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GEODYNAMICS & TECTONOPHYSICS / recent geodynamics
Published by the Institute of the Earth's Crust, Siberian Branch, Russian Academy of Sciences /
2020 VOLUME 11 ISSUE 1 PAGES 39-52 ISSN 2078-502X
DOI: 10.5800/GT-2020-11-1-0461
SEISMOTECTONICS OF THE INNER TIENSHAN: SUUSAMYR BASIN AND ADJACENT AREAS A.V. Mikolaichuk1, Z.A. Kalmetyeva2, J.-P. Burg3, D. Fossati34, D.V. Gordeev1
1 Institute of Geology of NAS, Bishkek, Kyrgysstan
2 Central-Asian Institute for Applied Geosciences, Bishkek, Kyrgyzstan
3 Department of Earth Sciences, ETH, Zurich, Switzerland
4 Marti Tunnelbau AG, Moosseedorf, Switzerland
ABSTRACT. The Ms=7.3 Suusamyr earthquake of August 19, 1992 occurred in an area reputedly aseismic. Because it was not expected there, this event attracted worldwide attention of researchers in seismology and seismotectonics, but their results have not been included in the most recent seismic zoning map of Kyrgyzstan. New studies of neotectonic structures and focal mechanisms of earthquakes in the Suusamyr area and adjacent areas give reason to revise the established notions about the seismicity of the region. The seismic hazard in Inner Tienshan appears important and Mmax are comparable to those of the Northern and Southern Tienshan, where numerous destructive events were documented in the XIX and XX centuries. For the southern parts of the study area, along Naryn River, where hydroelectric power stations are planned, the new data should be used.
KEYWORDS: neotectonics; active fault; earthquake mechanism; seismic hazard
FUNDING: The research was supported by SNSF (IB7320-110694).
RESEARCH ARTICLE Received: May 25, 2019
Revised: November 12, 2019 Accepted: December 4, 2019
FOR CITATION: Mikolaichuk A.V., Kalmetyeva Z.A., Burg J-P., Fossati D., Gordeev D.V., 2020. Seismotectonics of the Inner Tienshan: Suusamyr Basin and adjacent areas. Geodynamics & Tectonophysics 11 (1], 39-52. doi:10.5800/GT-2020-11-1-0461
СЕЙСМОТЕКТОНИКА ВНУТРЕННЕГО ТЯНЬ-ШАНЯ: СУУСАМЫРСКАЯ ВПАДИНА И ПРИЛЕГАЮЩИЕ ТЕРРИТОРИИ
А.В. Миколайчук1, З.А. Кальметьева2, Ж.-П. Бург3, Д. Фоссати3,4, Д.В. Гордеев1
1 Институт геологии НАН, Бишкек, Кыргызстан
2 Центрально-Азиатский институт прикладных исследований Земли, Бишкек, Кыргызстан
3 Департамент наук о Земле, Высшая техническая школа, Цюрих, Швейцария
4 Компания «Marti Tunnelbau AG», Мосзеедорф, Швейцария
АННОТАЦИЯ. Суусамырское землетрясение (М=7.3) произошло 19 августа 1992 г. в предположительно асей-смичном районе. Поскольку это событие оказалось неожиданным, оно привлекло внимание исследователей в области сейсмологии и сейсмотектоники всего мира. Однако результаты данных исследований не нашли отражения на последней карте сейсмического районирования Кыргызстана. Новые структурные исследования активных разломов и механизмов очагов землетрясений Суусамырской впадины и прилегающих территорий дают основание пересмотреть сложившиеся представления о сейсмичности региона. Сейсмическая опасность во Внутреннем Тянь-Шане (Ммах) представляется сопоставимой с таковыми в Северном и Южном Тянь-Шане, где были зарегистрированы многочисленные разрушительные события XIX и XX века. Полученные данные желательно учитывать на юге изученной территории, где планируется строительство гидроэлектростанций Нарынского каскада.
КЛЮЧЕВЫЕ СЛОВА: неотектоника; активный разлом; механизм очага землетрясения; сейсмическая опасность
ФИНАНСИРОВАНИЕ: Исследования проведены при поддержке SNSF (IB7320-110694).
1. INTRODUCTION
Recorded seismicity of the Kyrgyzstan Tienshan shows epicenters aligned along narrow linear zones striking N060°-070°. The coincidence of these earthquake lineaments with major faults of the Tienshan Mountains (Fig. 1, a, b) was recognized as early as the first seismotectonic investigations of the 1970s (e.g., [Djanuzakov et al., 1980]). Large destructive earthquakes are often a shock to the population. If specialists have some knowledge on the likely location of future earthquakes, they are still unable to precisely predict when seismic events may occur. This is the case for the M=7.3 1992 Suusamyr earthquake, which was unexpected by both the inhabitants and the earth scientists because, before this event, multiple arguments had been brought forward to conclude that the internal regions of Tienshan are weakly seismic. In particular, the instrumental records supported the assumption that the Suusamyr valley was seismically safe (Fig. 1, c). Because of this dramatic discrepancy between the prevision and the reality, the Suusamyr earthquake attracted worldwide attention of specialists and triggered much work on seismological aspects (e.g. [Djanuzakov et al., 1997; Mellors et al., 1997]) and surface effects in the epicentral area [Bogachkin et al., 1997; Ghose et al., 1997; Havenith et al., 2000; Su Zong-zheng et al., 1999; Ainscoe et al., 2019]. These studies considered seismotectonics and seismicity of the region, but their results have not been included in the most recent seismic zoning map of the Suusamyr area [Abdrakhmatov et al., 2012; Turdukulov, 1996]. This omission can be corrected with information on: (i) data on active faults, (ii) maximal earthquake magnitudes possible on these faults, and (iii) focal mechanisms for earthquakes. This paper addresses these issues.
2. SEISMOGENIC GEOLOGICAL STRUCTURES
The Suusamyr region is located to the NE of the Talas-Fergana sinistral strike-slip fault (Figs. 1 and 2, a) (e.g., [Burt-man et al., 1996]). The dextral Suusamyr-Toluk Fault is parallel to the Talas-Fergana Fault; it is associated with the strongest aftershock (M=6.7) of the 1992 event and makes the south-western boundary of the Suusamyr earthquake source zone. Two sinistral EW-striking Suek and North Suek faults border this zone at the north. The dextral Karakol and North Karakol faults are located in the north-western part of the region (Fig. 2, a). The EW-striking Northern Ka-vak Thrust is the southern boundary of the Suusamyr earthquake source zone (Fig. 2, a).
Paleomagnetic data on Late Paleozoic rocks of Central Tien Shan revealed regional, up to 90° counterclockwise rotation of upper-crust blocks. This rotation is consistent with sinistral wrenching along the EW-striking fault system and dated as pre-Jurassic. Paleomagnetic data from Jurassic and younger rocks show minor, if any, rotation [Bazhenov et al., 1999]. Such rotations evidence that the Late Paleozoic strike-slip faults in Tienshan were not reactivated during the Early Mesozoic. Structural data bring evidence for some of them being reactivated during the Cenozoic [Bazhenov, Mikolaichuk, 2004; Delvaux et al., 2001; Selander et al., 2012]. Sinistral transtension during Oligocene - Early Miocene led to the formation of intermountain basins, such as the Jumgal (Fig. 2, a) and Naryn basins (see Fig. 1, b) and has been inverted to dextral transpression since the Late Pliocene [Morozov et al., 2014]. Dextral movements at a rate of 5-6 mm/year activated the Karakol Fault (Fig. 2, a) over the Late Pleistocene - Holocene period [Makarov et al., 2005]. These observations are consistent with the results of tectonophysical studies. According to the reconstructed
Main quaternary and active faults:
^ Strike-slip fault
Thrust
/ Vertical fault
1997 Earthquake M: 74 epicenter,
year & magnitude
Earthquake maximal shaking areas
Fig. 1. Overview of seismicity and active faults in the Tienshan: (a) - large scale overview of the study area, TFF - Talas-Fergana Fault; MPT - Main Pamir Thrust; (b) - active faults after [Kalmetieva et al., 2009]; (c) - map of the М>4.5 earthquake epicenters from ancient times to August 19, 1992 according to the KIS NAN KR catalogue in the limits of 39.5-43 °N & 70.0-80.0 °E [Kalmetieva et al., 2009]. Beyond these limits USGS data (http://earthquake.usgs.gov) for the period since 1971 year (till the 1992 M=7.3 Suusamyr earthquake) were used.
Рис. 1. Обзорные схемы сейсмичности и активных разломов Тянь-Шаня: (a) - обзорная схема района исследования, TFF-Таласо-Ферганский разлом; MPT - Главный Памирский надвиг; (b) - активные разломы по [Kalmetieva et al., 2009]; (c) - карта эпицентров землетрясений М>4.5 с древних времен до 19 августа 1992 г. по каталогу КИС НАН КР (39.5-43 °N; 70.0-80.0 °E) [Kalmetieva et al., 2009]. Дополнительно использовались данные USGS (http://earthquake.usgs.gov) за период с 1971 г. до момента возникновения Суусамырского землетрясения М=7.3 в 1992 г.
Deposits ,—I Upper Pliocene - Lower
Pleistocene O Mesozoic - Cenozoic O Paleozoic basement
Faults
^ Strike-slip fault Thrust Vertical fault
Paleoseismodislocation
(after A.Strom, 2000, 2009, 2010, 2013)
® Caldera-like collapses ^ Largest landslides and rockslide dams
Suusamyr earthquake epicenters and seismodislocation
(after Bogachkin et al., 1997; Djanuzakov et al., 1997; Mellors et al., 1997; Korjenkov, 2006)
*=73 Main shock ^M=87 Secondary shock
Isoseismal (units MSK)
Sites of structural-geological observation
Equal density isolines _ of the aftershock epicenters.
The figure at the line corresponds to the epicenter quantity for 1km2 for the observation period of 1992-2004
yf1- Ruptures ® Mud eruption
Fig. 2. Neotectonics of the Suusamyr earthquake area (a) and seismotectonic framework of the Suusamyr earthquake source (b). Рис. 2. Неотектоническая схема района Суусамырского землетрясения (a) и сейсмотектоническая структура очага Суусамырского землетрясения (b).
present-day stress state, the Suusamyr and Kochkor intramountain basins are located in the zone of horizontal shear [Rebetsky et al., 2016].
According to instrumental data, the epicenter of the Suusamyr earthquake is in the heads of the West Aramsu and East Aramsu rivers, which are spatially related to the E-W South-Aramsu strike-slip fault and the Kyzyloi thrust (Fig. 2, a). The second, strongest shock came 68 minutes after the main shock on the N-W segment of the Suusamyr-Toluk Fault, where a surface rupture occurred. This rupture could be traced for more than 6 km lengthwise as a series of imbricate fractures cutting moraines and proluvial cones (Fig. 2, b). In kinematic terms, the rupture plane dipped <30° to the southwest and had a 0.9-1.4 m thrusting displacement with a small (10-15 cm) dextral component [Bogachkin et al., 1997; Su Zongzheng et al., 1999]. The second seismic disruption appeared 25 km to the east, at the junction of the Aigyrzhal and East-Aramsu faults (Fig. 2, a, b). It consisted of a 4 km long series of fractures, the most prominent of which in the flood plain of Suusamyr River, near km 162 of the Bishkek-Osh highway. It was also a thrust with dextral strike-slip component. The largest vertical displacement was 2.7 m with a horizontal offset of 20-30 cm [Bogachkin et al., 1997; Ghose et al., 1997; Ainscoe et al., 2019].
The area of subsequent events such as landslides, rockslides, rockfalls, mud eruption and soil fracturing amounts to more than 4,000 km2. Mapping of these features, together with the degree of infrastructure damage, formed the basis for the earthquake intensity assessment [Korjenkov, 2006]. Intensity isolines 9 and 10 (MSK64 units) define two separate ellipses elongated along the activated faults (Fig. 2, a), one for the main shock along the E-W Aigyrdjal Fault, the other for the second shock along the NW-SE Suusamyr-Toluk Fault. Westward propagation of the seismic rupture along the Suusamyr-Toluk Fault was inferred from the aftershock migration direction [Djanuzakov et al., 2003; Korjenkov, 2006]. As both rupture zones have thrust and dextral strike-slip components, the double shock induced a counterclockwise rotation of the Aramsu Block (Fig. 2, b). This interpretation was already stated after primary investigations of the source area of the Suusamyr earthquake [Bogachkin et al., 1997]. The highest density of aftershocks was recorded within this Aramsu block. Mud eruptions shortly after the seismic event along the borders of this block are consistent with the block rotations and subsequent openings of favorably oriented fracture zones (Fig. 2, b).
By dating paleoseismic dislocations in the epicentral zone of the Suusamyr earthquake, it was established that catastrophic earthquakes comparable to the 1992 event
ET
Я
43
о с
СЛ ri-'—i С
Minkush-Kokomeren basin
Northern slope of Ketmentube basin
Southern slope of Ketmentube basin
"Kaindy" section "Sargata" section
after A. V. Mikolaichuk (Orlov,1979) (current research)
vvyvvyjyi Unidirectional cross ^^^ beds in sandstones and siitstones
Angular unconformity
Stratigraphic unconformity, erosion
Line of age correlation
О CD О CL
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Fig. 3. Stratigraphic columns of the Mesozoic and Cenozoic deposits in the studied area.
Рис. 3. Стратиграфические колонки мезозойских и кайнозойских отложений изученной территории.
occur at an interval of 3-5 ka [Ainscoe et al., 2019]. These data, along with the decoding of the neotectonic structure of the area and information about the present-day stress field [Rebetsky et al., 2016] probably are sufficient to create a tectonophysical model of the earthquake source based on the dextral rotation of the Aramsu block.
Structures in the area to the south of the Suusamyr earthquake source zone are completely different. The EW-striking conjugated Northern Kavak and Southern Kavak Thrusts brought Paleozoic rock units on the up to 3500-4000 m thick Jurassic to Cenozoic sediments of the Minkush-Koko-meren depression [Bachmanov et al., 2008; Sadybakasov, 1990] (Fig. 3), the stratigraphy of which is similar to that of the main basins, such as the Chu, Issykul and Naryn Basins of Central Tien Shan (see Fig. 1b). The Northern Kavak and Southern Kavak Faults join near the eastern end of the Tokotgul reservoir, and the westward continuation of the Minkush-Kokomeren depression is a suture [Burg, Mikolaichuk, 2009; Mikolaichuk et al., 2008]. The Minkush-Ko-komeren depression formed during Late Pliocene - Pleistocene transpression with shortening (evidenced by folds, reverse and thrust faults) combined with sinistral strike-slip offsets [Bachmanov et al., 2008].
3. MICROSTRUCTURE - FAULT DATA
The structural work consisted in a systematic investigation of outcrops exposing mapped faults to determine relative movements from fault surface structures such as stria-tions and sense of shear criteria. Striae are mostly minerals fibres, ridges and grooves produced by hard objects driven along the fault surface (Fig. 4). Local senses of shear were defined from steps, calcite fibre growth, Riedel shears and half-moon features (e.g. [Twiss and Moore, 1992]). All fault planes were very sharp. Those are features characterizing brittle faults formed under very low temperatures near surface conditions. Taking into consideration this observation and working on or close to active faults with locally documented surface ruptures, we assumed that measured striae and movement features recorded recent movements. More
than 12 mesoscopic fault planes with attitudes as various as possible were measured in all sites, which are few tens of metres long and usually of uniform lithology. Such field precautions are required to allow a reliable kinematic analysis.
Fault data were systematically recorded with the aim of computer-aided paleostress tensor calculations. We used the Program FSA 28.3 [Celerier, 2009], which is based on a Monte Carlo search calculation, using random stress tensors to evaluate the tensor best-fitting the measured fault planes and their striations. The detailed assumptions and working procedure are described in [Burg et al., 2005] and further developed in [Celerier et al., 2012]. The best-fitting solution is a reduced stress tensor that can be graphically visualized as stereographic, lower projection of fault data and calculated principal stress. Robustness of the result can be checked with Mohr circles of calculated states of stress and histograms of angular error [Burg et al. 2005]. Since such calculations were aimed at supporting instrumental, seismic information from focal mechanism, we will not develop further this routine technique of structural geology (e.g. [Angelier, 1994; Twiss Unruh, 1998]). At variance with seismological information, it is accepted that such calculations provide a longer term assessment of 'stress' directions than the instrumental time.
The results are summarized as stereographic, lower hemisphere projections of principal stress directions and the shape ratio of the corresponding stress ellipsoid r=(a1-a2)/ (a1-a3), where al3a2>a3, all positive in compression. r»0 means that a1» a2, r«1 if The latter case concerns
the two easternmost sites, all other calculated tensors being >0.7 (Fig. 5). Altogether, these values indicate that principal stresses have magnitudes very close to each other, which can be expected for near-surface faulting and which makes easy swaps between ct1 and a2 or a2 and a3, thus a variable stress field combining compression and exten-sionregimes. Only two sites (Muztor River and Suusamyr 1.3) yielded 'Andersonian' states of stress, with one of the principal stress nearly vertical. However, horizontal ct1 in Muztor River indicates compression, while subvertical ct1
Fig. 4. Examples of fault plane features used for kinematic analysis: (a) - slickensides on a granitic rock near from Karakol Pass; (b) - half-moon shaped Riedels from SW Tuyashuu Pass.
Рис. 4. Примеры плоскостных характеристик разлома, использованных для кинематического анализа: (о) - зеркала скольжения в гранитах вблизи перевала Каракол; (b) - трещины Риделя в форме полумесяца к юго-западу от перевала Туяшуу.
Fig. 5. Site positioned, and determined for them lower hemisphere stereographic projections of paleostress orientations calculated from the kinematic fault analysis and the shape ratio. The method summarized in text.
Рис. 5. Местоположение сайтов и определенные для них стереографические проекции главных осей палеонапряжений в нижней полусфере, рассчитанные на основе кинематического анализа разломов, и коэффициенты Лоде - Надаи. Суть метода изложена в тексте.
in Suusamyr 1.3 indicates extension. All other calculated tensors yielded inclined principal stress directions, most of them with a rather, yet ill-defined WSW-ENE compression. Two reasons are envisioned to explain this variability in the orientation and the shape ratio of the calculated tensor. (1) Measured fault planes were reactivate while stresses vary or the rock mass rotates so that each fault datum records a different stress tensor relative to its reference frame; (2) Measured fault planes were reactivated under a stable configuration of stress and rock mass orientation, but local reactivation matching local heterogeneities yields a regionally imperfect solution. Since in most tensors, none of the principal axes is either vertical or horizontal, a most likely hypothesis is tilting due to block rotations after faulting, possibly linked to free topographic effects.
The complexity of the results may also reflect the fact that measurements lump fault information related to major faulting events, which are responses to regionally significant stress fields, with fault data recording 'aftershock' events, which relax local stresses and deformation. Comparison with modern seismicity suggests that calculated tensors like focal mechanisms document movements responding to local post-seismic relaxation of stresses along different faults under possibly different states of stress. Calculations are therefore significant in interpreting long-term accumulation of stresses and strain in the deforming upper crust.
4. MOTION TYPES IN THE EARTHQUAKE SOURCES
The existing network of seismic stations allows comparing the types of motion at the earthquake source with the movements from fault surface structures. There was no seismic event in the 20 years preceding the Ms=7.3 Suusamyr earthquake in its source area. For this reason, we could only use the fault plane solutions for the main shock and the aftershocks recorded by the Kyrgyz analogue network. The aftershock solutions within the first five hours after the main shock are not defined because of record overlays. The Suusamyr main shock is consistent with structural observations, i.e. reverse with a dextral component (Fig. 6). Focal mechanisms of M>4 aftershocks vary regionally. In the southern part of the aftershock area, the thrust component is similar to the motion of the main shock. To the north, thrust movements that occurred on shallower dipping planes whilst strike-slip components are important. Normal faulting took place in the peripheral part of the aftershock area. Several normal faults are located to the north-west of the main M=6.7 aftershock, and others at the south-eastern edge of the aftershock area (Fig. 6).
These solutions correlate well with the variety of motions and stress tensor calculations defined from microstructural studies, for example, for the Tuyashuu Pass, Alabel Pass and Karakol. However, thrusting is the prevailing motion of active faults of the Suusamyr earthquake source
Fig. 6. Map of the 1992, M=7.3 Suusamyr earthquake with focal mechanisms of aftershocks (M>4) during 1992-1994 and source mechanisms for weaker seismic events (M=3.3) of the Talas-Fergana fault area during the 1992-2007 period. According to 'Earthquakes of Northern Eurasia', Yearbook, 1992-2007. Compressional quadrants are shaded.
Рис. 6. Карта фокальных механизмов главного толчка Суусамырского землетрясения 1992 г. М=7.3 с и его афтершоков (M>4) в течение 1992-1994 гг., а также механизмов очагов более слабых сейсмических событий (М=3.3) в зоне Таласо-Ферганского разлома за 1992-2007 гг. (по данным ежегодника «Землетрясения Северной Евразии», 1992-2007). Области сжатия закрашены.
area. Earthquakes to the south of the Suusamyr earthquake epicenter were not strong (M<4.5). Only 4 earthquakes with M>4 were recorded in the last 15 years along the middle segment of the Talas-Fergana Fault (Fig. 7). Their focal mechanisms (two of them are normal faults, and two are thrusts) yield no prevailing motion type. Again, this difference in stress regimes matches microstructural calculations, normal faults likely accommodating local tension, for example in releasing bends in the general transpres-sional tectonic system under a sub-spherical stress tensor. To complement information of so few earthquakes, the fault plane solutions of events with M<3.5 (Fig. 7) have also been considered in 'Earthquakes of Northern Eurasia', Yearbook, 1992-2007. There are 7 strike-slip, 5 thrust and 3 normal fault events. This suggests prevalence of strike-slip motion along the Talas-Fergana Fault segment traced on the map (Fig. 7).
5. MAXIMAL MAGNITUDE OF THE EARTHQUAKES
Historical and instrumental data provide no record of any ancient earthquake comparable in magnitude with the 1992 Suusamyr earthquake in the study area over the last
200-300 years (see Fig. 1, c). This period, however, is very short compared to the recurrence intervals of large intraplate earthquakes, which usually range from several centuries to several millennia [Djanuzakov et al., 1980, 1997]. That is why more reliable Mmax estimates require using paleo-seismologic data [McCalpin, 1996, 2009; Solonenko, 1974; Yeats et al, 1997]. Paleoseismologic studies in the study area identified numerous surface ruptures, large rockslides and caldera-like cavities associated with large prehistoric earthquakes [Strom, 2000,2009,2013; Korjenkov, 2006; Korjenkov et al. 2012; Mamyrov et al. 2009]. The largest possible Mmax M=7.3 for the South-Aramsu and M=6.9 for the Suusamyr-Toluk Faults (see Fig. 2, a) were estimated in accordance with the magnitudes of the main shock and largest aftershock of the Suusamyr earthquake. The M for the Kyzy-
j i max J J
loi thrust was estimated from the Late Pleistocene Koko-meren rockslide, which is located in the western part of the fault and is one of the biggest paleoseismologic events in Kyrgyzstan [Strom, Stepanchikova, 2008; Strom, 2010]. This gigantic rockslide (41.93 °N, 74.23 °E) is approximately 1.0 km3. The 400-m thick rockslide is exposed on the left bank of Kokomeren River, where it covers a high fluvial terrace
Fig. 7. Focal mechanisms of weak (M< 3.3) seismic events along the Talas-Fergana fault during the 1992-2007 period, using Earthquakes of Northern Eurasia, Yearbook, 1992-2007.
Рис. 7. Фокальные механизмы слабых (М<3.3) сейсмических событий вдоль Таласо-Ферганского разлома за период 19922007 гг. по данным ежегодника «Землетрясения Северной Евразии», 1992-2007.
that was about 100 m above the riverbed at the time of the rockslide. The most important indication in favour of seis-mically-triggered landslide is the presence of an active fault that displaced the river terraces few hundred meters downstream from the site [Strom, Stepanchikova, 2008]. According to its morphological parameters, this landslide is bigger than all the known surface damages caused by the Suusamyr earthquake. Consequently, the Mmax value along the Kyzyloi Fault is likely >7.3.
The M of the Talas-Fergana Fault is taken from the
max °
Chatkal earthquake (1946; M=7.5, I0=9-10 of MSK64) [Djanuzakov et al., 2003]. Moreover, the earthquake source
zone with M=7.1-8 is aligned along the Talas-Fergana Fault [Abdrakhmatov et al, 2012; Djanuzakov et al., 1980].
This zone is based on 17 seismic events documented between 6120±170 and 250±50 years, with an average return period of 300 years [Korjenkov et al. 2012; Mamyrov et al., 2009]. These events were dated by the radiocarbon method (Table; Fig. 8). Traces of the largest events allow concluding that Mmax for these events might reach 8 units [Abdrakhmatov et al., 2012; Djanuzakov et al., 1980].
One paleoseismic evidence is the 234 m deep landslide-dammed Sarychelek Lake in the upper reaches of the West Karasy River valley (41°51.5'N, 71°59'E). It was formed
Fig. 8. Paleoseismicity along the Talas-Fergana Fault after [Burtman et al., 1996; Korjenkov et al., 2012; Mamyrov et al., 2009; Strom, 2010; Trifonov et al., 1990]. White rectangles are sites where surface rupture were investigated with trenches. Dating for these sites is given in Table.
Рис. 8. Палеосеймодислокации вдоль Таласо-Ферганского разлома по [Burtman et al., 1996; Korjenkov et al., 2012; Mamyrov et al., 2009; Strom, 2010; Trifonov et al., 1990]. Светлые прямоугольники - сегменты разлома, вскрытые траншеями. Датировки по этим участкам приведены в таблице.
Radiocarbon dates of samples collected from displaced gullies along the Talas-Fergana Fault
Радиоуглеродные датировки образцов (палеопочв), отобранных из смещенных русел вдоль Талас-Ферганского разлома
River valley or a name of the fault segment Obtained radiocarbon ages, years Average age of the earthquakes, years River valley or a name of the fault segment Obtained radiocarbon ages, years Average age of the earthquakes, years
1720 ±70 1720±70 Kok-Bel 4900 ±230 4900 ±230
1940 ±50 1940 ±50 Janaryksay 1440 ±30 1440 ±30
Jilangach 2630 ±70 2740 ±70 2685 ±70 440 ±45 505 ±80 475 ±80
3970 ±40 3970±40 1130 ±100 1130 ±100
Chitty-West 4590 ±100 4590±100 2385 ±130
5800 ±1300 5800±1300 Sary-Bulak 2415 ±100 2400 ±130
Birguzy 3030 ±90 3030±90 4930 ±90 4930 ±90
3740±600 3740±600 5200 ±140 5220 ±150
2180±120 2230±120 5240 ±150
2280 ±70 2590±600 6120 ±170 6120 ±170
Pchan 2540 ±70 250 ±50 250 ±50
2640±600 3150 ±40 3150 ±40 1150 ±40 1220 ±50 1220 ±50 1195 ±50
2320 ±40 2320 ±40
Kyldau 3670 ±80 3670 ±80
3670 ±80 Chatkal 1350 ±60 1350 ±60 1450 ±40 1385 ±60
Urumbash 1510 ±60 1510 ±60
Keklikbel 1240 ±60 1240 ±60
2020 ±50
285 ±35 285 ±35 2020 ±50
975 ±65 2020 ±50
Karasu 980 ±55 1015 ±75 990 ±75 405 ±100 460 ±40 450±100
240 ±50 Kara-Bura 480 ±35
270 ±85 295 ±90 4465 ±130 4465 ±130
Kok-Bel 370 ±90 5910 ±130 5910 ±130
2340±120 2435 ±120 6100 ±200 6100 ±200
2500±100 Sulu-Bakair 5210 ±155 5210 ±155
Note. Sites (fault segments) are arranged as shown in Fig. 8 from SE to NW. Compiled by [Korjenkov et al., 2012] after [Burtman et al., 1996; Korjenkov et al., 2010; Mamyrov et al., 2009; Trifonov et al., 1990].
Примечание. Участки (сегменты разломов), расположенные в последовательности, показанной на рис. 8, с ЮВ на СЗ. Составлены [Korjenkov et al., 2012] по [Burtman et al., 1996; Korjenkov et al., 2010; Mamyrov et al., 2009; Trifonov et al., 1990].
by a 34 km2 prehistoric landslide that left the 6.5 km long headscarp in Devonian sedimentary rock. The dam volume is >6 km3 [Strom, 2010]. Another paleoseismic evidence is the 300x106 m3 Karakul rockslide that blocked the Kara-su-Left River mouth (41°38'N, 72°39'E). The 2.5x108 m3 and about 250 m high rockslide is composed of Devonian limestone that collapsed from the 900 m high left bank of the valley and thrusted over Permian sandstone and conglomerates. Besides the Karasu-Left River mouth, it blocked also the Naryn River [Strom, 2010]. The resulting 150 m deep Karasu Lake invaded the Karasu-Left River valley. This dam is located at 41°34.5'N, 73°13.5'E exactly over the trace of the Talas-Fergana active fault [Mamyrov et al., 2009; Strom, 2010]. Comparable paleoseismological
events occurred along the Northern-Kavak Fault, as evidenced by a series of caldera-like craters and rockslides (see Fig. 2, a). The eastern crater (Kyzylkul, 41°48.1'N, 73°45.3'E) is a roughly elliptic body, about 3x2 km in size and 3 km3 in volume with steep, 250 to 700 m high edges and a relatively flat bottom [Strom, 2000; Strom, Groshev, 2009]. The second crater (Djuzumdy, 41°48.75'N, 073°22.85'E), about 1x0.5 km and 200-300 m deep, has a roughly rhomboid form. Its volume is about 0.12 km3. It is located 28 km to the west of the Kyzylkul dam in the upper reaches of the Djuzumdybulak stream. The southern boundary of the Djuzumdy crater is an active fault that ruptured about 2000 years ago [Strom, 2000; Strom, Groshev, 2009]. These craters were compared to
a similar crater formed during a M>8 earthquake in 1957 in Gobi Altai, Mongolia [Florensov, Solonenko, 1963] and accordingly attributed to a paleo-earthquake of M=7.5-8.0 [Strom, 2009].
6. CONCLUSION
This work shows that the geographically unexpected Ms=7.3 Suusamyr earthquake of August 19, 1992 is not the strongest event that may occur in the area. Stronger seismic events took place not only in the western, but also in the southern parts of the Suusamyr earthquake source zone, namely within Minkush-Kokomeren transpressional zone, along which the Naryn River.
The Kambarata HPP-2 projects is already completed. Construction of the Kambarata Hydro Power Plant-1 has already started. Following the existing seismic zoning maps [Abdrakhmatov et al., 2012; Turdukulov, 1996], these two power plants are designed with account of risks of possible earthquakes with <7.5. Our study shows that magnitudes up to 8 should be expected. We hope that experts in seismic zoning and earthquake-resistant construction will revise and reassess their project to face the risk.
8. ЛИТЕРАТУРА/REFERENCES
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With a similar warning conclusion, attention should be drawn to the western part of the Minkush-Kokomeren transpressional zone that includes the Toktogul water reservoir, the largest in Central Asia with a volume of 19.5 km3 and an area of 284 km2 [Simpson, Negmatullaev, 1978]. Filling of the reservoir started in 1973. At that time, the geological study of the territory subject to flooding consisted only of geological mapping (scale 1:200000) and aero-magnetic studies (scale 1:100000). Deep structures hidden beneath the Cenozoic cover were ignored.
Our data showing that the Minkush-Kokomeren transpressional zone extends as far west as the Talas-Fergana Fault give grounds to conclude that the reservoir is a high-risk site that should be surveyed with geophysical sounding techniques (electric, magnetic, seismic), and activities aimed at mitigation of any catastrophic event should be properly planned.
7. ACKNOWLEDGMENT
We are grateful to Alexander Strom for a comprehensive discussion of the Inner Tienshan seismodislocations. We thank SNSF for financial support of this research (Project No IB7320-110694).
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ALEXANDER V. MIKOLAICHUK
Candidate of Geology and Mineralogy, Senior Researcher Institute of Geology of NAS 30 Erkindyk Blvd, Bishkek 720481, Kyrgyzstan e-mail: [email protected] ORCID: 0000-0002-0247-1856
АЛЕКСАНДР ВЛАДИМИРОВИЧ МИКОЛАЙЧУК
канд. геол.-мин. наук, с.н.с. Институт геологии НАН
720481, г. Бишкек, бул. Эркиндик, 30, Кыргызстан
ZOYA A. KALMETEVA
Candidate of Physical and Mathematical sciences, Senior Researcher
Central-Asian Institute for Applied Geosciences 73/2 Timur Frunze Rd, Bishkek 720027, Kyrgyzstan e-mail: [email protected] ORCID: 0000-0001-5172-3741
ЗОЯ АРСЛАНОВНА КАЛЬМЕТЬЕВА
канд. физ.-мат. наук, с.н.с.
Центрально-Азиатский институт прикладных исследований Земли
720027, г. Бишкек, ул. Тимура Фрунзе, 73/2, Кыргызстан
JEAN-PIERRE BURG
Doctor, Full Professor of Geology ETH Zurich Earth Sciences 5 Sonneggstrasse, Zurich CH-8092, Switzerland e-mail: [email protected] ORCID: 0000-0002-4927-4729
ЖАН-ПЬЕР БУРГ
докт., профессор геологии
Департамент наук о Земле, Высшая техническая школа СН-8092, г. Цюрих, Зоннегштрассе, 5, Швейцария
DAVID FOSSATI
Geological Engineer Marti Tunnelbau AG
21 Seedorffeldstrasse, Moosseedorf 3302, Switzerland e-mail: [email protected] ORCID: 0000-0003-3995-6336
ДЭВИД ФОССАТИ
инженер
Компания «Marti Tunnelbau AG»
3302, г. Мосзеедорф, Зеедорфельдштрассе, 21, Швейцария
DMITRY V. GORDEEV
Post-graduate Student
Institute of Geology of NAS
30 Erkindyk Blvd, Bishkek 720481, Kyrgyzstan
e-mail: [email protected]
ORCID: 0000-0001-8287-1018
ДМИТРИЙ ВАЛЕНТИНОВИЧ ГОРДЕЕВ
аспирант
Институт геологии НАН
720481, г. Бишкек, бул. Эркиндик, 30, Кыргызстан
