom of horizontal striations; (b) upper limit of the gouge and reappearance of fresh limestone: (b1) the relation of C and S0 structures indicates a lateral movement, (b2) fault mirror in the soft the Upper Pliocene.
The first outcrop is a fault gouge of more than 50 m length, composed of incohesive white clay includes microstructure elements, slickenside, and a minor fault mirror (azimuth N070, 85°) (Fig. 7, a1, a2). The second outcrop fault gouge revealing the C–S relation indicates a sinistral strike slip (Fig. 7, b1, b2).
The gouges in both sites display the intense strain that affected Pliocene units. They reveal simple shear mechanism and the geometrical relation of the C-S fabrics [88] establishes the left lateral motion (with C corresponds to fracture cleavage and S0 being the stratification plane).
On the right bank of Rhumel River, tectonic activity is associated with the south Rhumel fault. The north slope of Djebel Felten mountain shows fault scarps, oriented all in NE‒SW direction (Fids. 3, 8).
The site S3 reveals the most recent scarp in the slope toe and the oldest main scarp in the summit where we observe blocks of sheared and recently collapsed Cretaceous limestone (Figs. 8a, 8b).
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Fig. 8.
Photos through section S3, trace of the south Rhumel fault, northern slope of Djebel Felten massif. (a) and (b) correspond the right block of the fault; (c) fault breccia observed under the pathway (see (а)). Left: compacted breccias oriented in the direction of the scarp. Middle: sheared blocks. Right: pseudo striation indicating lateral sliding movement.
The youngest fault scarp in the slope toe displays an outcrop of tectonic breccia oriented N060, composed of angular incohesive elements (gravels and sheared blocks). Some of these blocks indicate the left lateral motion, (Fig. 8c).
The transpression is a type of strike-slip deformations that results from simple shear [43]. This tectonic regime affects the Middle Rhummel Valley, also verified at regional scale from the DEM [108] (Fig. 9).
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Fig. 9.
Tectonic framework showing the study area under simple shear. “C” represents shear planes, “S0” represents layer stratifications; (A) corresponds to the zone of intense deformation within the Rhumel Fault where the “C” planes and “S0” planes are parallel; (B) far from the fault zone: the “C” planes and “S0” planes form an angle between them, solid red star represents the epicenter of the October 27th 1985, Constantine earthquake, perspective view of the topography from SRTM1 data (after [115]).
The sheme illustrates undulations of all terrains including the Pliocene of the Middle Rhummel Valley. The topography is rugged and steep along the Rhumel faults.
Within the corridor, at the north Rhumel fault where C–S fabrics are parallel to the main fault trend were observed, is the location of the maximum deformation (Fig. 9, A).
We interpret this zone as corresponding to the core of the Rhumel Fault zone. Beyond, the planes C and S0 form between them an angle and the direction induces the sinistral movement (Fig. 9, B).
DISCUSSION
Geological Data Provided
The study brings results to the most plausible source of the October 27, 1985 earthquake and the position of Aїn Smara active fault. In fact, all previous seismological studies have located the epicenter of the earthquake at El Aria, East Constantine [28]. At the same time, they associate the earthquake to the Aїn Smara Fault. This one is located in the S‒W prolongation of the causative fault.
The Aїn Smara Fault is bordering the Middle Rhumel Valley (MRV), the Neogene basin exclusively with Plio‒Quaternary infill. We argue its neo-activity near the footwall of both (north Rhumel fault and south Rhumel fault) by:
(i) morphology features of its landform, as the assymetric shape of the MRV massifs (Djebel Chettabah, Djebel Felten);
(ii) fault scarps in the proximity of the Rhumel faults, as expressions of seismic activity during the late Quaternary;
(iii) structural indications of the fault zone showing simple shear in the Pliocene units with C–S fabrics indicating sinistral motion, and associated W‒E, N‒S minor normal faulting affecting both the Pliocene and the Quaternary. These are obvious a major strike slip fault under transpressive regime. The fault geometry can be explained with a large fault system associated Riedel shears.
Seismic Hazard Assessment
The importance of the recent deformations inducing by the Aїn Smara Fault along the Rhumel Valley, to which we link all or part of the seismic activity in SW of Constantine region. And we associate to El Aria Fault; all the seismicity recorded in the NE of Constantine, above all the main shock of October 27, 1985 earthquake and its aftershocks.
If we take into account the cartographic layout along the Middle Rhume Valley, we recognize that Aїn Smara fault constitutes the natural extension to the northeast, towards El Aria Fault system. Considering this fact and the similarities (strike-slip fault, NE‒SW orientation, comparable plunging) existing between the two faults:
— Aїn Smara strike-slip fault NE‒SW with sub-vertical component (plunging 70°) over ~30 km;
— El Aria Fault (NE strike-slip fault and vertical plunging).
Therefore, we can assume that they constitute two segments of the same Miocene network, which extends, at least, from the Middle Rhumel Valley in the southwest to the Djebel El Ouahch in the northeast.
If the two faults break during a probable earthquake, even stronger magnitudes can be reaching. We have employed of the empirical formula of [105] and [102], to estimate the maximum magnitude (Mw) of a probable earthquake. We suggest the length of 50 km (the Rhumel Fault zone and the El Aria Fault combined), the depth of 15 km (the epicentral depth of the 1985 Earthquake) and strike-slip motion. With the considered dimensions, the maximum moment magnitude (Mw) of a probable earthquake could reach M = 7.0.
CONCLUSIONS
The study provides new insights into the neotectonics observed on Aїn Smara fault along the Rhumel Valley in the Constantine area of Algerian Eastern Tell Atlas mountain chain. Our contribution consists on the following observations:
(i) Geomorphic features, the drainage system is largely controlled by Miocene faults network and by the asymmetric shape of the Tellian massifs.
(ii) Structural evidence, the deformation (tilt) of the Pliocene strata near of the footwall of both faults (North and South Rhumel faults) and microtectonic indications at outcrop and regional scales.
(1) The structural criteria are in favor of a system of NE‒SW to ENE‒WSW strike-slip faults with a sinistral component. Their occurrence can be explained by simple shear under a compressional regional strain field.
(2) In terms of seismic hazard assessment, we suggest that Aїn Smara Fault and its extension El Aria Fault that hosted the 1985 Earthquake are two segments of the same active neotectonic system. These need to be considered in an improved seismic hazard mapping of the Constantine area. Knowing that the historical seismicity is characterized by a long earthquake return period, we stress that the instrumental seismicity is not representative for the worst-case earthquake scenario. Thus, we propose taking into account both active faults, in case they may rupture together.
ACKNOWLEDGMENTS
We acknowledge the General Directorate of Scientific Research and Technological Development (MERS/DGRSDT) (Algiers, Algeria), the National Centre of Research Applied for Earthquake Engineering (CGS) (Algiers, Algeria) and Geology Department belongs to Institute of Architecture and Earth Sciences of the University of Ferhat Abbes 1-Sétif (UFAS-1) (Sétif, Algeria) for the support of our research.
We are sincerely grateful to Christoph Grützner (Friedrich Schiller University, Jena Germany), Maouche Said (Astronomy Research Center Astrophysics and Geophysics, Algiers, Algeria), Benfedda Amar (Center of Research Applied for Earthquake Engineering, Algiers, Algeria) for their constructive discussions. We warmly thank our colleague Kheiri Ahmed (Center of Research Applied for Earthquake Engineering, Constantine, Algeria) for consultations. We are thankful to anonymous reviewers for useful comments and extend our gratitude to editor M.N. Shoupletsova (Geological Institute of Russian Academy of Sciences, Moscow, Russia) for careful editing.
FUNDING
This work was supported by Center of Research Applied for Earthquake Engineering (CGS) (Algiers, Algeria) as part of Research project.
CONFLICT OF INTEREST
The authors of this work declare that they have no conflicts of interest.
Publisher’s Note.
Pleiades Publishing remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
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