Active Fault, Fault Growth and Segment Linkage Along the Janauri Anticline (Frontal Foreland Fold), NW Himalaya, India

Tectonophysics 483 (2010) 327–343

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Tectonophysics

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Active fault, fault growth and segment linkage along the Janauri anticline (frontal foreland fold), NW Himalaya, India

Javed N. Malik a,⁎, Afroz A. Shah a,1, Ajit K. Sahoo a,2, B. Puhan a, Chiranjib Banerjee a, Dattatraya P. Shinde b, Navin Juyal b, Ashok K. Singhvi b, Shishir K. Rath a a Department of Civil Engineering, Indian Institute of Technology Kanpur, Kanpur 208 016, UP, India b Physical Research Laboratory, Ahmedabad 380 009, Gujarat, India article info abstract

Article history: The 100 km long frontal foreland fold — the Janauri anticline in NW Himalayan foothills represents a single Received 27 October 2009 segment formed due to inter-linking of the southern (JS1) and the northern (JS2) Janauri segments. This Accepted 30 October 2009 anticline is a product of the fault related fold growth that facilitated lateral propagation by acquiring more Available online 10 November 2009 length and linkage of smaller segments giving rise to a single large segment. The linked portion marked by flat-uplifted surface in the central portion represents the paleo-water gap of the Sutlej River. This area is Keywords: comparatively more active in terms of tectonic activity, well justified by the occurrence of fault scarps along Active faults Fault related fold growth the forelimb and backlimb of the anticline. Occurrence of active fault scarps on either side of the anticline Lateral propagation of fault suggests that the slip accommodated in the frontal part is partitioned between the main frontal thrust i.e. the Segment linkage Himalayan Frontal Thrust (HFT) and associated back-thrust. The uplift in the piedmont zone along southern Paleoseismology portion of Janauri anticline marked by dissected younger hill range suggests fore-landward propagation of NW Himalaya tectonic activity along newly developed Frontal Piedmont Thrust (FPT), an imbricated emergent thrust branching out from the HFT system. We suggests that this happened because the southern segment JS1 does not linked-up with the northwestern end of Chandigarh anticline segment (CS). In the northwestern end of the Janauri anticline, due to no structural asperity the tectonic activity on HFT was taken-up by two (HF1 — in the frontal part and HF2 — towards the hinterland side) newly developed parallel active faults (Hajipur Fault) branched from the main JS2 segment. The lateral propagation and movements along HF1 and HF2 resulted in uplift of the floodplain as well as responsible for the northward shift of the Beas River. GPR and trench investigations suggest that earthquakes during the recent past were accompanied with surface rupture. OSL (optical stimulated luminescence) dates from the trench suggests occurrence of at least two events during the recent historic past, with the latest — Event II during 1500 AD (?). © 2009 Elsevier B.V. All rights reserved.

1. Introduction represent the principal intracrustal thrusts: the Main Central Thrust (MCT), Main Boundary Thrust (MBT), and Himalayan The tectonic collision between Indian and Eurasian plates has Frontal Thrust (HFT), with younger initiation ages towards the made the Himalayan arc as one of the most seismically active south (Thakur, et al., 2007). The strain accumulated across the regions of the world. Since collision (∼50 Ma) along the Indus– Himalayan zone due to ongoing deformation has been episodically Tsangpo Suture Zone, the successive zones of deformation have released in form of large to moderate magnitude earthquakes in progressively advanced southward, resulting in faulting and folding the region. The recent 2005 (Mw 7.6) Muzaffarabad earthquake has along the prominent structural features of the Himalayan orogenic again proved the capability of the Himalaya in producing large belt (Gansser, 1964; Seeber et al., 1981; Lyon-Caen and Molnar, magnitude earthquakes. Field investigations revealed a rupture of 1983). From north to south these prominent structural features about 65 km along an earlier identiﬁed “Tanda active fault” having lateral extend of about 16 km (Nakata et al., 1991; Kaneda et al., 2006; Yeats and Hussain, 2006). These earthquakes have raised ⁎ Corresponding author. concerns toward the seismic hazard assessment in Himalaya, E-mail addresses: [email protected] (J.N. Malik), [email protected] (A.A. Shah), especially in the foothill zones bordering the thickly populated [email protected] (A.K. Sahoo), [email protected] (D.P. Shinde), Indo-Gangetic Plain. Apart from few large magnitude events in NW [email protected] (N. Juyal), [email protected] (A.K. Singhvi). Himalaya with M≥ 7.6 viz. 1555 and 1885 Kashmir events; 1905 1 Now at School of Earth & Environmental Sciences, James Cook University, Townsville Queensland 4811, Australia. Kangra and recent 2005 Muzaffarabad, no historical records are 2 Now at Reliance India Limited, Mumbai. available from this region. In seismically active regions of the

Fig. 1. (a) DEM of the area around NW Himalaya showing prominent NNW–SSE striking frontal foreland fold — the Janauri anticline. Inset shows map of India with location of Janauri anticline and study area, (b) Profile AA` is across the Hajipur fault in the northwestern fringe of Janauri anticline, (c) BB` is drawn in the central part of Janauri anticline, and (d) CC` is across the southern fringe showing the Frontal Piedmont Thrust. HFT — Himalayan Frontal Thrust, BT — Back Thrust, SnT — Soan Thrust and NaT — Nalagarh Thrust. J.N. Malik et al. / Tectonophysics 483 (2010) 327–343 329 world, active faults are considered to be the source for large 2. Geomorphology magnitude earthquakes, and the paleoseismic investigations along such faults have proved their capability in producing large earth- 2.1. Geomorphological setting and active fault distribution quakes periodically (e.g. Nakata, 1989; McCalpin, 1996; Yeats et al., 1997; Meghraoui and Doumaz, 1996; Oatney et al., 2001; The area along the NW Himalayan foothill zone shows three major Meghraoui et al., 2003; Malik and Nakata, 2003; Pantosti et al., geomorphic zones (Figs. 1 and 2) from north to south. These zones are 2004; Malik and Mathew, 2005; Lavé et al., 2005; Kumar et al., bounded by major fault lines (Fig. 1a). The longitudinal intermontane 2006; Kaneda et al., 2006; Yeats and Hussain, 2006). It is therefore valley — Soan Dun (Dun= valley) is the northern most major extremely important to have precise active fault map in the region geomorphic unit in the study area. The Soan Dun is confined between like Himalaya, where not much information is available on the the Lower Siwalik Hills to its north and the Sub-Himalayan range (Upper distribution of active faults. Because without such studies the Siwalik) in south. The boundary between the Lower Siwalik Hills and hazard posed by these faults may be underestimated. Soan Dun is marked by Nalagarh Thrust (NaT) and the southern limit by The studies on active tectonic deformation in the Himalayan frontal Back-thrust (BT) along the back-limb of Janauri anticline. The Sub- zone from Nepal and India have revealed occurrence of uplifted-tilted Himalayan range marked by the Janauri anticline represents the late Pleistocene and Holocene fluvial terraces and alluvial fan surfaces, youngest foreland fold demarcating the southern boundary the with prominent fault scarps ranging in height from 5 to 50 m resulted Himalaya with respect to the Indo-Gangetic Plain (IGP) to its south. due ongoing active deformation along the Himalayan Frontal Thrust This vast flat alluvial plain (IGP) represents the present foreland basins (HFT), Main Dun Thrust (MDT) and the Main Boundary Thrust (Nakata, 1972; Powers et al., 1998; Malik and Mohanty, 2007). (MBT) (Nakata, 1972, 1975; Valdiya, et al., 1984; Nakata, 1989; Nakata The boundary between the Janauri anticline and Indo-Gangetic Plain is et al., 1990; Valdiya, 1992; Yeats et al., 1992; Mugnier et al., 1998; marked by Himalayan Frontal Thrust (HFT). Wesnousky et al., 1999; Lavé and Avouac, 2000; Malik and Nakata, The Sutlej and Beas Rivers emerging from higher Himalayas are the 2003; Malik et al., 2003; Mugnier et al., 2004). However, still there are major drainage in the region (Figs. 1–3). The Beas River borders to the several areas particularly in NW Himalaya were very little information northern fringe of the Janauri anticline and Sutlej River to its south is available. before debauching on the Indo-Gangetic Plain. The growth of the Along with active fault identification it is important to know the 100 km long Janauri anticline has influenced the flow paths of these pattern of deformation, which in turn, helps in understanding the major rivers. The flat topped uplifted surface in the central part of the overall evolution of the landscape and also towards identifying the anticline marks the paleo-water gap of Sutlej River and a linked-up geometry of the fault related fold segments. Frontal fault-propaga- segment formed by the linkage of two smaller fault segments (Malik tion fold growth in forward as well as lateral directions are and Mohanty, 2007). commonly noticed in active fold-and-thrust belt (e.g. Mueller and Talling, 1997; Delcaillau et al., 1998; Champel et al., 2002; Delcaillau 3. Active fault distribution along Janauri anticline et al., 2006; Malik and Mohanty, 2007; Simoes et al., 2007). Lateral propagation of fault and related development of fold to some extent Several traces of active fault scarps were identified in the central has been attributed to slip along the fault during major earthquakes portion along the Janauri anticline by Malik and Mohanty (2007),butno (Walsh et al., 2002). It has been suggested that fault and associated ground truthing was carried out. In this study re-interpretation and fold grows by radial propagation and linkage of several smaller fold- ground truthing was carried out in the central portion and several new segments develops an elongated fold or anticline (Catwright et al., active fault traces were identified in the central, and along the 1995; Davis et al., 2005). Development of elongated folded segments northwestern and southeastern fringes of Janauri anticline (Fig. 2b). and lateral propagation results in fluvial diversion in fold-and-thrust Most prominent fault traces (HF1 and HF2) were observed from the belt, hence helps to rebuilt the landscape history (e.g. Be´s de Berc northwestern fringe of the anticline on the left bank of Beas River (Figs. 2 et al., 2005; Champel et al., 2002; Burbank et al., 1999; Burbank and and 3). Some discontinuous traces were observed from the central Anderson, 2001). portion along forelimb and backlimb of the anticline (Figs. 2a and 8). Keeping this in mind we focused our present study along the These fault traces on the surface are discontinuous, but probably frontal foreland fold — Janauri anticline (30°45′–32°00′ N Latitude, connects subsurface. The discontinuous pattern could be due to the rapid 75°45′–76°35′ E Longitude) emphasizing towards (1) mapping and degradation as well as burial of the ground deformational features along documenting the traces of active faults, and (2) understanding dynamic range fronts. These fault traces have displaced late Pleistocene- the segmentation relationship based on remote sensing and field Holocene floodplain surface along the northern fringe and central part of observations. The study area falls under meizoseismal zone of 1905 the Janauri anticline as well as alluvial fan deposits (Fig. 2b). In the Kangra event (Fig. 1). Apart from some preliminary information southeastern fringe of the Janauri anticline, uplift has been observed in available on active faults (Nakata, 1972; Malik and Nakata, 2003; the Piedmont Zone (Figs. 2a and 9). Malik and Mohanty, 2007), no attempt has been made to map active faults from this region. In this paper we report several newly 3.1. Active fault along HFT in northwestern fringe of Janauri anticline identified active fault traces and attempted to propose a model to explain the pattern of ongoing deformation. For identification of Two active fault traces striking NNW–SSE, parallel to the trend of the active faults and related landforms, along with high resolution Himalayan arc were identified along the northwestern end of the Janauri declassified CORONA KH-4B satellite data (stereo pair) with ground anticline, named as Hajipur fault (Figs. 1–5 and refer profiles e-h in resolution of approximately 6 feet acquired during 28 September Fig. 2). These faults (HF1 – in the front having boundary between the 1971, Shuttle Radar Topographic Mission (SRTM) 3 arc second data Indo-Gangetic Plain and HF2 – towards the hinterland side) have with resolution of about 90 m and SOI (Survey of India) topo- vertically displaced and warped the late Pleistocene to Holocene graphic maps (scale 1:50,000) were used. Digital Elevation Model floodplain deposits of the Beas River, made up of gravel and sandy (DEM) extracted from SRTM was utilized to construct the terrain lithounits (Figs. 2a–5). Vertical displacement is revealed by well profiles — to understand the morphology of the landscape and developed southwest facing fault scarps ranging in height from 5 to prominent breaks in the terrain (Fig. 1a–d). To confirm the pattern 15 m (Fig. 2b). Distinct back-tilting of the uplifted floodplain surface was offaultingandmostrecentearthquakeeventweexcavatedatrench observed along HF2 near the range front (Fig. 2a refer profile g and 4a). across a branching fault of HFT in the northern fringe of the Janauri The HF1 and HF2 faults are about 2.5 km apart, marked by prominent anticline. step like topography; this is well revealed in the topographic profiles — 330 J.N. Malik et al. / Tectonophysics 483 (2010) 327–343

Fig. 2. (a) Mosaic of CORONA photos of the frontal foreland fold — Janauri anticline. The Sutlej River in the southeast and the Beas River in the northwest defines the edges of the Janauri anticline. Black boxes show the location of Figs. 3a, 6a, 8a and 9a. The forelimb of anticline in the piedmont zone marks boundary with low-lying Indo-Gangetic Plain. Topographic profiles extracted from DEM across the fault scarps identified in the central part — a and b in along the forelimb, c and d along the backlimb, e and f across HF1 and, g and h across HF2. (b) Generalized geomorphic map of the study area along Janauri anticline. The alluvial fans (AF) occur as coalesced fans at the base of front. The flat-uplifted surface in the central portion of the Janauri anticline marks the paleo-water gap of the Sutlej River. Two parallel active faults (Hajipur faults) propagating towards NW have been responsible for the deflection and shift of the Beas River further northwest. J.N. Malik et al. / Tectonophysics 483 (2010) 327–343 331

Fig. 2 (continued). 332 J.N. Malik et al. / Tectonophysics 483 (2010) 327–343

Fig. 3. (a) Close-up of CORONA photos of the northern fringe of the Janauri anticline showing two traces of newly identiﬁed active faults HF1 and HF2, named as Hajipur fault.Yellowboxmarksthe location of Fig. 4a. Open arrow shows direction of lateral propagation of the faults. (b) Fault scarps associated with HF1 near Siprian and Bamonwal village. The height of the scarp is about 15 m with gentle free-face. The total 15 m height is a cumulative height indicative of long-term deformation along HF1, and (c) NW–SE striking fault scarp along HF2 near Hajipur village. The movements along this fault have displaced the ﬂoodplain deposits of Beas River resulting into 6 to 8 m high scarp. The scarp along HF2 trace shows less dissected morphology. J.N. Malik et al. / Tectonophysics 483 (2010) 327–343 333

Fig. 4. (a) Stereo-pair of CORONA photos of the area around Siprian and Hajipur village. The HF1 and HF2 fault traces are shown by black arrows. The height of the fault scarp is much higher along HF1 as compare to that along HF2. The HF1 scarp morphology is diffuse and degraded by more erosion (refer to Fig. 3a for location), and (b) Geomorphic sketch prepared from the above CORONA photo interpretation. Two levels of ﬂuvial surfaces (T1 and T2) are displaced along the HF1 and HF2 faults.

AA′ drawn across these faults (Fig. 1a and b). The HF1 fault extends for near Bamonwal–Siprian village, reduces up to 8 m along the strike and as about 8 to 8.5 km and HF2 for about 10 to 10.5 km (Figs. 2b and 3a). The low as up to 2 to 3 m before it die out towards NW (Figs. 3a and 4). The scarp height ranging from 10 to 15 m was observed along the HF1 fault scarp height along HF2 ranges from 6 to 8 m near the range front, which

Fig. 5. (a) 3D GPR profile collected across the HF2 fault near Hajipur village with 200 MHz antenna (refer to Fig. 3a for location). Data collected in a 22 m long and 10 m wide grid revealed a low-angle thrust fault displacing the near sub-surface sediments of older floodplain of Beas River. Fault was traceable up to the depth of about 6 m from the surface with prominent georadar reflection between 0 m and 12 m horizontal marker. (b) SW facing active fault scarp (∼5 m high) along HF2 at Sandhwal village. Trenching site is shown by black arrow and red arrows show trace of fault. For location refer to Fig. 3a. (c) Northwall trench section excavated across HF2. (d) Interpretation with fault traces and stratigraphic units on northwall of trench excavated across HF2 fault scarp. F1, F2, F3 and F4 are the thrust faults dipping in NE direction. Latest event has been observed along F1, F2 and F3 displacing the units a, b, c and d. 334 J.N. Malik et al. / Tectonophysics 483 (2010) 327–343

Fig. 5 (continued). is comparatively less than measured along HF1 (Figs. 3a, b and 4). 3.1.1. Ground Penetrating Radar survey and trench investigation Similarly reduction in height along the strike as seen along HF1 was also Ground Penetrating Radar (GPR) profile was acquired across noticed along the HF2 fault trace (Figs. 2b, 3a, c and 4a). Satellite data Hajipur fault (HF2) to confirm the near sub-surface faulting (Fig. 3a). interpretation, topographic profiles as well as field survey suggests that A 200 MHz antenna with SIR 3000 GSSI system was used to collect the surface manifestation of both the faults die out along the strike as we 22 m long GPR profile. To get better cross-sectional view of the fault move away from the hill range in NW direction, this is well justified by geometry 3D data with 22 m×10 m grid was collected (Fig. 5a). the gradual reduction of the scarp heights along the HF1 and HF2 faults Prominent inclined georadar reflections were identified between 0 m (Figs. 3a and 4). The fault scarp morphology along HF1 is much more and 12 m horizontal marker (Fig. 5a). The inclined reflections mark a diffused and degraded as compared to HF2 (Figs. 3a and 4). Also the scarp low-angle thrust fault strand with fault plane dipping towards NE. along HF2 has relatively lesser height and less dissected topography as This clearly suggests that even this part of the Himalayan front along compared to that along HF1 (Figs. 3a, c and 4a). The diffused morphology HFT has been ruptured during historic past as observed in other of the HF1 suggests more erosion and probably an older scarp, whereas locations from paloeseismic investigations (Lavé et al., 2005; Malik the younger movement has been taken up by the HF2 fault showing and Nakata, 2003; Kumar et al., 2006; Malik et al., 2008). sharper and less dissected topography. The gradual reduction in height Along with the GPR survey trench investigation was carried out to of the scarps is attributed to lateral propagation of faults and growth of finally confirm the near surface displacement, to know the pattern of associated folds along strike towards northwest. It is also suggested that deformation/faulting and occurrence of most recent event (Fig. 3a). A the scarps along HF1 and HF2 with more height near the hill range are 16 m long, 1 to 3 m deep and 4 to 5 m wide NE–SW trench was indicative of accumulation of greater displacements on faults as excavated across HF2 (Fig. 5b–d). The height of the SW facing scarp compared to the area near the tip where the faults gradually die out. varies from 5 to 6 m. Five sedimentary units a — older to f — younger This phenomenon of lateral propagation of HF1 and HF2 faults has been were identified. Units a and b are the gravel units, about 3.0 m thick responsible for the northward deflection–diversion of Beas River (Figs. 2 comprise rounded to sub-rounded poorly sorted cobble-pebble, and 3). The geometric occurrence of these faults indicates phenomenon weakly stratified fining upwards sequences with sandy matrix. Unit of imbricated fault system, most commonly observed in fold-and-thrust a is marked by coarse clasts and b mainly contains pebble clasts. belts. The morphological characteristics and length of both the faults These units represent deposition by a coarser bed-load stream under suggest that HF2 fault is more active as compare to the HF1 fault. channel-fill environment. Unit c consists of medium to fine sand J.N. Malik et al. / Tectonophysics 483 (2010) 327–343 335

Table 1 Optically-stimulated luminescence ages from trench excavated across HF2 — Hajipur fault along Himalayan Frontal Thrust, NW Himalaya.

Sedimentary units in trench Samplea Grain size De (Gy) U ppm Th ppm K (%) Dose Rate (Gy/Ka) Age (ka)

Unit e HT-1 Course grain 1.75±0.3 4.93±0.94 7.62±3.1 1.7±0.04 3.2±0.3 0.55±0.1 (150±30 µm) Unit d HT-4 Course grain 4.3±0.1 3.63±0.75 6.91±2.49 1.3±0.04 2.46±0.3 1.75±0.2 (180±30 µm) Unit d HT-8 Course grain 5.11±0.1 3.5±0.76 8.42±2.6 1.6±0.04 2.8±0.3 1.8±0.2 (180±30 µm) Unit d HT-10 Course grain 4.27±0.1 3.47±0.72 7.79±2.47 1.3±0.04 2.5±0.3 1.7±0.2 (180±30 µm)

†‡Equivalent dose (De) computed using minimum plus two sigma, water content assumed to be 10%, cosmic ray dose 150 micro gray per year. Dating was carried out at Physical Research Laboratory, Ahmedabad, India. a Refer trench section to Fig. 5d for sample location.

(∼0.5 m) with scattered gravel (pebble) clasts overlying the unit b SSE trending scarp was identified near Bhatpur village (Fig. 6a, b, d, and represents colluvial wedge. Unit d is a thick (∼1.5 m) medium to refer profile b in Fig. 2a). The fault trace extends for about 4 km in length, coarse sandy unit capping the units b and c. Its lower part comprises has displaced the alluvial fan surface comprising well-rounded pebble- more clayey silt package, whereas, medium to coarse sand along with cobble debris deposits in the proximal part. The vertically displaced fan sparsely scattered gravel clasts in the middle and upper portions. This surface is marked by 15 to 20 m high SW facing scarp (Fig. 6b and d). The unit marks deposition under overbank deposition. The contact streams crossing the active front exhibits deeply entrenched narrow between the gravel unit b and overlying unit d is sharp and irregular. channels, and formation of paired terraces close to the front (Fig. 6a–d). The unit e made up of medium to coarse sand with scattered gravel Two set of paired terraces were observed around Bhatpur (Fig. 6b). clasts caps the units b and d. This unit shows abundant scattered Further north near Jaijon village Panjolanwala Khad (Khad=stream) gravels as compared to the underlying unit d. The contact is irregular– show very similar evidence of paired terraces (Figs. 6a, 7a and b). Here the erosive suggestive of deposition in channel fill environment. Finally, fault has displaced the fan surface giving rise to 15 to 18 m high SW facing the sequence is capped by loose sandy material with few gravel clasts scarp, most prominent was observed along the left bank. Along the left unit f, suggests artificial fill. bank in the upstream side close to the front the river has incised the Displacement has occurred along NE dipping thrust faults — F1, F2, F3 channel-fill deposits (late Pleistocene-Holocene age e.g. Valdiya, 2003; and F4. The dip of F1 varies from ∼24° at a depth in the northeast of trench Malik and Mohanty, 2007) along with the underlying southerly dipping and graded to ∼8° to almost horizontal in the southwest near surface, Upper Siwalik succession giving rise to strath terrace. Total incision of whereas, F2 and F3 shows fault dip from 24° to 15°, the fault F4 shows about 10 to 12 m was observed (T1-surface), which includes the bed-rock slightly higher angle of about ∼45°. F1 has displaced units b and d by about incision 8 to 9 m along with the overlying 2 to 3 m thick late Quaternary 5 m, and F2 and F3 have displaced units a, b, c and d.Nearsurface channel-fill deposits (Fig. 7c). The T2-surface was about 5 to 6 m from the displacement of these units ranges from 0.5 m to 0.75 m. Looking to the top of the T1-surface, giving a cumulative incision of about 15 to 18 m pattern of vertical stacking of the gravel clasts in units a and b it is (Fig. 7aandc). suggested that more than one events have occurred along the HF2. F1 marks the main fault with maximum displacement and other are the 3.3. Active fault along backlimb in the central of Janauri anticline subordinate faults. The deformation pattern also indicates that major part of the deformation has been consumed by folding. The front along the backlimb of the Janauri anticline marked by OSL (optical stimulated luminescence) ages obtained from four back-thrust provides excellent example of slip-partitioning along in samples from the northwall of trench succession range from 1.8± the sub-Himalayan zone. The north dipping thrust has displaced the 0.6 ka to 0.55±0.1 ka (Table 1). Unit d yielded age of 1.7 to 1.8 ka, fluvial terraces as well as coalesced alluvial fan surfaces (Figs. 2a, b, 8a– and the overlying unit e gave an age of 0.5 ka (Fig. 5d). Taking into e). Most prominent fault traces trending NNW–SSE were observed consideration pattern of displacement and stratigraphic relationship between Palata and Bathu villages (Fig. 8a–e, and refer profile c in our preliminary interpretation suggests at least two events have Fig. 2a). Two parallel trace of active fault scarps were noticed near occurred along the HFT in this region with manifestation of surface Palata and Supalwan village (Fig. 8a, b, e and f). These faults extend for faulting along HF2. The Event-I occurred before the deposition of unit about 2 to 2.5 km, have displaced the alluvial fan surface resulting in c and d, and after the deposition of unit b. During Event-I gravel unit NE facing scarps (Fig. 8a, b and e). The alluvial fan surface is seen (a and b) was displaced along F1 and its subordinate faults. The displaced in proximal as well as in the distal end parts. Two distinct colluvial wedge (unit c) deposited after this event only remained levels (L1 and L2) of uplifted surfaces were observed along the fault preserved in the upper portion of the scarp. Later the depositional scarps with height ranging from 8 to 10 m (Fig. 8b, e and f). The took place under overbank environment, could be attributed to streams crossing the thrust-front are marked by narrow deep incised shifting of Beas River to its present position due to the lateral channels (Fig. 8b). Another prominent fault scarps were observed propagation of the HF2. The latest Event-II occurred after the around Bathri village (Fig. 8a, c, d and g). Here two parallel fault scarp deposition of unit d and before the deposition of unit e, i.e. between traces of about 2 to 4 km in length, trending NNW–SSE have displaced 1.7 ka and 0.5 ka. the fluvial surface resulting in formation of NE facing scarps ranging in height from 12 to 15 m (Fig. 8c and g). Displacements along these 3.2. Active fault along HFT (forelimb) in central part of Janauri anticline faults have resulted into two level uplifted surfaces (L1 and L2) (Fig. 8a and g). Back-tilting was noticed at one location southwest of Bathri Active fault traces facing the Indo-Gangetic Plain were delineated (Fig. 8c and refer profile d in Fig. 2a). This fluvial terrace is a part of the between Jaijon and Bhudia-Pau villages in the central portion of Janauri flat-uplifted surface with thick gravel deposit, suggestive of older anticline (Fig. 6a and in Fig. 2a refer profile a). Whereas, further southeast floodplain of the paleo-Sutlej River, which flowed through this area in no prominent traces were observed other than the topography revealing the past. Further northwest distinct convex slope along the edge of the warped surfaces and sharp linear fronts. These active faults extend with front was noticed between Bathu and Mankot with prominent scarp variable length ranging from 1 to 4 km (Fig. 6a). The most distinct NNW– around Taliwal (Fig. 8a, h). We interpret this slope as a flexural or 336 ..Mlke l etnpyis43(00 327 (2010) 483 Tectonophysics / al. et Malik J.N. – 343

Fig. 6. (a) Contour map showing distinct topographic variations in the central part along the forelimb of Janauri anticline, between Bhudia Pau and Lalwan village. Discontinuous traces of active faults were identiﬁed around Bhatpur, Jaijon and Lalwan villages, (b) Stereo-pair of CORONA photo showing occurrence of fault scarp around Bhatpur (refer to Fig. 6a for location). The NW–SE striking scarp is well marked by uplifted paired-terrace close to the front. The fault scarp extends for about 4 km along the strike, height of the scarp ranges from 15 to 20 m. The streams crossing the front are marked by deeply incised narrow valleys, (c) Geomorphic map showing major landforms in the area. Paired terraces are seen along the frontal part. T1 — younger terrace, T2 — older terrace. AF — marks the active alluvial fan surface, and (d) View of fault scarp at Bhatpur village. Faulting has displaced proximal part of the alluvial fan surface giving rise to SW facing scarp (15 to 20 m). Dotted circle shows the person standing at base of the scarp with 1.5 m height. Fault trace is marked by white arrow. ..Mlke l etnpyis43(00 327 (2010) 483 Tectonophysics / al. et Malik J.N. – 343

Fig. 7. (a) Stereo-pair of the area around Jaijon village along the frontal part of Janauri anticline (refer to Fig. 6a for location). Fault trace is shown by arrows. The occurrence of terraces and high degree of incision in the alluvial fan material close to the front suggests displacement along the active fault. The fault trace further NW is marked by sharp front and prominent geomorphic boundary between the hill range and Indo-Gangetic plain. The fault extends for about 1 to 1.5 km, (b) Geomorphic sketch prepared from the CORONA photo interpretation showing major landforms. Paired terraces are noticed along the frontal part along the HFT. T1 — younger terrace and T2 — older terrace. Active fault trace is marked by arrows, and (c) Incised section along the left bank of Panjolonwala Khad shows occurrence of strath terrace (T1) and valley fill terrace (T2). The T1 terrace cliffy bank is about 12 m, where river has incised about 2–3moffluvial deposits and 8 to 9 m of Upper Siwalik succession (bedrock). White broken line show the bounding surface of the channel-fill troughs with respect to the underlying Upper Siwalik succession. Total incision of T1 and T2 is about 15–18 m. 337 338 ..Mlke l etnpyis43(00 327 (2010) 483 Tectonophysics / al. et Malik J.N. – 343

Fig. 8. (a) Contour map of the area along the back-limb in the central part of the Janauri anticline showing prominent traces of active fault scarps between Palata and Supalwan village, and around Bathari and Bathu. Distinct warping was observed near Bathu village and further up to Mankot, (b) Stereo-pair of the area around Palata and Supalwan village. Two active fault traces with NE facing scarps are marked by arrows, (c) Stereo-pair of the area around Bathri village showing traces active faults displacing the ﬂuvial surface giving rise to NE facing fault scarps (refer Fig. 6a for location). (d) View of NNW–SSE striking fault scarp near Bathri village, (e) View of displaced fan surface in the distal part near Supalwan village, (f) Geomorphic map showing displaced alluvial fan surfaces along the Back Thrust. Fan surface is displaced along two fault parallel traces resulting in two northeast facing scarps. L1 and L2 represents the two level of surface, (g) Fluvial surface, part of ﬂat-uplifted surface has been displaced along two parallel fault traces giving rise to northeast facing scarps. L1 and L2 represent the two level of surface. (h) stereo-pair of the area around Taliwal village showing warping and active fault scarp trace (marked by arrows). T1 — younger terrace and T2 — older terrace. J.N. Malik et al. / Tectonophysics 483 (2010) 327–343 339

Fig. 8 (continued). warping scarp caused by thrust faulting beneath the scarp. The anticline formed as a result of movements along Frontal Piedmont Thrust occurrence of two parallel traces of active fault along the front are (FPT). The hill range trending NNW–SSE extends laterally for about 7 to interpreted as the branching out imbricated faults, and the flexure 8 km between Rel Majra and Mauhar (Figs. 2a–b, 9a–b). It is marked by northwest to Bathu probably points toward the change in dip of the gullied surface, relatively less dissected compare to the Janauri anticline. fault plane from high to low along the strike of the fault. Such variable It extends in E–Wdirectionforabout3to4.5km(Figs. 2a and 9a). manifestation of the deformation on the surface is common along the The height of the ridges ranges from 10 to 20 m. Along the strike the fold-and-thrust belt in Himalaya (Malik and Mathew, 2005). height of the range is variable, at places near Retwal village the range is marked by higher elevation (Fig. 9b), whereas around Mauhar village it 3.4. Uplift in Piedmont Zone along the southeastern portion of Janauri reduces and die out further NW. The streams flowing across this range anticline exhibits well developed terraces and at places channel is marked by deep incision along the course (Fig. 9a–b). The uplifted piedmont sediments The Piedmont Zone is a part of the Indo-Gangetic Plain made up of and evolution of this growing young hill range is a result of southward coalesced alluvial fan deposits, drained by the streams originating from propagation of tectonic activity and movements along FPT which the forelimb side of the Janauri anticline, finally joining the higher order represents an emergent imbricated thrust branching out from the main channel of Sutlej River (Figs. 1a, 2a–b). Younger hill range was main HFT system (Figs. 2a–b, 9a–b). Similar evidence of uplift in the observed in the piedmont zone around southeastern end of the Janauri piedmont zone has been observed around the foothill zone of Dehra Dun 340 J.N. Malik et al. / Tectonophysics 483 (2010) 327–343

Fig. 9. (a) CORONA photo showing the uplift in the piedmont zone due to movement along Frontal Piedmont Thrust (FPT). The uplifted gullied surface extends for about 7 to 8 km between Rel Majra and Mauhar village, and (b) A view of active fault scarp in the piedmont zone near Retwal village along FPT (refer the topographic proﬁle CC` in Fig. 1d).

(Thakur, 2004). These observations provide support to the model that 2007). In this phenomenon it has been suggested that (1) the tectonic large-to-great earthquakes originated in the locked part of the activity (faulting) initiates at the location above the pre-existing fault detachment and propagated southward to the range front, producing system with a nucleation close to the centre of each fault, (2) as dis- surface–ruptures, fault scarps and uplifts in the Gangetic Plain (Thakur, placement occurs during major earthquake - fault grows, propagates 2004). laterally by acquires more length, and (3) the propagating fault segments either overlap or get linked-up giving rise to one single large segment 4. Discussion (Walsh et al., 2002; Champel et al., 2002; Davis et al., 2005). The new active fault traces identified along the northern, central The phenomenon of fault related fold growth, lateral propagation and and southern portion of the Janauri anticline provided ideal oppor- fault segmentation-linkage in many tectonically active region have played tunity to understand the pattern of ongoing tectonic deformation in pivotal role in shaping the landscape (e.g. Delcaillau et al., 1998; Burbank the frontal part of the Himalayan arc. The active fault distribution and and Anderson, 2001; Davis et al., 2005; Be´s de Berc et al., 2005; Malik and associated geomorphic features revealed that the evolution of Janauri Mohanty, 2007), and could be considered as a source for future anticline is not only related to one single fault segment, but more than earthquakes. Several experimental as well as field based studies from one fault segments were responsible for its development (Figs. 2a–b normal faulting environment have given remarkable understanding and 10). The occurrence of fault scarps along the forelimb and back- towards the phenomenon of fault-growth, fault segmentation and limb of the Janauri anticline suggests that the slip accommodated in segment linkage, which in turn also helped in understanding the scaling the frontal part along the HFT system is partitioned between the relationship between the displacement (D) on fault and length (L) of the main HFT and associated back-thrust (Figs. 1–8). The prominent fault fault (e.g. Cartwright et al., 1995; Walsh et al., 2002). In recent years some scarps extending in length up to 4 km around Bhatpur, and 1 to 2 km studies have proved that the lateral propagation of faulting-and-folding, around Jaijon and Lalwan along the forelimb suggests that Himalayan fault-growth and segment linkage is also most commonly observed front had ruptured in the past (Figs. 6a–d and 7a–c). The fault scarps phenomenon in the active thrust-and-fold belt region (e.g. Mueller and heights up to 20 to 25 m and occurrence of paired alluvial-fill as well Talling, 1997; Delcaillau et al., 1998; Burbank et al., 1999; Burbank and as strath terraces (Figs. 6a and 7a–c) are suggestive of cumulative Anderson, 2001; Champel et al., 2002; Be´s de Berc et al., 2005; Davis et al., uplift and ongoing long-term deformation along the fault. Similar 2005; Delcaillau et al., 2006; Malik and Mohanty, 2007; Simoes et al., evidences of occurrence of fault scarp traces along the backlimb side J.N. Malik et al. / Tectonophysics 483 (2010) 327–343 341

and ongoing deformation. Along the backlimb side we identified more than one line of fault scarp traces. The occurrence of these parallel to sub-parallel fault scarp traces suggest propagation of tectonic activity towards hinterland side in the Soan Dun, which represent imbricated thrusts. It is suggested that the shortening in the frontal part is ab- sorbed by the main HFT and back thrust (BT). In the southern portion of the Janauri anticline the uplifted piedmont zone marked by dissected landform (Fig. 9a, b) suggests that the tectonic activity has propagated towards foreland along the newly developed range front registering movement along Frontal Piedmont Thrust (FPT). The FPT represents an imbricated emergent thrust that belongs to the HFT system. Similar phenomenon of uplift has been also noticed in the region west of the study area from the piedmont zone of Dehra Dun hills (Thakur, 2004). Also, the most prominent two active fault traces —“Hajipur fault” (HF1 and HF2) along the northern fringe of Janauri anticline provided an excellent example of lateral propagation of faulting along HFT and relation of fault and associated fold growth (Figs. 2a and 3a). The movements along these faults are well repre- sented on the surface in form of SW facing fault scarps formed due to vertically displaced floodplain deposits of Beas River (Figs. 2b, 3a and 4). Also the gradual reduction of the height of the scarp in northwest clearly points towards northwestward propagation of these faults, which forced Beas River to shift towards northwest forming huge ‘U’ shape turn (Figs. 2b, 3a and 4). An alternative interpretation could be that the Beas River during the period of tectonic movements i.e., lateral propagation of the HF1 and HF2 was not capable enough to cut through the uplift along these active faults, and had low energy conditions causing lateral shifting-deflection to its present position. 3D GPR profile further helped us in identifying the evidence of low- angle fault (thrust fault) dipping NE along HF2 (Fig. 5). This was also confirmed from the trench investigations across HF2, which revealed clear displacement along low-angle thrust faults. Preliminary interpretation suggests at least two events have occurred during recent historic past, with the latest one (Event II) during 1.7 to 0.5 ka registering displacement of more than 3 m during one single event. The historic record from the surrounding area suggests occurrence of major earthquake during 1555 AD Kashmir event and the paleoseismic studies from the Chandigarh region located about 150 km southeast of the study area suggests evidence of occurrence of large magnitude event during 1400–1500 AD (Malik et al., 2008). Consid- ering the above information it is quite possible that the latest event (Event II) in our trench might have occurred during 1500 AD (?). The only present convergence rate available from this region is from the recent GPS measurements collected during the period from 1995 to 2000 (Banerjee and Bürgmann, 2002). The rate of shortening observed across 100 km long transect between the frontal Himalayan zone (sub- Himalaya) and the Higher Himalaya was 14±1mm/yr,alsobasedon restoration of balanced geological cross-sections similar rate of 14± 2 mm/yr was deduced across the Kangra reentrant for 140 km long transect (Powers et al., 1998). It has been suggested that at present HFT is locked and have showed no movement during the period of observation, and the major portion of the slip is accommodated by the faults to the north of sub-Himalayan foothill zone (Banerjee and Bürgmann, 2002; Fig. 10. (a) Stage I: Fault related fold growth initiated along the smaller segments along NW Malik and Mohanty, 2007). The present study along the frontal zone Himalayan frontal viz. CS — the Chandigarh anticline Segment; JS1 — the southern Janauri suggests that HFT had observed slip during recent historic past as segment; and JS2 — the northern Janauri segment. Gaps between the growing folds allowed indicated from the trenching data and traces of active fault scarps. the rivers to flow through, (b) Stage II: The lateral propagation of the growing folds resulted The 100 km long Janauri anticline ridge represents a linked into linkage of JS1 and JS2 segments. Uplift of the linked segment caused disruption and deflection of Sutlej River, and (c) Stage III: Due to sub-surface structural asperity the JS1 segment formed due to inter-linking of two fault segments; the segment does not linked up with the CS segment. The tectonic activity propagated towards linked segment marked by flat-uplifted surface in the central portion foreland along newly developed — Frontal Piedmont Thrust (FPT). Due to no structural asperity represents the paleo-water gap of the Sutlej River (Malik and in the northwestern end the tectonic activity was transferred and taken-up by two parallel Mohanty, 2007). Taking into consideration the evidences of active to sub-parallel young active faults (Hajipur Fault) branched from the main JS2 segment. The lateral propagation and movements along HF1 and HF2 resulted into shift of the Beas River. faults along Janauri anticline and models of lateral propagation of faults and segment linkage suggested by Malik and Mohanty (2007) around Palata, Bathu and Bathri (Fig. 8a–g) are indicative of parti- and Delcaillau et al. (2006), an attempt has been made to reconstruct tioning of slip from the main Himalayan Frontal Thrust (HFT). Also the the phases of evolution of Janauri anticline along the frontal zone scarp heights ranging from 8 to 25 m represent the cumulative uplift (Figs. 2a–b and 10a–c). Stage I: Smaller segments along NW Himalayan 342 J.N. Malik et al. / Tectonophysics 483 (2010) 327–343 frontal viz. CS — the Chandigarh anticline segment; JS1 — the southern Acknowledgements Janauri segment; and JS2 — the northern Janauri segment, started growing (Fig. 10a). The growing folds allowed the rivers to flow through JNM pays his due respect and gratitude to Prof. Nakata, Hiroshima the gaps available between them. Stage II: The lateral propagation of the University, Japan for constant encouragement and support to undertake growing fault related fold resulted into linkage of JS1 and JS2 segments. this research along Himalaya. Financial support provided by Ministry of The linked portion experienced rapid uplift, causing upliftment of Sutlej Earth Sciences (MoES) and Department of Science and Technology (DST), River bed along with disruption and deflection Sutlej River (Malik and New Delhi is duly acknowledged. Authors are thankful to Ashutosh Mohanty, 2007)(Fig. 10b). The high (rapid) degree of activity in the Kumar, Prashant Mishra and Arvind Pandey for their help. We are grateful linked area is well manifested by the flat uplifted surface in the central to Ashutosh Kumar, both the anonymous referees for providing valuable portion of the Janauri anticline (Figs. 1 and 2). During this stage the comments and suggestions, which helped us in improving the manu- southeastern end of the JS1 segment has not been linked-up with the script. We are also grateful The Editor for keeping belief in us and for give a northwestern end of the CS. Stage III: It is suggested that due to sub- chance to revise the manuscript. surface geological asperities the tectonic activity along the Himalayan front was transferred further south towards the foreland along the References newly developed Frontal Piedmont Thrust (FPT) (Figs. 1, 2, 8 and 10c). Whereas, probably due to no presence structural asperity on Banerjee, P., Bürgmann, R., 2002. Convergence across the northwest Himalaya from GPS measurements. Geophysical Research Letter 29 (13), 30-1–30-4. the northwestern end of the Janauri anticline resulted into further Be´s de Berc, S., Soula, J.C., Baby, P., Souris, M., Christophoul, F., Rosero, J., 2005. northwest propagation of fault related fold (Figs. 2, 3 and 10c). The Geomorphic evidence of active deformation and uplift in a modern continental northwestward propagation of activity in this part was transferred wedge-top-foredeep transition: example of the eastern Ecuadorian Andes. Tectonophysics 399, 315–350. and taken-up by two parallel to sub-parallel young active faults Burbank, D.W., Anderson, R.S., 2001. Tectonic Geomorphology. Blackwell Science, branched from the main JS2 (Figs. 4a, 10c). The lateral propagation p. 274. and movements along these newly identified active faults HF1 and HF2 Burbank, D.W., McLean, J.K., Bullen, M., Abdrakhmatov, K.Y., Miller, M.M., 1999. fl Partitioning of intermontane basins by thrust-related folding, Tien Shan, Kyrgyz- (Hajipur fault) resulted into uplift of the oodplain of Beas River as well stan. Basin Research 11, 75–92. as responsible for the northward shift (Figs. 3, 4a and 10c). Cartwright, J.A., Trudgill, B.D., Manfield, C.S., 1995. Fault growth by segment linkage: an The recent 2005 event triggered along earlier identified Tanda active example for scatter in maximum displacement and trace length data from the – fault (Nakata et al., 1991), has pointed towards the importance of active Canyonlands Grabens of SE Utah. Journal of Structural Geology 17, 1319 1326. Champel, B., van der, B.P., Mugnier, J.L., Leturmy, P., 2002. Growth and lateral fault identification in Himalayan domain where very few studies are propagation of fault-related folds in the Siwaliks of western Nepal: rates, focused for active fault mapping. The evidence of active fault distribution mechanisms, and geomorphic signature. Journal of Geophysical Research 107 – along the Janauri anticline, lateral propagation of fault related folding, (2111), 2-1 2-18. Davis, K., Burbank, D.W., Fisher, D., Wallacec, S., Nobes, D., 2005. Thrust-fault growth linkage of smaller segments giving rise to one single large segment and and segment linkage in the active Ostler fault zone, New Zealand. Journal of diversion of drainage suggests that tectonic activity not only have Structural Geology 27, 1528–1546. implications to the landscape evolution but also towards the potentiality Delcaillau, B., Deffontaines, B., Floissac, L., Angelier, J., Deramond, J., Souquet, P., Chu, H.T., Lee, J.F., 1998. Morphotectonic evidence from lateral propagation of active frontal fold; of producing large magnitude earthquake in future in this region. It is also Pakuashan anticline, foothills of Taiwan. Geomorphology 24, 263–290. suggested that the future rupture along the Hajipur fault will result into Delcaillau, B., Carozza, J.-M., Laville, E., 2006. Recent fold growth and drainage further propagation of the fault towards northwest. Our finding will be development: the Janauri and Chandigarh anticlines in the Siwalik foothills, northwest India. Geomorphology 76, 241–256. helpful in further understanding the ongoing deformation in Himalayan Gansser, A., 1964. The geology of the Himalaya. New York, Wiley Interscience. pp. 189. frontal zone and will form base for detailed paleoseismic investigations in Kaneda, H., Awata, Y., Nakata, T., Tsutsumi, H., Awan, A.A., Hussain, A., Khattak, W., Ashraf, the region. Also several newly identified active fault traces along the M., Yeats, R.S., Baig, M.S., 2006. Extensive surface fault rupture associated with the 2005 Mw 7.6 Pakistan earthquake. Abstract, 3rd Annual Meeting AOGS, Singapore. Janauri anticline will be helpful in seismic hazard assessment of areas Kumar, S., Wesnousky, S.G., Rockwell, T.K., Briggs, R.W., Thakur, V.C., Jayangondaper- marked by increasing population growth in the foothills. umal, R., 2006. Paleoseismic evidence of great surface rupture earthquakes along the Indian Himalaya. Journal of Geophysical Research 111, B03304. doi:10.1029/ 5. Conclusions 2004JB003309. Lavé, J., Avouac, J.P., 2000. Active folding of fluvial terraces across the Siwaliks Hills, Himalayas of central Nepal. Journal of Geophysical Research 105 (B3), 5735–5770. The major findings of the present study are as follows: Lavé, J., Yule, D., Sapkota, S., Basant, K., Madden, C., Attal, M., Pandey, R., 2005. Evidence for a Great Medieval Earthquake (1100 A.D.) in the Central Himalayas, Nepal. – — Science 307, 1302 1305. 1) The 100 km long NNW-SSE striking frontal foreland fold the Janauri Lyon-Caen, H., Molnar, P., 1983. Constraints on the structure of the Himalaya from the anticline is a product of a linked-up segment form due to inter-linking analysis of gravity anomalies and a flexural model of the lithosphere. Journal of of two segments JS1 and JS2. Geophysical Research 88, 8171–8191. Malik, J.N., Mathew, G., 2005. Evidence of paleoearthquakes from trench investigations 2) Occurrence of active fault traces along the forelimb and backlimb across Pinjore Garden fault in Pinjore Dun, NW Himalaya. Journal of Earth System of Janauri anticline in the central portion and less dissected topo- Science 114 (4), 387–400. graphy of the flat uplifted surface (paleo-water gap of Sutlej River) Malik, J.N., Mohanty, C., 2007. Active tectonic influence on the evolution of drainage and landscape: Geomorphic signatures from frontal and hinterland areas suggests partition of slip along the HFT and associated back-thrust in along Northwestern Himalaya, India. Journal of Asian Earth Sciences 29 (5–6), the frontal zone and probable region of rapid uplift. 604–618. 3) Development of Frontal Piedmont Thrust (FPT) suggests propaga- Malik, J.N., Nakata, T., 2003. Active faults and related late Quaternary deformation along the northwestern Himalayan Frontal Zone, India. Annals of Geophysics. 46 (5), tion of tectonic activity towards foreland. 917–936. 4) The lateral propagation and movements along HF1 and HF2 (Hajipur Malik, J.N., Nakata, T., Philip, G., Virdi, N.S., 2003. Preliminary observations from trench fault) are attributed to the uplift of the floodplainaswellasnorthward near Chandigarh, NW Himalaya and their bearing on active faulting. Current – shift of Beas River. Science 85 (12), 1793 1799. Malik, J.N., Nakata, T., Philip, G., Suresh, N., Virdi, N.S., 2008. Active fault and 5) GPR survey confirmed the near sub-surface deformation and paleoseismic investigation: evidence of historic earthquake along Chandigarh displacement of young alluvial deposits along a thrust fault. Fault in the frontal Himalayan zone, NW India. Journal of Himalayan Geology – 6) Trench excavated across HF2 indicates occurrence of at least two 29 (2), 109 117. McCalpin, J.P., 1996. Paleoseismology. Academic Press, New York, p. 588. earthquake and associated surface rupture during recent historic past, Meghraoui, M., Doumaz, F., 1996. Earthquake-induced flooding and paleoseismicity of El with the latest one occurred around 0.5 to 1.7 ka. Considering the Asnam, Algeria, fault-related fold. Journal Geophysical Research 101 (B8), historic and paleoseismic records from the surrounding area it is 17,617–17,644. 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