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Rate of erosion and exhumation of crystalline rocks in the Hunza Karakoram defined by Apatite fission track analysis.

1. INTRODUCTION

Studies of the extent of denudation and erosion of near-surface parts of the Earth's crust in active orogenic belts are fundamental for knowledge of landform evolution during the late Cenozoic (e.g. Burbank, 2002). The geomorphological record of active orogeny is associated with research of climate-morphogenetic changes of landform patterns in the Karakoram (see Desio, 1974, 1979; Kalvoda, 1992a, b; Derbyshire, 1996; Seong et al., 2007, 2009; Hewitt, 2005, 2009). It provides evidence of the Quaternary evolution of the dissected high-mountain relief. In the presented study, the geomorphological signatures of extreme erosion supported by the surface uplift of the Hunza Karakoram in the late Cenozoic is compared with the thermochronological history of relevant crystalline rocks during active collision orogeny. In order to estimate the rate of exhumation of crystalline rocks from the Hunza Karakoram in north-eastern Pakistan (Fig. 1), we used the apatite fission-track (AFT) geochronology technique. Generally, this radiometric dating method provides the characteristics of the time-low-temperature evolution of studied rock masses and their cooling ages (Burbank et al., 1996) in the period from the Upper Miocene to the recent. The AFT method is also useful for studies of the denudation/exhumation orogen evolution and the tectonics-climate relationship. Our data represents new Thermo-chronological information from the Hunza Karakoram area and, together with already published data from the Himalaya (compare e.g. review in Thiede and Ehlers 2013), contributes to a comprehensive view of the region between the Karakoram, the Tibetan Plateau and the Himalaya affected by the convergence and collision of Indian and Eurasian plates in the period from 50 Ma to the present.

2. GEOLOGICAL SETTING AND LANDFORM PATTERNS OF THE HUNZA KARAKORAM

The Karakoram Range represents a great mountain system with the highest concentration of peaks over 8000 m in height and one of the most heavily glaciated parts of the Earth. The Karakoram Range extends ca. 500 km from the easternmost extension of Afghanistan in a southeasterly direction to NE Pakistan and is part of a complex of mountain ranges at the centre of Asia (Schneider 1957, 1960; Tahirkheli, 1982; Searle, 1991), including the Hindu Kush to the west, the Pamirs to the northwest, the Kunlun Mountains to the northeast, and the Himalayas to the southeast (e.g. Desio, 1979; Rex et al., 1988). The recent orogeny of the Karakoram Range and the Himalaya are the youngest evolutionary stage of the Alpine-Himalayan system (e.g. Searle, 1991, 2007). During the Quaternary, most of these mountain ranges achieved their morphotectonic characteristics and landform patterns.

The studied area of the Hunza Karakoram includes the adjacent area lying northward of the Main Karakoram Thrust zone dividing the Karakoram from the Ladakh-Kohistan arc-batolith with the Indus Suture Zone on its southern margin (Fig. 1). The Indus Suture Zone is the major suture forming the boundary between the Indian plate and the Karakoram and Lhasa morphostructural blocks. It represents a small back-arc basin as a result of magmatic episodes during the Indo-Asian collision (Jurrasic and middle-Upper Cretaceous ages) before closing the Tethys Ocean at ca 50-45 Ma (Searle, 1991). The Main Karakoram Thrust is interpreted as a steep north-dipping thrust fault zone representing a reactivated break-back thrust. It followed after the late Cretaceous closing of the Shyok suture zone (Pudsey et al., 1985; Coward et al., 1986, 1987, 1988). Karakoram high-grade metasediments were thrust southwards over low-grade metasediments previously deformed along the Shyok suture zone (Carboniferous to Albian-Aptian) and the Ladakh Batholith (Cretaceous to Eocene) (Searle et al., 1987; Searle and Tirrul, 1991). The (post)-Miocene uplift of the Karakoram was a response to the continuous crustal thickening in the above mentioned magmaticcollision periods (Rex et al., 1988; Foster et al., 1994). The young AFT-cooling ages of high-grade rocks in this thrust zone yielded ages less than 10 Ma suggesting a late Tertiary uplift along the thrust zone.

The main morphotectonic units of the Hunza Karakoram are from SW to NE (Fig. 1):

a) Karakoram Metamorphic Complex, b) Karakoram Batholith and c) The Northern Karakoram Terrane. The Karakoram Metamorphic Complex forming the southern margin of the Karakoram consists of various metasedimentary (Hunza schists and dominantly Hunza limestone) and metaigneous granodiorite rocks, which show a complex polyphase evolution of deformation and metamorphism (Bertrand and Debon, 1986; Searle, 1986). The last stage of the evolution of the entire southern Karakoram represents low P-T metamorphism. It is related to the post-Miocene uplift along the Main Karakoram Thrust zone (Searle and Tirrul, 1991).

The Karakoram Batholith belongs, with the Ladakh- and Kohistan Batholiths and the Gandese magmatic belt, to the Trans-Himalayan plutons and gives evidence to the Late Mesozoic subduction of the Indian Plate (Coward et al., 1982; Rolland et al., 2000). The subduction of the Indian plate also documents high-pressure and/or ultra high-pressure metamorphism in the Tso Morari area and the Ladakh batholith (Sachani et al., 2004). Initial Nd, Sm and Pb isotopic compositions of the Trans-Himalayan plutons indicate that they have predominantly mantle-derived components. U-Pb zircon ages of Trans-Himalayan plutons varying from 105 to 45 Ma (Honegger et al., 1982; Scharer et al., 1984; Weinberg and Dunlap, 2000) and their geochemistry point to the northward subduction of the Tethyan oceanic lithosphere beneath the Eurasian Plate (Singh and Jain, 2003). Along the Karakoram Batholith are widespread pre-collision granites (Hunza plutonic unit), whose geochemistry (Crawford, 1988) and age (Searle et al., 1988, 1989) suppose that they were formed in the Jurassic and Early Cretaceous by a partial melting of the crust above a northward-dipping oceanic subduction zone along the southern continental margin of the Karakoram plate.

The Karakoram Batholith is a composite intrusion represented by two sections-the Hunza Batholith and Baltoro Granites. The Hunza Batholith is made up of a) early biotite-hornblende-bearing granodiorites with U-Pb ages of zircons of c. 95 Ma in the Hunza Karakoram dating the emplacement of the batholith (Le Fort et al., 1983), and b) Miocene peraluminous garnet and two-mica-bearing granites which formed a section along the Baltoro glacier (Debon et al., 1986). Granitoids of the collision zone and also studied samples from the Hunza Karakoramindicate the presence of Paleo-Meso Proterozoic rocks, and emplacement of Early Paleozoic granitoids (Singh and Jain, 2003). The Northern Karakoram Terrane comprises sedimentary units such as Pasu limestones, Pasu slates, chiastolite slates and precollision K2 orthogneiss and granites.

The main localities of studied samples from the Hunza Karakoram (Fig. 1) are situated between the Hunza river and the Hispar glacier. Samples (No. 14, 18, 71, 72 and 77) were selected from an elevation profile from SW-NE transect in the Hispar and Gharesa regions of the Hunza Karakoram. Sample No. 2 is a large block of amfibolite-biotitic granite material from the Gilgit catchment area. Observations of landform patterns of peculiar relief types between the Distaghil Shar (7 886 m) and the Hunza valley (2 000 m) suggest extremely high rates of denudation, sediment transfer and deposition (Li Jijun et al., 1984; Kalvoda, 1990; Kalvoda and Goudie, 2007). The vertical hierarchy of variable high-mountain reliefs is striking (Derbyshire et al., 1984; Hewitt, 1989; Kalvoda, 1992a, b; Iturrizaga, 2001) from the extremely cold extraglacial ridges of the western Himalaya and the Great Karakoram Range (Fig. 2) through the heavily glaciated and periglacial areas (Fig. 3) to the seasonally cold/warm semiarid Bualtar, Nagar and Hunza valleys.

Distinctive vertical climatic zoning of the Hunza Karakoram influences various features of morpho-structural and lithological control of characteristic weathering phenomena (Cilek and Kalvoda, 1983; Goudie, 1984; Goudie et al., 1984a, b; Kalvoda and Goudie 2007). There are extraordinary geomorphological hazards which include high-magnitude rapid events of mass movements triggered by earthquakes, glacier surging, avalanches, flash floods and landslides (Brunsden and Jones, 1984; Hewitt, 1989, 2009; Gardner and Hewitt, 1990; Derbyshire et al., 2001). Studies of the dynamics of glaciers are also connected with the Late Glacial and Post Glacial sedimentary record of geomorphological processes (Owen and Derbyshire, 1989, 1993; Kalvoda, 1990; Owen et al., 2002; Kuhle 2006) and very high erosion rates (more than 1 cm.[yr.sup.-1]) in the Hunza Karakoram. Averaged rates of maximum incision from areal denudation for mass movements, glacial and river erosion for the past ca 55 ka are recorded between 2.2 and 1.1 cm.[yr.sup.-1] (Goudie et al., 1984a; Derbyshire, 1996; Kalvoda and Goudie 2007). Similarly as in neighbouring regions (compare e.g. Kuhle, 1988a, b, 2001, 2006; Iturrizaga, 2001; Kalvoda et al., 2004; Hewitt, 2005, 2009, Seong et al., 2007, 2009; Hewitt et al., 2011), a striking phenomenon of the Hunza Karakoram is that the oldest relics of Quaternary sediments, which are preserved in accumulation landforms of mountainous valleys and basins, are younger than 2 x [10.sup.5] years but most of them are from the Upper Pleistocene and younger than ca 50 x [10.sup.3] years.

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3. METHODS AND ROCK SAMPLES

3.1. ANALYTICAL TECHNIQUES

Apatite Fission Track analysis (AFTA) was used in order to understand the time-low-temperature evolution of crystalline rocks from studied area. This dating method is based on radiation damage trails ("fission tracks") within apatite grains produced continuously during geological time by spontaneous fission of single atoms of [sup.238]U. For details and principle of the analysis see e.g. papers by Fleischer et al. (1965), Naeser (1979), Wagner and Van den Haute (1992), Gallagher et al. (1998), Jonckheere and Van den Haute (2002), Ketcham (2005) and Ketcham et al. (2007a). Fission-track ages and exhumation rates of studied samples are identified by measuring the concentration of uranium in apatite grains. It is determined by irradiation of the samples in a nuclear reactor with thermal neutrons. These neutrons induce fission of [sup.235]U isotopes in the irradiated sample. The induced fission-track density (pi; number of tracks/[cm.sup.2]) is obtained in an identical way as spontaneous tracks (by etching and counting tracks using an optical microscope) and provides a measure for the [sup.235]U concentration. Because in nature the [sup.235]U/[sup.238]U ratio is a constant, the overall uranium concentration can be derived and finally should enable the age of the studied samples to be calculated.

Time-temperature evolution of the studied samples is defined by a combination of confined (horizontal) track length measurements and determination of the fission track-age of individual apatite grains. Fission tracks (FT) are thermally unstable and each individual decay event can be identified. The maximum length of the apatite FT (16.3 gm) is shortening (annealing) at a rate which depends on the temperature at the time of their forming. The final shortening is reflected by thermal annealing determined by the highest temperature which the track has experienced.

The apatite grains of studied samples were processed using conventional separation methods: crushing, Wilfley table-density separation, magnetic and heavy liquid techniques to obtain the purest apatite fractions. The subsequent analytical techniques for dating of apatites in the presented study are identical to the instructions described by Fitzgerald and Gleadow (1988, 1990) and Foster and Gleadow (1992). The apatite crystals were sealed in epoxy resin, polished, etched with a 2.5% HN[O.sub.3] solution for 70 s at 22 [degrees]C to enable visibility of the spontaneous fission tracks, fitted with a muscovite external detector (Miller et al., 1993) and irradiated in a nuclear reactor (Oregon State University Radiation Center) by thermal neutrons. For details of specific laboratory instrumentation and fission track procedure at the Institute of Geology, Academy of Sciences of the Czech Republic, see Murakami and Svojtka (2007). The Zeta calibration factor, determined in accordance with Hurford and Green (1983), together with the measured FT-densities, was used in the equation for the FT-ages calculation in the Trackscan software. Using TrackKey 4.2 g software (Dunkl, 2002), the FT-ages of the studied samples were graphically dispayed and evaluated. Confined (horizontal) tracks were measured as 'tracks in tracks' type in c axis parallel etched and polished surfaces of apatite grains and were normalized for a crystallographic angle using a c-axis projection (Green and Durrani, 1977; Ketcham et al., 2007a). In addition to temperature mentioned above, the amount of chlorine in the apatite lattice represents a critical compositional control on the degree of annealing. Chlorine-rich apatites are more resistant (slowly annealed) to track annealing than fluorine-rich apatites (e.g. Barbarand et al., 2002). Accordingly, Cl-content was measured by electron probe microanalyzer. As a result, all the studied apatites are fluorine-apatites (Cl-content was below 0.05 wt%, see Table 1). Such low chlorine content in apatites does not influence annealing parameters. In time-temperature modelling graphs (Fig. 6) are marked by "black boxes" geological constraints that represent independent geochronological information from previously published papers. Using time-temperature information on rocks with similar tectonometamorphic history as studied rocks (see legend in Fig. 6), but with different isotope system and different blocking temperature, significantly improves the t-T modelling to higher temperatures.

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3.2. GEOMORPHOLOGICAL POSITIONS OF THE STUDIED ROCK SAMPLES

For the purposes of AFT analysis a set of varied crystalline rock samples from the Hunza Karakoram was used. The samples come mainly from the SW-NE transect in the Hispar and Gharesa regions of the Hunza Karakoram (Fig. 1). The highest mountain massifs from these regions of the central Karakoram are Distaghil Shar (7 885 m), Trivor (7 720 m) and Lupar Shar (7 220 m). The glaciated high-mountain zone displays an integration of deep weathering of rocks with major glacial and nival processes (Fig. 3). The valleys and ridges of the Hispar Karakoram are overfilled by glacier masses at high altitudes above 5 600 m a. s. l. Large ice source areas contrast with the very narrow canyon-like lower parts of the valleys (Fig. 4). The recent retreat of the glaciers is accompanied by an increase of the active periglacial processes which is a dominant phenomenon of the present-day changes of landform patterns stimulated by climate-morphogenetic processes.

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Variable lithological types of crystalline rocks were collected from altitude of ca. 2 400 to 5 600 m a.s.l. Sampling strategy (Fig. 1) was carried out with the aim to cover both crystalline units (Karakoram Metamorphic Complex and Karakoram Batholith) that are located in uneasily accessible terrain. Sample collection represents selection of representative lithological rock-types suitable for AFT dating and not continuous altitude profile. Exception is sample No. 2 that was collected from a large block (30[m.sup.3]) of amfibolite-biotitic granite from flood accumulation on the right bank of the Gilgit river (2 200 m), 2 km westward from the confluence of the Hunza and Gilgit rivers (Fig. 1). It was transported from the middle part of the Gilgit catchment area situated SW of the Hunza region of the Karakoram. Other samples were collected from rock outcrops and represent "in situ" material. Sample No. 14 is calcalcalic-biotitic granite with amfibole from a large rock outcrop near the foot of a structural slope (2 400 m), 2 km westward from the small town Aliabad in the Hunza valley. Sample No. 18 is amfibole-biotitic granodiorite from a rock outcrop northward from Nagar village (2 550 m) in the middle part of a steep erosional slope of the Hispar valley. Sample No. 71 is muscovite-biotitic granodiorite from 5 650 m (Fig. 4) in the southern wall of the Trivor Massif. Sample No. 72 is biotitic granodiorite from a large rock wall of a cirque of the Gharesa glacier (5 500 m, Fig. 2) in the Trivor Massif. Sample No. 77 is biotitic quartz diorite from strongly cryogenically weathered nunatac (5 200 m, Fig. 3) near the southern wall of the Lupar Shar.

Terms such as denudation, exhumation and erosion used in this paper correspond to (re)definition by England and Molnar (1990) and further description by Summerfield (1991) and Ring et al. (1999). Denudation is understood as a removing (unroofing) of material from an area on the Earth's surface, exhumation characterizes unroofing of a point or vertical transect of studied rocks. Denudation and exhumation occur as a result of erosion and tectonic processes (e.g. Lisker et al., 2009). Erosion is a set of geomorphic processes causing weathering and the transport of material. The rate of erosion quantifies the transported material from one place on the Earth's surface to another. Active tectonics involves processes such as extension, normal faulting and thrusting that result in rapid removing of large rock volumes. The rate of denudation and exhumation of rocks express results of integrated activity of climate-morphogenetic and tectonic processes.

4. RESULTS

Apatite fission-track dating of the "in situ" rocksamples from the Hunza Karakoram yielded ages between 3.9 [+ or -] 0.8 Ma to 7.5 [+ or -] 1.8 Ma in narrow age cluster (Table 1). AFT- age of flood-transported sample No. 2 yielded 9.9 [+ or -] 2.4 Ma, which is comparable with observed older cluster of ages and probably reflect influence of higher altitude of the source area. There is no clear correlation between apatite fission-track age and topographic elevation (m a. s. l.) of the studied samples (Fig. 5). All the studied samples failed the probability test P([chi square]) for Poisson distribution because P-values are <1%. The samples have experienced a long-term cooling period within the apatite partial annealing zone. The age spread of all apatite grains show relatively distinct homogenous age-population in the radial plots (Figs. 6 and 7). It also is documented by minimal differences in the chlorine content (Table 1) between individual apatite grains within the samples.

The apatite grains of samples were examined by electron microprobe analyser (Cameca SX 100) for chlorine content, which varies between 0.012 to 0.035 wt% and thus represents fluorapatites. All studied apatites from the Hunza Karakoram provided a large number of confined tracks (above 100 tracks) necessary for track-length measurement and consequently for time-temperature modelling (Figs. 6 and 7). Measured track-lengths for the "in situ" rocksamples vary from 10.7 [+ or -] 2.4 [micro]m to 12.1 [+ or -] 2.2 [micro]m, and have been shortened on average 4.9 [+ or -] 2.4 [micro]m from maximal value. The average track-length of the flood-transported sample No. 2 was 10.3 [+ or -] 2.8 [micro]m (Table 1) and is shorter than the maximal value by about 6 [+ or -] 2.8 [micro]m. The maximal peak in the track length-frequency diagrams (Fig. 7C) shows a long-term stable uplift across the apatite partial annealing zone of all the studied samples, which also confirm the modelled time-temperature trajectories in Figure 6. Sample No. 2 had this uplift probably more gradually than the other "in situ" samples. Figure 8 captures a striking correlation between fission-track length and elevation of collected samples. The red line in the graph shows a slightly increasing trend in average lengths of measured confined tracks with increasing elevation of the studied samples. The observed trend can be interpreted as a signature of increasing morphogenetic impact of erosion rates stimulated by the large-scale tectonic uplifts of the Karakoram region.

Time-temperature modelling of all the studied samples shows a similar thermal history style, involving a period of total thermal annealing and a subsequent period of cooling corresponding to considerable exhumation and erosion processes. Based on time-temperature curves and track-length-distribution histograms (Figs. 6 and 7), apatite fission-track ages can be interpreted as cooling ages accompanying denudation of the Hunza Karakoram in the late Cenozoic. Time-temperature (t-T) curves of samples (Fig. 6) testify to two dominant trends of cooling rate in both above units (Karakoram Metamorphic Complex and Karakoram Batholith): an Upper Miocene to Pliocene period of a slow cooling rate of ca. 0.1 km/Ma followed by the Quartenary period of a relatively rapid cooling rate of ca. 2.6 km/Ma. Despote slightly different trajectory in individual samples, the average cooling rates are similar to all studied samples. Differences in t-T trajectory are mainly for uplift of samples from Oligocene to Miocene, the later stages are comparable (Fig. 6). The later period of cooling is associated with the approach of (sampled) rock assemblages near late Cenozoic denudation and/or erosion surfaces. However, time-temperature curve of the one transported sample No. 2 is well comparable with "in situ" samples No. 18 and 77. These samples have endured a prolonged period of cooling within the apatite partial annealing zone (APAZ) and its uplift was probably more gradually than the other samples.

Apatite fission-track t-T data indicate that the studied rock samples from the Hunza Karakoram were positioned in shallow sub-surface depths up to 4 000 m from the Oligocene-Miocene boundary for samples No. 2, 18 and 77 and from the Upper Miocene for samples No. 14, 71 and 72. Denudation and erosion of rock masses in the Hunza Karakoram estimated by a combination of current elevations of samples and depths of the fossil apatite partial annealing zone reached up to 4000 m from the Upper Miocene to the present. In view of the present-day elevation of individual samples, it is possible to determine the maximum rock uplift (Table 2), which can be assessed as more than 9 000 m.

5. DISCUSSION

Pioneer geological and geographical studies have already argued that continuous denudation of the near-surface part of Hunza Karakoram rock massifs from the Neogene to the present time is caused by active orogeny as well as intensive exogenous processes (compare Paffen et al., 1956; Schneider 1957, 1960; Wiche, 1959, 1962; Desio, 1974, 1979; Desio and Martina 1972). Thermochronological data confirmed very effective denudation, erosion and transport of near-surface rock masses during the late Cenozoic. Rapid exhumation (unroofing) of deeper parts of the rock massifs also needs vigorous transport agencies. Apatite fission-track dating of variable lithological types of crystalline rocks from the Karakoram Metamorphic Complex and the Karakoram Batholith gives evidence of an increasing significance of erosion rates from the period of a slow rate (Upper Miocene to Pliocene) to the Quaternary period of a relative rapid rate. The high intensity of recent denudation and rapid transport of weathered and eroded material correlates with a striking absence of older Quaternary sediments (e.g. Kalvoda, 1984; Hewitt, 1989, 2009, Hewitt et al., 2011; Kalvoda and Rosenfeld, 1998; Goudie and Kalvoda, 2004). It suggests a long-term influence of these morphogenetic processes on the exhumation of deeper parts of the Earth's crust during the active collision orogeny of the Hunza Karakoram.

In strikingly uplifted orogenic belts, an increase of fission-track age with increasing elevation is often observed. Such a linear data set implies uplift of the area as a homogeneous block without significant faulting structures. In opposite, blocks without a clear correlation between age and elevation represent areas strongly affected by faulting (Wagner et al., 1977; Naeser, 1979). Due to the observed uncertain ageelevation correlation from the studied area (Fig. 5), we assume that the measured apatite fission-track ages from the Hunza Karakoram were probably affected by thrusting and faulting in an active orogenic belt, and uplifted as a more independent rock-massive blocks. A similar non-linear data set is described from Gasherbrum IV diorite by Cerveny et al. (1989) and interpreted as variable time-spatial tectonic activity along thrust- and fault-systems. Further reason can be suggested according to Le Fort et al. (1983) as a partial resetting of fission-track ages by contact metamorphism during emplacement of the Hunza Batholith (106-95 Ma, U-Pb zircon age) and also by subsequent Eocene regional metamorphism at the time of the Indo-Eurasian collision. Moreover, hydrothermal fluids migrated through fractures are mentioned by Cerveny et al. (1989) as a resetting factor for annealing of fission-track data from the Hunza and Gasherbrum regions. The differences in the measured apatite fission-track ages can probably be caused by extreme dissection of high-mountain relief, which affects erosion rates.

Early Cretaceous zircon fission-track ages of K2gneisses (120-115 Ma) in the Gasherbrum IV region can be correlated with Karakoram Batholith Granitoids (106 Ma) and with the Hunza Batholith (106 Ma) including early to pre-Miocene components (Cerveny et al., 1989). Both regions lie close to the Karakoram Thrust Zone and, therefore, they probably experienced similar tectonic evolution. We adopted the value of 30 [degrees]C/km as geothermal gradient, typical for orogenic belts for T-t modelling. Similar values of palaeogeothermal gradient were used in late Tertiary rocks of the northern Karakoram by Cerveny et al. (1989). Using this value, calculation of the amount of erosion material is considered to be about 4 km from Upper Miocene till recent. All studied F-rich apatites had a chlorine content of below 0.4 wt%, which is the threshold for no effect on the annealing parameters in apatite grains (Barbarand et. al., 2003). According to the very close Cl-values spread, it seems that the studied samples probably represent uniform age population. Track-length frequency histograms (Fig. 7) demonstrate a slightly bimodal distribution of confined tracks in apatite grains. This distribution illustrates cooling evolution associated with the maximally two thermal events for the studied rocks. This also corresponds to the radial plots (Fig. 7), which did not reveal more clearly defined age-population of apatite grains in most of the samples.

Foster et al. (1994) studied apatite separated from samples collected from elevations of 5 300 to 8 611 m in the K2 region of the Baltoro glacier. The apatite yielded fission-track ages of 2.1 [+ or -] 0.6 to 4.3 [+ or -] 1.4 Ma, and suggest an initial, apparent denudation rate of 3-6 mm.[yr.sup.-1] commencing after 5 Ma. Shroder and Bishop (2000) thought that rapid erosional unroofing of the Nanga Parbat Massif in the western Himalaya was initiated at 12-10 Ma. It also can be mentioned that even rough valuations of erosion and denudation rates suggested in pioneer papers about the Karakoram (e.g. Schneider, 1957; Desio, 1974; Goudie et al., 1984b) approximately coincide with recent analytic and modelling studies.

Data in our paper correspond well with published data from mineral cooling ages summarized by Thiede and Ehlers (2013) for the northern Greater Himalaya, adjacent to the Karakoram. These authors provide evidence that measured low denudation rates were < 1 mm/yr in the period 10-4 Ma followed by rapid faster rates of 1.2-2.6 mm/yr in the last cca. 4 Ma. It confirms our AFT results for the Hunza Karakoram, when we distinguish two stages of cooling: an Upper Miocene to Pliocene period of a slow cooling rate (ca. 0.1 mm/yr) followed by the Quaternary period of a relatively rapid cooling rate (ca. 2.6 mm/yr). Variability in denudation rates across the Himalaya as referred to in Thiede and Ehlers (2013) are observed as temporal and spatial differences: in a ca 1000 km long belt of the southern Greater Himalaya denudation rates were higher (cca. 1.5-3 mm/yr) between 10-2 Ma followed by lower rates of ca. 0.5-2.6 mm/yr in the last 2 Ma.

6. CONCLUSIONS

Low-temperature stage of the Hunza Karakoram crystalline rocks from Karakoram Metamorphic Complex and Karakoram Batholit gives evidence about exhumation processes during active collision orogeny. AFT-ages of studied rocks yielded between 3.9 [+ or -] 0.2 Ma to 9.7 [+ or -] 0.4 Ma and constrained the period of a rapid exhumation and unroofing as Upper Miocene to Quaternary. Time-temperature (t-T) curves of all the samples show two dominant trends of exhumation rate: the Upper Miocene to Pliocene period of a slow rate of ca. 0.1 km/Ma followed by the Quaternary period of a relatively rapid rate of ca.

2.6 km/Ma. Track-length distributions and modelled t- T curves defined AFT-ages of crystalline rocks as cooling ages accompanying the late Cenozoic denudation and uplift in Hunza Karakoram. This t-T evolution and uplift of rocks across the apatite total annealing zone to the current temperature on present erosion surface documents a very active orogenic belt. The erosion rate reached up to a maximum of cca. 4000 m from Upper Miocene to the present. The maximum (topographical) uplift of studied rocks can be estimated as more than 9 000 m. Rapid exhumation of crystalline rocks in the Hunza Karakoram has been caused by collision orogeny as well as intensive and variable climate-morphogenetic processes during the late Cenozoic. The high intensity of denudation and transport of eroded material suggest their long-term influence on the exhumation of deeper parts of the rock massifs during orogenetic processes in the Karakoram.

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DOI: 10.13168/AGG.2014.0010

Article info

Article history:

Received 28 February 2014

Accepted 4 June 2014

Available online 24 June 2014

ACKNOWLEDGEMENTS

The paper was completed in the framework of projects PRVOUK P43 "Geography" of the Faculty of Science, Charles University in Prague and AVOZ30130516 of the Academy of Sciences of the Czech Republic.

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Dagmar KORINKOVA (1), Martin SVOJTKA (1) and Jan KALVODA (2) *

(1) Institute of Geology, Academy of Sciences of the Czech Republic, Laboratory of Geological Processes, Rozvojova 269, Praha 6, 165 00, Czech Republic

(2) Charles University in Prague, Faculty of Science, Department of Physical Geography and Geoecology, Albertov 6, raha 2, 128 43, Czech Republic

Corresponding author's e-mail: kalvoda@natur.cuni.cz
Table 1 Apatite fission-track analytical data of the studied rock
samples from the Hunza Karakoram. Key: [[rho].sub.s] -spontaneous
track density of a sample; [N.sub.s]--number of tracks counted to
determine [[rho].sub.s]; [[rho].sub.i]--induced track density of a
sample measured in a muscovite external detector; [N.sub.i]--number
of tracks counted to determine [[rho].sub.i]; [[rho].sub.d]--induced
track density of glass dosimeter CN5 measured in a muscovite external
detector; [N.sub.d]--number of tracks counted to determine pd; AFT-
age--apatite fission-track age with its to error; n--number of
counted grains; P([chi square])--probability of obtaining the
observed value of [chi square] parameter, for N degree of freedom,
where N = (number of counted crystals)--1 (Galbraith, 1981; Green,
1981; Green et al., 1989); L--mean length of horizontal confined
fission tracks with 1 standard error (S.E.) in all crystallographic
orientations; N--number of measured tracks to determine L; [sigma]--
standard deviation for the length-distribution of confined fission
tracks.

No of       Locality       Elevation   [[rho].sub.s]   [[rho].sub.i]
sample                        [m]       ([N.sub.s])     ([N.sub.i])
                                       [x[10.sup.6]    [x[10.sup.6]
                                       [cm.sup.-2]]    [cm.sup.-2]]

2        2 km W from the     2 200     2.357 (1702)    8.536 (6163)
          confluence of
          the Hunza and
          Gilgit rivers

14         2 km W from       2 400     0.192 (1385)    1.437 (10375)
          town Aliabad

18       Rocky slopes N      2 550     0.204 (1474)    1.414 (10226)
            of Nagar
             village

77        Nunatac near       5 200     0.172 (1340)    1.616 (12600)
          S-wall of the
           Lupar Shar

72        Rock-wall of       5 500     0.211 (1439)    2.158 (14724)
          the cirque of
         Gharesa glacier

71        S-wall of the      5 650     0.167 (1514)    1.626 (14719)
          Trivor Massif

No of    [[rho].sub.d]   n          AFT-age            P([chi square])
sample    ([N.sub.d])         [Ma [+ or -] 1[sigma]]         [%]
         [x[10.sup.6]
         [cm.sup.-2]]

2         3.21 (6021)    70      9.9 [+ or -] 2.4            < 1

14        3.16 (5985)    70      5.3 [+ or -] 1.3            < 1

18        3.16 (5985)    67      6.3 [+ or -] 1.3            < 1

77        3.93 (6003)    66      7.5 [+ or -]1.8             < 1

72        3.16 (5985)    58      3.9 [+ or -] 0.8            < 1

71        3.16 (5985)    70      4.1 [+ or -] 0.9            < 1

No of    L (N) [[micro]m]     [sigma]     Cl-content
sample                       [[micro]m]     [wt%]

2        10.3 [+ or -] 2.8      0.2         0.025
               (155)

14       11.7 [+ or -] 2.3      0.2         0.015
               (108)

18       10.7 [+ or -] 2.4      0.2         0.016
               (147)

77       11.2 [+ or -] 2.6      0.2         0.012
               (162)

72       11.1 [+ or -] 2.3      0.2         0.035
               (178)

71       12.1 [+ or -] 2.2      0.2         0.024
               (167)

Table 2 Maximum denudation, rock uplift and surface uplift of the
studied samples from the Hunza Karakoram. Key: D--maximum denudation
(exhumation and erosion) from Upper Miocene to Recent [m];
[U.sub.S]--surface uplift of studied samples [m], which reflects
changes in surface elevation and responds to present elevation
of them; [U.sub.R]--rock uplift = [U.sub.S] + D [m].

No of    D [m]                           [U.sub.S]
sample                                   [m]

2        [less than or equal to] 4 000   2 200
14       [less than or equal to] 4 000   2 400
18       [less than or equal to] 4 000   2 550
77       [less than or equal to] 4 000   5 200
72       [less than or equal to] 4 000   5 500
71       [less than or equal to] 4 000   5 650

No of    [U.sub.R] [m]
sample

2        [less than or equal to] 6200
14       [less than or equal to] 6400
18       [less than or equal to] 6550
77       [less than or equal to] 9200
72       [less than or equal to] 9500
71       [less than or equal to] 9650
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Title Annotation:Original paper
Author:Korinkova, Dagmar; Svojtka, Martin; Kalvoda, Jan
Publication:Acta Geodynamica et Geromaterialia
Article Type:Report
Date:Jul 1, 2014
Words:8722
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