Abstract

Reconstructing the geometry of exhumation in the western Himalayan syntaxis region around Nanga Parbat is of critical importance to understanding how tectonics and surface processes interact during orogenesis. In order to determine the role played by the main Himalayan thrusts, we combine apatite U-Pb dating with apatite and zircon (U-Th-[Sm])/He analyses as well as apatite fission track dating from the Neelum valley region of Azad Jammu and Kashmir, Pakistan. Apatite U-Pb ages range from Proterozoic to mid-Miocene and can be separated into three age groups depending on the degree to which they have been affected by Himalayan tectonothermal events. Pooled fission track ages range from 7.0 ± 0.4 to 2.2 ± 0.4 Ma (1σ), apatite He ages range from 8.7 ± 0.2 to 2.0 ± 0.2 Ma, and zircon He ages range from 20.0 ± 0.4 to 6.1 ± 0.1 Ma. The data support rapid regional cooling at 10–8 Ma caused by the removal of 5–6 km of crust. This is synchronous with the initiation of movement along the Main Boundary thrust. Stream power analysis of the Neelum River catchment indicates a high normalized steepness index (ksn) of >500 m0.9 along the major river and lower ksn in the headwaters. The boundary between the different apatite U-Pb age groups and the transition from high ksn to lower ksn values coincide with the mapped trace of the Main Central thrust, corroborating the presence of the thrust in the southwestern part of the region. Compiling all apatite fission track cooling ages from the Nanga Parbat syntaxis region shows that cooling age contours are parallel to the major thrusts. Collectively these data provide convincing support for the contention that the well-established pattern of exhumation known from much of the Himalayan front continues around to the western syntaxis of the Himalayas.

INTRODUCTION

The western syntaxis of the India-Asia collision zone is arguably the most active and spectacular example of a collisional orogeny. It features extreme rates of both mountain building and erosion. Nanga Parbat, the ninth highest mountain on Earth, is at its center, and one of the largest drainage systems in Asia, the Indus River, crosses the region (Fig. 1A). The syntaxis is surrounded by several crustal-scale thrusts (Main Mantle thrust, MMT; Main Central thrust, MCT; Main Boundary thrust, MBT) (Burg et al., 1996; Guillot et al., 2008; Wilke et al., 2012; Pêcher et al., 2002, 2008; Zeitler et al., 2001a, 2001b; Zeitler, 1985; Fig. 1B). The highest rock uplift and erosion rates have been recorded here (Zeitler, 1985; Zeitler et al., 1982; Wilke et al., 2012) with fluvial incision rates as high as 12 mm/yr (Burbank et al., 1996). The core of the syntaxis records unusually young high-temperature cooling ages and contains leucogranites that are indicative of the extreme thermal events in the region (see review of Schneider et al., 2001; Koons et al., 2013).

Figure 1.

Topographic and geological maps showing the major geologic subdivisions of the northwest Himalayas in the western syntaxis region (after Wilke et al., 2012). (A) Topographic map of the western syntaxis. The red rectangle in the inset figure shows the location of Figure 1 in a regional context. H—Haramosh. (B) Geological map of the same region as A. Mint green—Karakoram (Asian plate); pink—Kohistan Ladakh arc; turquoise—Higher Himalayas (High Himalayan Crystalline and intrusive rocks—HHC); brown—Lesser Himalayas (metasediments); yellow—Sub-Himalayan Range (molasse sediments); HKS—Hazara-Kashmir syntaxis. MKT—Main Karakoram thrust; MMT—Main Mantle thrust; STDZ—South Tibet detachment zone; MCT—Main Central thrust; MBT—Main Boundary thrust; MFT—Main Frontal thrust. (C) Map showing published apatite fission track ages and contours in the region of the Nanga Parbat syntaxis. Green dots and contours are after Zeitler (1985); green area is region of high exhumation rates. Dashed parts of green contours are as shown by Zeitler (1985), but not necessarily supported by data and reinterpreted herein. Red dots are after Wilke et al. (2012 and references therein); purple dots are from van der Beek et al. (2009); and black dots in the core of Nanga Parbat–Haramosh massif indicate general representation of data along Indus Gorge and Astore valley transacts from Treloar et al. (2000). Contours are labeled for apatite fission track ages in million years for base-level samples. Dashed contours (red and green) show different possible extensions of Zeitler’s (1985) contours. Kaghan v.—Kaghan valley.

Figure 1.

Topographic and geological maps showing the major geologic subdivisions of the northwest Himalayas in the western syntaxis region (after Wilke et al., 2012). (A) Topographic map of the western syntaxis. The red rectangle in the inset figure shows the location of Figure 1 in a regional context. H—Haramosh. (B) Geological map of the same region as A. Mint green—Karakoram (Asian plate); pink—Kohistan Ladakh arc; turquoise—Higher Himalayas (High Himalayan Crystalline and intrusive rocks—HHC); brown—Lesser Himalayas (metasediments); yellow—Sub-Himalayan Range (molasse sediments); HKS—Hazara-Kashmir syntaxis. MKT—Main Karakoram thrust; MMT—Main Mantle thrust; STDZ—South Tibet detachment zone; MCT—Main Central thrust; MBT—Main Boundary thrust; MFT—Main Frontal thrust. (C) Map showing published apatite fission track ages and contours in the region of the Nanga Parbat syntaxis. Green dots and contours are after Zeitler (1985); green area is region of high exhumation rates. Dashed parts of green contours are as shown by Zeitler (1985), but not necessarily supported by data and reinterpreted herein. Red dots are after Wilke et al. (2012 and references therein); purple dots are from van der Beek et al. (2009); and black dots in the core of Nanga Parbat–Haramosh massif indicate general representation of data along Indus Gorge and Astore valley transacts from Treloar et al. (2000). Contours are labeled for apatite fission track ages in million years for base-level samples. Dashed contours (red and green) show different possible extensions of Zeitler’s (1985) contours. Kaghan v.—Kaghan valley.

The recognition of these extreme rates of mountain building and destruction has sparked an active discussion regarding their causes. Two opposing models have been developed: one hypothesis considers that both rock and surface uplift are directly related to the geodetic rates of contraction (>10–15 mm/yr) (Khan et al., 2008; Seeber and Pêcher, 1998; Garcia-Castellanos and Jiménez-Munt, 2015), the high erosion rates being the consequence. The alternative posits that erosion by rivers provides extreme denudational unloading and that the high uplift rates are the consequence, implying a direct feedback between deep-seated tectonic and surface processes (Koons et al., 2013; Zeitler et al., 2001a, 2001b). This recognition has led to the formulation of the tectonic aneurysm model (e.g., Zeitler et al., 2001a, 2001b), which implies localized surface uplift and exhumation in the syntaxis region only. While this model has found wide appeal for the interpretation of the western syntaxis, studies in the eastern syntaxis question the universal application of this model (King et al., 2016; Wang et al., 2014). Recent studies have shown that in addition to the normal convergence between India and Asia the extreme topography is sustained by the horizontal mass flux into the region that occurs due to the unusual geometry of the syntaxis (Whipp et al., 2014).

Many recent studies of the western syntaxis region discuss models that explain the inferred aneurysm (e.g., Koons et al., 2013). However, the southern limits of the rapid exhumation (or the aneurysm) remain poorly constrained (Fig. 1C) because data from the critical region directly south of the Nanga Parbat syntaxis (around the Neelum valley region of Azad Jammu and Kashmir, Pakistan) are missing (Figs. 1C and 2). Data from this region are crucial if we are to discern if the region of rapid exhumation is spatially confined to Nanga Parbat region (i.e., it forms an isolated aneurysm), or if it forms a lobe around the syntaxis, thus paralleling the major structures.

Figure 2.

Geological map of the Neelum valley region showing locations of samples collected for this study (red and green dots; after Fontan et al., 2000). Inset shows the broader structural subdivisions of the area. Note that (still controversial) Main Central thrust is marked at a different location in this map by Fontan et al. (2000) compared to others (e.g., Greco and Spencer, 1993; DiPietro and Pogue, 2004; Wilke et al., 2012; Pêcher et al., 2008; Searle et al., 2008; Guillot et al., 2008; and as shown in Fig. 1). Perm.-Tri.—Permian to Triassic; Carb.-Tri.–Carboniferous to Triassic; Camb.-Ord.—Cambrian to Ordovician; Precamb.-Camb.—Precambrian to Cambrian; Precamb.—Precambrian.

Figure 2.

Geological map of the Neelum valley region showing locations of samples collected for this study (red and green dots; after Fontan et al., 2000). Inset shows the broader structural subdivisions of the area. Note that (still controversial) Main Central thrust is marked at a different location in this map by Fontan et al. (2000) compared to others (e.g., Greco and Spencer, 1993; DiPietro and Pogue, 2004; Wilke et al., 2012; Pêcher et al., 2008; Searle et al., 2008; Guillot et al., 2008; and as shown in Fig. 1). Perm.-Tri.—Permian to Triassic; Carb.-Tri.–Carboniferous to Triassic; Camb.-Ord.—Cambrian to Ordovician; Precamb.-Camb.—Precambrian to Cambrian; Precamb.—Precambrian.

In order to understand the exhumation processes at the western syntaxis and to identify the southern limits of the rapidly exhuming region, we have performed a study of the low-temperature cooling history (e.g., Reiners and Brandon, 2006) of the Neelum valley region. We report apatite U-Pb thermochronometry (recording cooling through ∼450 °C; Chamberlain and Bowring, 2000), apatite fission track (AFT) ages (recording cooling through 80–140 °C), as well as apatite and zircon (U-Th-[Sm])/He ages (recording cooling through 40–80 °C and 140–205 °C intervals, respectively), for samples from two altitudinal profiles and an along-river transect. The data are complemented by geomorphic analyses of selected fluvial channels in the Neelum River catchment in order to constrain the geomorphological and geodynamic evolution of the Nanga Parbat syntaxis.

GEOLOGICAL BACKGROUND

The Himalayan mountain belt formed due to the collision of the Indian and Asian plates that initiated in the Paleocene (Ding et al., 2016). In the northwest Himalayas the main rock units are separated by regional-scale thrusts (Fig. 1B). North of Nanga Parbat, the MMT demarcates the southern boundary of Asia and the Kohistan-Ladakh arc and outlines the Nanga Parbat syntaxis. The High Himalayan Crystalline (HHC) rocks in the footwall are mainly high-grade metamorphic rocks intruded by granites (Calkins et al., 1975; Fontan et al., 2000). The HHC rocks were thrust onto the Lesser Himalayan rocks along the MCT during the early Miocene (Hodges et al., 1992). The Lesser Himalayan units are composed primarily of low-grade metamorphic and sedimentary rocks. Further south, the MBT forms the Hazara-Kashmir syntaxis (HKS), where rocks of the Lesser Himalayas are thrust onto the Neogene Sub-Himalayan molasse sediments (Kazmi and Jan, 1997; Shah, 2009).

Deformation has generally propagated from north to south. Asia and the Kohistan island arc were sutured in northern Pakistan between 102 and 85 Ma along the Main Karakoram thrust (Treloar et al., 1989). Further south, the collision of India with Asia and the Kohistan-Ladakh island arc was not synchronous: India collided in northern Pakistan with the Kohistan-Ladakh island arc along the MMT at 65–55 Ma (Kazmi and Jan, 1997), but only at 54 Ma in the Ladakh region of northwest India (Patriat and Achache, 1984). However, more recent studies have shown that initial collision occurred between India and the Kohistan-Ladakh island arc ca. 50 Ma followed by collision of this assembled landmass with Asia ca. 40 Ma (Bouilhol et al., 2013). Regardless of the chronology, this resulted in sandwiching of the Kohistan-Ladakh island arc between Asian (Karakoram) and Indian (Higher Himalayan) crust at the northwestern edge of Indian plate. Elsewhere, Indian plate is sutured directly to the Asian (Eurasian) plate along the Tsangpo suture (Bouilhol et al., 2013). HHC rocks were exhumed from mid-crustal levels along the MCT between 24 and 10 Ma (Searle et al., 2008). Deformation then shifted to lower structural levels to the south. Movement on the MBT initiated in the late Miocene (before10 Ma) in the western Himalaya (Meigs et al., 1995), followed by the development of the Main Frontal thrust (or Salt Range thrust), the youngest of all the regional faults, at 5.4–1.0 Ma (Kazmi and Jan, 1997).

Despite this well-defined sequence of major tectonic activity along the major thrusts, it is not clear if the final exhumation of rocks and the elevated topography of the present-day landscape are related to the same series of thrusting events. For example, although the main movement along the MCT is thought to have taken place during the early to middle Miocene (Butler et al., 1989; Vannay et al., 2004), AFT ages from HHC rocks in the syntaxis region are substantially younger, and an isolated area of extreme exhumation has been recognized (Zeitler et al., 1982; Zeitler, 1985). Generally AFT cooling ages are ca. 1 Ma in the core region of the Nanga Parbat syntaxis, whereas they are as old as 6 Ma toward the southwest in the Kaghan and Indus valleys (Fig. 1C). Wilke et al. (2012) reported AFT ages of ca. 10 Ma or younger from the upper Kaghan valley, but their samples are not from valley bottoms so they do not record the most recent part of the thermal history. Although the MMT may only have remained active from early Eocene until late Oligocene or early Miocene (DiPietro and Pogue, 2004), many of the low-temperature cooling ages from the Kohistan arc are significantly younger (20–10 Ma; e.g., Zeitler, 1985). Thus, much of the final stage of exhumation occurred after the majority of the tectonic history identified by geochronology, and paleomagnetic, metamorphic, and stratigraphic methods (Treloar et al., 1989; Kazmi and Jan, 1997; Patriat and Achache, 1984; Searle et al., 2008; Meigs et al., 1995).

It has been suggested that the rapid exhumation may be related to rock uplift over a crustal-scale ramp in the basal décollement, and not to individual structures (Bollinger et al., 2004, 2006), and the pronounced three-dimensional (3D) nature of the exhumation history has been documented (Whipp et al., 2007; Herman et al., 2010). While rock uplift over an unexposed basal décollement implies a more distributed young exhumation and a complicated relationship between cooling and exhumation, surface uplift of the region appears to have occurred by the Oligocene. The Deosai Plateau to the northeast of the study region is considered to be a remnant of this early surface uplift (van der Beek et al., 2009). While the surface uplift at Nanga Parbat west of the Deosai Plateau is likely to have occurred in the past few million years (Whipp et al., 2014), the Kashmir Basin south of Nanga Parbat has remained at a low elevation, accommodating terrestrial sediment for the past 4 m.y. (Burbank and Johnson, 1982).

The geology of the Neelum valley region was mapped by Malik et al. (1996) and Fontan et al. (2000) (Fig. 2). The region is in the hanging wall of the MBT and forms three distinct tectonic units separated by two thrusts, the Gumot shear zone (GSZ), a 100–200-m-wide ductile shear zone inside the HHC, and the MCT. From the structurally highest to lowest levels the tectonic units separated by these thrusts are the Shontar unit in the hanging wall of GSZ, the Kalapani unit between the GSZ and MCT, and the Salkhala unit below the MCT (inset, Fig. 2). The position of the MCT in the Neelum valley region is subject to debate. Fontan et al. (2000) proposed that the MCT crosses the Neelum River near Doarian village (Fig. 2). In contrast, Greco and Spencer (1993) mapped a mylonite zone along the MCT that extends through the Leswa section, crossing the Neelum River between Nauseri and Jura (Fig. 2). This location is widely acknowledged to represent the position of the MCT in the Neelum valley region (Wilke et al., 2012; Pêcher et al., 2008; Searle et al., 2008; Guillot et al., 2008; DiPietro and Pogue, 2004; Greco and Spencer, 1993), and is shown in Figure 1. During field work for this study we observed a mylonite zone at a similar location along the Leswa road. The timing of thrusting on these structures is not known and is correlated with movement on the MCT in other portions of the northwest Himalayas where it was active until 16 Ma (Vannay et al., 2004), and possibly reactivated later (Catlos et al., 2001; Hodges et al., 2004). The morphology of the Neelum River catchment is similar to the Indus valley to the northwest. It spans an elevation range from 700 m (at the junction with the Jhelum River) to ∼5000 m, and crosses almost the entire morphological range of the Himalayas from the Punjab plains to the high Deosai Plateau, which is thought to be a preserved remnant of the Eocene Tibetan Plateau in the east (van der Beek et al., 2009).

LOW-TEMPERATURE THERMOCHRONOLOGY: SAMPLES AND TECHNIQUES

Rock samples were collected along high-relief sections from near the Neelum River to the adjoining peaks in the Neelum valley. The samples were collected near major regional-scale structures (e.g., the MCT and MBT) along two altitudinal profiles (Fig. 2); one near Kel in the upper parts of the Neelum valley and the second along the Leswa road in the lower part. The Leswa road leaves the main Muzaffarabad-Kel road in the Neelum valley, crosses a pass, and joins the valley again near Maira (Fig. 2). Sampling sites cover the maximum vertical range with minimum horizontal separation between samples of the same profile. Samples were also collected between the two transects along the Neelum River.

We collected 10 samples between 2000 m and 4200 m elevation along the Kel profile. The average vertical separation between samples is 200–250 m (Table 1). Seven samples were collected along the Neelum River between the Kel and Leswa sections with ∼100 m vertical separation. Thirteen samples were collected along the Leswa altitudinal profile. Samples were taken from both sides of the Leswa pass between ∼1200 m at the Neelum River and ∼2700 m at the pass (Table 1). Two samples are sandstones of the Murree Formation, one sample is Panjal andesite, and the remaining 10 samples are metamorphic rocks from the Salkhala Group (sensu Fontan et al., 2000). The quality and quantity of apatite were variable, so only a subset of samples could be used for analysis. Where possible we have combined apatite U-Pb ages, AFT ages, and (U-Th-[Sm])/He zircon and apatite ages in order to obtain the cooling history from ∼450 to ∼40 °C.

TABLE 1.

DETAILS OF SAMPLES TAKEN FOR LOW-TEMPERATURE THERMOCHRONOLOGIC ANALYSIS

We selected 16 samples for analysis. Apatites from 12 samples were dated using the U-Pb and AFT methods (Table 2): 4 samples from the Kel profile, 3 samples from the Neelum River, and 5 from the Leswa profile. Eight samples (largely a subset of the 12 used for U-Pb and AFT dating) were dated by the apatite U-Th-[Sm]/He (AHe) method (Farley, 2002) (Table 3) and seven samples were dated by the zircon U-Th/He (ZHe) method (Reiners, 2005) (Table 4). (For details of laboratory methods, see the GSA Data Repository Item1.)

TABLE 2.

APATITE FISSION TRACK AND U-Pb RESULTS

TABLE 3.

APATITE (U-Th-Sm)/He RESULTS

TABLE 4.

ZIRCON (U-Th)/He RESULTS

The thermal history of Kel and Leswa profiles have been modeled using QTQt version 5.3.3 (Gallagher, 2012). Modeled thermal histories used all thermochronometry data. This incorporated the fission track annealing model of Ketcham et al. (2007) and the effect of radiation damage on He ages using the models of Flowers et al. (2009) for apatite and Guenthner et al. (2013) for zircon. The high-temperature constraint employed the weighted mean U-Pb age (28 ± 6 Ma) of all the samples that have Cenozoic (unanchored) lower intercept ages and the corresponding U-Pb apatite closure temperature of 450 ± 75 °C. The maximum temperature change (heating or cooling rate) for all model runs was limited to 1000 °C/m.y. The present-day temperature offset between the top and bottom samples of the Kel and Leswa profiles was set at 15 ± 5 °C and 10 ± 5 °C and a present-day temperature of 5 ± 5 °C and 10 ± 10 °C was used for the top sample in each profile, respectively. The paleotemperature offset is based on the total vertical separation between the top and bottom samples of a profile section. The models were run for 200,000 iterations as burn-in (which were discarded) and the subsequent 200,000 iterations were used for the analysis.

THERMOCHRONOLOGY RESULTS

Apatite U-Pb ages for unknowns (uncorrected for common Pb) were determined by fitting isochrons on a Tera-Wasserburg (TW) concordia to determine lower intercept 238U/206Pb ages (Fig. 3; see Data Repository Item). The data plot into three groups: (1) apatites that are on a well-defined discordia with Cenozoic lower intercepts that range from 32.0 ± 26.0 to 17.0 ± 10.0 Ma (2σ, unanchored) or 43.0 ± 12.0 to 18.5 ± 4.6 Ma (2σ, anchored at a 207Pb/206Pb initial value of 0.837 ± 0.005 corresponding to the Stacey and Kramers, 1975, terrestrial Pb composition ca. 28 Ma) (Fig. 3A; Table 2); (2) samples that yield Cenozoic lower intercepts ranging from 42.0 ± 11.0 to 20.0 ± 19.0 Ma (2σ, unanchored) or 48.3 ± 9.1 to 28.9 ± 4.0 Ma (2σ, anchored at 0.837 ± 0.005) but also contain older grains that can be clearly identified as a separate group (Fig. 3B). It is important to note that only the younger grains were used to fit the isochrons. The young apatite age population was also identified on the basis of the trace element composition. For example, the apatites yielding the Cenozoic lower intercept in sample N5 (Fig. 3B) are depleted in La relative to the older grains that are partly affected by Himalayan exhumation. (3) The third group is apatite that yields Proterozoic lower intercepts (Fig. 3C).

Figure 3.

Representative examples of U-Pb Tera-Wasserburg (TW) concordia lower intercept ages for each of the three resultant groups. MSWD—mean square of weighted deviates. (A) Example for the completely affected samples from Kel profile in the hanging wall of the Gumot shear zone (GSZ). (B) Example of a partially affected sample from within the High Himalayan Crystalline rocks (red data points are not used for the calculation of the intercept). (C) Example for an unaffected sample from the Leswa profile in the Lesser Himalaya. Discordia diagrams for all other measured samples are shown in Figure S1. (D) Weighted (Wtd.) mean age for all the affected samples. (E) Schematic map of the Neelum valley region showing the distribution of completely, partially, and unaffected samples (yellow ellipses; see also Fig. 2 for more detail). MCT—Main Central thrust; MBT—Main Boundary thrust.

Figure 3.

Representative examples of U-Pb Tera-Wasserburg (TW) concordia lower intercept ages for each of the three resultant groups. MSWD—mean square of weighted deviates. (A) Example for the completely affected samples from Kel profile in the hanging wall of the Gumot shear zone (GSZ). (B) Example of a partially affected sample from within the High Himalayan Crystalline rocks (red data points are not used for the calculation of the intercept). (C) Example for an unaffected sample from the Leswa profile in the Lesser Himalaya. Discordia diagrams for all other measured samples are shown in Figure S1. (D) Weighted (Wtd.) mean age for all the affected samples. (E) Schematic map of the Neelum valley region showing the distribution of completely, partially, and unaffected samples (yellow ellipses; see also Fig. 2 for more detail). MCT—Main Central thrust; MBT—Main Boundary thrust.

For all three groups, the first U-Pb age column in Table 2 lists unanchored lower intercept TW concordia ages where the isochron regression was constrained by the analyses alone. Lower intercept TW concordia ages are listed in Table 2 as anchored at a 207Pb/206Pb initial value of 0.837 ± 0.005, which represents the common Pb composition at 28 Ma calculated by the Stacey and Kramers (1975) crustal Pb evolution model. The weighted mean age of all the unanchored Cenozoic lower intercept ages is 27.3 ± 5.6 Ma (Fig. 3D).

AFT ages range from 7.0 ± 0.4 to 2.2 ± 0.4 Ma (1σ) (Fig. 4; Table 2). Only sample K2 had sufficient confined tracks (n = 44) to allow track length measurements. It has a mean track length of 13.36 ± 1.65 µm. The kinetic parameter, Dpar, shows a range from 1.11 to 1.59 µm, while the chlorine content ranges from 0.01 to 0.74 wt%. All samples passed the chi-squared (χ2) test (Galbraith, 1981, modified for laser ablation–inductively coupled plasma–mass spectrometry fission track dating by Donelick et al., 2005).

Figure 4.

Apatite fission track (AFT) thermochronology done for this study shown as a plot of AFT ages versus elevation. Note that sample K10 is shown in blue (i.e., part of the Kel profile), but it is at Neelum River level. Its value can therefore also be read in connection with the ages shown in red (Neelum River samples). Corresponding logic applies to sample N8 (see sample locations in Fig. 2).

Figure 4.

Apatite fission track (AFT) thermochronology done for this study shown as a plot of AFT ages versus elevation. Note that sample K10 is shown in blue (i.e., part of the Kel profile), but it is at Neelum River level. Its value can therefore also be read in connection with the ages shown in red (Neelum River samples). Corresponding logic applies to sample N8 (see sample locations in Fig. 2).

AFT ages at the base (2015 m) and top (3916 m) of the Kel profile are ca. 4 Ma and ca. 7 Ma, respectively, and show a positive correlation with elevation. AFT ages from the Leswa profile show no resolvable relationship with elevation, ranging from 3.5 to 2.2 Ma. The ages of the six samples are indistinguishable within analytical uncertainty, indicating rapid cooling through the apatite partial annealing zone, and these ages are likely linked to rapid exhumation. Three AFT ages along the Neelum River (3.9–3.7 Ma) are indistinguishable within analytical uncertainty. Sample N8, from the base of the Leswa profile, which is also the lowest sample of the Neelum River transect, yields a slightly younger cooling age of 2.9 ± 0.3 Ma (Fig. 4).

Individual uncorrected ZHe ages range from 13.3 ± 0.3 to 5.2 ± 0.1 Ma (1σ), while corrected ages range from 20.0 ± 0.4 to 6.1 ± 0.1 Ma (1σ) (Fig. 5; Table 4). Within-sample age variation is significant, typical of many ZHe studies. This may reflect U and/or Th zonation (Dobson et al., 2008) and/or radiation damage (e.g., Guenthner et al., 2013). Average ZHe ages range from 16.5 ± 2.2 to 8.8 ± 0.7 Ma and there is no significant variation with elevation.

Figure 5.

Plots for Kel, Neelum River and Leswa samples showing relationship between zircon U-Th/He (ZHe) and apatite fission track (AFT) and U-Th-[Sm]/He (AHe) ages, plotted against the sample elevations. Note that the Neelum River plot shares samples K10 and N8 with Kel and Leswa plots, respectively (see text for details). Samples not used for calculation of average ages are shown in the lighter shade of the same color. Average (Ave.) sample AHe and ZHe ages are shown by a larger symbol of the same color.

Figure 5.

Plots for Kel, Neelum River and Leswa samples showing relationship between zircon U-Th/He (ZHe) and apatite fission track (AFT) and U-Th-[Sm]/He (AHe) ages, plotted against the sample elevations. Note that the Neelum River plot shares samples K10 and N8 with Kel and Leswa plots, respectively (see text for details). Samples not used for calculation of average ages are shown in the lighter shade of the same color. Average (Ave.) sample AHe and ZHe ages are shown by a larger symbol of the same color.

Single grain AHe ages range from 7.6 ± 0.2 to 1.4 ± 0.1 Ma (1σ, uncorrected) and from 8.7 ± 0.2 to 2.0 ± 0.2 Ma (1σ, Ft corrected) (Fig. 5; Table 3). Average AHe ages typically overlap or are slightly younger than the corresponding AFT ages (Fig. 5). As with the AFT data, there is a weak trend of increasing AHe ages with elevation for the Kel profile, but no significant AHe age deviation with elevation for the Leswa profile is observed (Fig. 5; Table 3). Apatites from sample L6 were small and of low quality, and the oldest AHe age from this sample was not used in the calculation of the average age (Table 3).

THERMAL MODELING

In order to improve upon the interpretation of the ages described here, a thermal history for the region was modeled with QTQt (Gallagher, 2012), using the combined data sets from the different thermochronometers. For the Kel profile, which represents the structurally highest rocks, five samples (K1, K2, K3, K6, K10; Tables 24) from which we obtained AHe, AFT, and ZHe data were used for thermal history modeling. Because the vertical separation of the Kel profile samples is more than 2000 m (Table 1), a paleotemperature offset between the top and bottom samples of 60 ± 30 °C was used in the modeling. The modeled thermal history (i.e., the weighted mean model) of the Kel profile (Fig. 6) shows that the region has a complicated cooling history. The data record the cessation of the first cooling phase ca. 19 Ma, the upper sample cooling to ∼120 °C at that time. This was followed by reheating of ∼60 °C until ca. 10 Ma, followed in turn by a discrete cooling event between 10 and 8 Ma with a cooling rate of ∼100 °C/m.y. A final phase of slow cooling to surface temperatures may have involved a period of minor reheating between 8 and 6 Ma.

Figure 6.

Thermal history modeling of thermochronological data for the Kel and Leswa profiles. For clarity, thermal histories are shown for top and bottom samples (thick black lines) with the gray region showing the 95% credible interval (the Bayesian form of confidence intervals) for top and bottom samples combined together. Closure temperatures of apatite U-Th-[Sm]/He (AHe), apatite fission track (AFT), and zircon U-Th/He (ZHe) systems are also indicated with dotted lines at 60, 120, and 180 °C respectively. The orange box shows the range of general priors, i.e., the time-temperature box used for start of modeling the thermal history and its values are time = 17 ± 17 Ma (to cover the entire time range of weighted mean apatite U-Pb age of 28 ± 6 Ma) and temperature = 150 ± 150 °C (to cover the entire temperature range of ZHe, AFT, and AHe systems). The black box shows a high temperature constrained point, which is the weighted mean apatite U-Pb age: in this case, 28 ± 6 Ma and 475 ± 75 °C.

Figure 6.

Thermal history modeling of thermochronological data for the Kel and Leswa profiles. For clarity, thermal histories are shown for top and bottom samples (thick black lines) with the gray region showing the 95% credible interval (the Bayesian form of confidence intervals) for top and bottom samples combined together. Closure temperatures of apatite U-Th-[Sm]/He (AHe), apatite fission track (AFT), and zircon U-Th/He (ZHe) systems are also indicated with dotted lines at 60, 120, and 180 °C respectively. The orange box shows the range of general priors, i.e., the time-temperature box used for start of modeling the thermal history and its values are time = 17 ± 17 Ma (to cover the entire time range of weighted mean apatite U-Pb age of 28 ± 6 Ma) and temperature = 150 ± 150 °C (to cover the entire temperature range of ZHe, AFT, and AHe systems). The black box shows a high temperature constrained point, which is the weighted mean apatite U-Pb age: in this case, 28 ± 6 Ma and 475 ± 75 °C.

For the Leswa profile near the MBT, the AHe, AFT, and ZHe data from six samples (N8, L2, L6, L7, L9, L10; Tables 24) were used for thermal history modeling. As this sample set spans the widely acknowledged trace of the MCT (e.g., Greco and Spencer, 1993), we modeled the samples from either side of this structure separately. This yielded results that are similar to the modeled thermal history of all the samples together and thus provides evidence that all samples across the trace of the MCT have the same thermal history below the ZHe closure temperature (∼180 °C). The ∼1350 m of vertical separation between the top and bottom samples required a 40 ± 20 °C paleotemperature offset. It is interesting that the modeling results for the Leswa profile show a thermal evolution similar to that of the Kel profile, particularly since ca. 10 Ma (the timing of initiation of the MBT). The Leswa region underwent a rapid cooling event ca. 9 Ma, during which the uppermost samples cooled from ∼180 to 60 °C in <1 m.y. (Fig. 6). Samples were reheated by ∼60 °C from ca. 8 to ca. 3 Ma, followed by a second short-duration (∼1 m.y.) rapid cooling event that brought rocks from 120–100 °C to surface temperatures ca. 2 Ma.

MORPHOLOGICAL ANALYSIS

In order to characterize the modern erosional regime we report a morphological analysis of selected fluvial channels in the region. Channel profile analysis was carried out in ArcMap 10.1 using the 1 arc second (∼30 m) resolution ASTER GDEM version 2 (Advanced Spaceborne Thermal Emission and Reflection Radiometer Global Digital Elevation Model; https://asterweb.jpl.nasa.gov/gdem.asp) data (Fig. 7). Following common procedures, we study channel characteristics and compare them to an assumed geomorphic steady state, where channel slope (S) and drainage area (A) are related by a power law function S = ksA–θ, where ks and θ are referred to as steepness and concavity indices, respectively (e.g., Wobus et al., 2006, and references therein). The values of ks and θ can be measured directly from digital elevation model data by performing a regression analysis on a log-log plot between A and S. The normalized steepness index (ksn) is calculated using a fixed reference concavity value (θref), which is usually ∼0.45 (Wobus et al., 2006). The ksn is proportional to erosion rate and can be used to infer zones of variable exhumation related to fault activity (Whittaker, 2012). The ksn of all the streams was calculated in Matlab R2011b by linking it to the ArcMap 10.1 through the Profiler toolbar using a value of 0.45 for θref (for details, see Whipple et al., 2007).

Figure 7.

Results of geomorphic analyses of the western Himalayan syntaxis area. (A) Topographic map and results of a numerical analysis of the stream power; ksn is steepness index. MMT—Main Mantle thrust; MCT—Main Central thrust; MBT—Main Boundary thrust; GSZ—Gumot shear zone. (B) Long profiles of selected streams (i.e., Jhelum, Neelum, Kunhar, and Sind Rivers). Stream power is color coded for steepness index, normalized to a reference concavity index of 0.45. White stars on map and blue plus signs on long profiles show major knickpoints 90–110 km upstream from the stream junction. Blue polygon outlines the Neelum River catchment. Flat portion of Jhelum River long profile upstream of the major knickpoint shows the extent of the Kashmir Basin.

Figure 7.

Results of geomorphic analyses of the western Himalayan syntaxis area. (A) Topographic map and results of a numerical analysis of the stream power; ksn is steepness index. MMT—Main Mantle thrust; MCT—Main Central thrust; MBT—Main Boundary thrust; GSZ—Gumot shear zone. (B) Long profiles of selected streams (i.e., Jhelum, Neelum, Kunhar, and Sind Rivers). Stream power is color coded for steepness index, normalized to a reference concavity index of 0.45. White stars on map and blue plus signs on long profiles show major knickpoints 90–110 km upstream from the stream junction. Blue polygon outlines the Neelum River catchment. Flat portion of Jhelum River long profile upstream of the major knickpoint shows the extent of the Kashmir Basin.

The ksn values of almost all the streams are lowest near the headwaters (ksn < 200 m0.9) and in the lowest reaches of the Neelum River (yellow parts of streams in Fig. 7A). In contrast, the central parts of the Neelum River are characterized by high ksn (ksn > 500 m0.9; red parts of streams in Fig. 7A). The transition from high to low ksn values along the Neelum River main channel occurs at the location where it crosses the MBT and MCT (sensu Greco and Spencer, 1993). In contrast, the Kunhar and Jhelum Rivers show comparatively low ksn values (200–500 m0.9) in main channels except small segments of higher ksn values that are located primarily close to the regional faults and are thus linked to changes in lithology (Figs. 7A and 1B). In summary, the variable steepness index of the Neelum River catchment has all the characteristics of a catchment that is either not in a geomorphic steady state, or a steady-state catchment with variable rock uplift rates in different subregions.

Channel profiles of the four rivers are shown in Figure 7B. These rivers provide key information for our following interpretation. The Neelum River is of principal interest to our study. The Jhelum River, which joins the Neelum from the east just below the MBT, is the principal river draining the Kashmir Basin to the south of the study region, and was chosen because the history of its confluence will be inferred from the thermochronological data. The Kunhar River is roughly parallel to the Neelum valley to the west and north. It was chosen because its confluence with the Jhelum is only 10 km downstream of the Jhelum-Neelum confluence and because it is expected to exhibit similar morphological channel characteristics. The Sind River that flows westward through the Kashmir Basin was chosen because it does not cross any of the major faults that dissect the Neelum valley region and can thus be used for comparison.

Knickpoints have been identified on the long profiles of Kunhar, Jhelum, Neelum, and Sind Rivers (Fig. 7B). The confluence of the Neelum and Kunhar Rivers with the Jhelum River occur within ∼10 km of each other on the western limb of a major antiformal structure of northwestern Himalayas, the HKS. These three rivers show knickpoints along their long profiles at a distance of ∼90 km to ∼110 km upstream from the confluence. It is interesting that the Sind River, which does not cross any of the major Himalayan structures and joins the Jhelum River in the Kashmir Basin, also has a knickpoint ∼80 km upstream, where the river long profile shows a change from apparently equilibrated channel (downstream) to a stepped morphology (upstream). Knickpoints identified here show a good match with the ksn values of the corresponding rivers (Fig. 7).

DISCUSSION

Summary of Cooling Ages

The thermochronometric analyses provide series of ages that document different parts of the cooling history. Starting with the highest closure temperature system (U-Pb apatite) it was shown that the samples plot into three distinct age groups, and we interpret these three groups in terms of the effects of cooling due to exhumation related to the Himalayan orogeny as (1) completely affected, (2) partially affected, and (3) unaffected ages. One example of each is shown in Figure 3 (all other data are listed in the Data Repository Item).

All samples from the Kel profile in the hanging wall of the GSZ (according to the map of Fontan et al., 2000) are within the HHC and show completely affected apatite U-Pb ages that range between 43.0 and 18.5 Ma. Assuming a surface temperature of 20 °C, a closure temperature of 450 °C for U-Pb system in apatite, and following Wilke et al. (2012) by assuming 30 °C/km as the geothermal gradient, a total exhumation of more than 14 km is inferred for the structurally highest sample and more than 16 km for the structurally lowest sample of the Kel profile. The partially affected samples of the second group all come from the lower part of the Neelum valley and consist of granites to granitic gneisses (Table 1; Figs. 2 and 3E). These analyses may represent old (Proterozoic?) apatites that have been partly to completely affected during Himalayan orogenesis, with possible additional growth of new metamorphic apatite. The third (oldest) group is from the Leswa profile, where four gneisses yield Proterozoic apatite U-Pb ages implying that they have not been affected by Himalayan tectonothermal events (Fig. 3E; Fig. S1 in the Data Repository Item). These old U-Pb apatite ages suggest that the rocks of the Lesser Himalayas (between the MBT and MCT) have undergone total Himalayan exhumation of <∼14 km but certainly >5 km (based on the late Cenozoic AHe, AFT, and ZHe age data).

The low-temperature thermochronometry data indicate that all samples record Himalayan tectonics. Both profiles record cooling through the ZHe partial retention zone (180–140 °C) between 17 and 9 Ma, with no significant difference between the two transects. Assuming generally accepted values for the closure temperatures of the different systems (i.e., ZHe = cooling through 180 °C and AHe = cooling through 50 °C), a mean cooling rate can be estimated. The average ZHe age is ca. 11 Ma and the average AHe age is ca. 4 Ma, reflecting a cooling rate for the region of ∼19 °C/m.y., broadly consistent with the thermal history model derived from QTQt. This is consistent with an exhumation rate of >0.6 mm/yr (for an assumed regional geothermal gradient of 30 °C/km; Wilke et al., 2012). However, due to the effect of heat advection that accompanies rapid exhumation, these calculated exhumation rates should be considered as an upper limit.

Tectonic Interpretation

This new data set allows us to propose new constraints on the history of rock uplift and exhumation in the Neelum valley region and consequently resolve the evolution of the western Himalayan syntaxis region. While previous studies have developed 3D models, we show that much of the thermal history derived here can be understood using a simple 2D approach, based on a southwest-northeast profile from the Jhelum River confluence toward the Deosai Plateau (Fig. 8).

Figure 8.

Five time slices of the interpreted surface uplift and erosion history of the Neelum valley region along a schematic southwest-northeast section more or less along the Neelum River. MCT—Main Central thrust; MBT—Main Boundary thrust; GSZ—Gumot shear zone. Note that different symbols convey graphic representation of sample locations: star —Kel, square—Neelum + Leswa (east of MCT), circle—Leswa (west of MCT), black—current location, gray—location at previous time slice. Red dashed lines are 60, 120 and 450 °C isotherms.

Figure 8.

Five time slices of the interpreted surface uplift and erosion history of the Neelum valley region along a schematic southwest-northeast section more or less along the Neelum River. MCT—Main Central thrust; MBT—Main Boundary thrust; GSZ—Gumot shear zone. Note that different symbols convey graphic representation of sample locations: star —Kel, square—Neelum + Leswa (east of MCT), circle—Leswa (west of MCT), black—current location, gray—location at previous time slice. Red dashed lines are 60, 120 and 450 °C isotherms.

The first constraint on the tectonothermal evolution is given by apatite U-Pb ages that constrain exhumation through ∼450 °C (Chamberlain and Bowring, 2000). These data show that there are regions that have not undergone substantial Himalayan tectonothermal events, while other samples have been partly or fully affected by Himalayan tectonics in the Cenozoic (Fig. 3E; Table 2). The boundary between these two domains is between samples L2 and L6 along the Leswa road. This likely corresponds to the MCT, and suggests that movement on this structure in the Oligocene (ca. 27 Ma, as given by the weighted mean U-Pb cooling age) caused rock and surface uplift, steepening of the topography, and ultimately erosion of the hanging wall. As the samples with young apatite U-Pb ages from the Kel profile are also in the hanging wall of the GSZ, this Oligocene rock uplift may have been generated in part by motion along the GSZ.

The differing U-Pb ages along the Leswa profile are consistent with the position of the MCT as suggested by Greco and Spencer (1993; Figs. 1 and 2). We suggest that the MCT remained inactive since at least the early-middle Miocene, as thermal history modeling of samples from either side of the MCT suggests a consistent shared cooling evolution since that time. The mixed U-Pb age samples record the combined effects of thrusting, initially along the MCT and later along the MBT (Fig. 8). The young U-Pb apatite age samples from the Kel profile are the result of greater amounts of exhumation and the combined effect of thrusting along the GSZ, MCT, and MBT (Fig. 8). Detrital zircon U-Pb ages also confirmed enhanced Himalayan exhumation at 35–23 Ma (Ding et al., 2016).

Following this early stage of exhumation, the Kel profile rocks were at 180–100 °C ca. 19 Ma. Cooling to this point was likely a result of continuous erosion following movement on the MCT and GSZ so that the relief created by the earlier event was removed (Fig. 8). It is possible that MCT was active during this entire period. Reheating (∼60 °C) between 19 and 10 Ma has no obvious associated regional tectonic event; it may simply relate to the rapidly exhuming hot rocks from great depths from the south focused into the Nanga Parbat region (Koons et al., 2002) and the resultant active hydrothermal system (Chamberlain et al., 2002; Craw et al., 1994). Rapid cooling at 10–8 Ma coincided with the first movement of the MBT (Meigs et al., 1995), and likely records the onset of rock uplift and erosion of the hanging wall. This is evident from the thermal history of the Leswa profile (Fig. 6). However, rapid cooling of the Kel profile at the same time (i.e., 10–8 Ma) may represent activity along the GSZ. The north to south propagation of deformation in the Himalayas at that time (Vannay et al., 2004) is consistent with the MBT being the main active tectonic structure, which in turn implies that the MCT had ceased to be active by that time (Vannay et al., 2004). Both sides of the MCT have a similar cooling history from between 27 Ma (based on U-Pb apatite data) and 11 Ma (based on ZHe data) onward. Treloar et al. (1992) suggested that the southwest-verging Kashmir thrust system (which includes both the MCT and MBT) at the eastern limb of the HKS (southwestern part of our study region) was actively propagating to the southwest with its frontal thrusts cutting up through the south-southeast–verging Pakistan thrust system on the western limb of the HKS. This also supports the hypothesis that the MBT was the locus of the main tectonic activity ca. 10 Ma. Formation of the MBT was followed by nearly isothermal to slow reheating conditions (Fig. 6). Final cooling recorded by the Kel profile is likely due to incision of the Neelum River catchment into an existing topographic plateau, whereas the Leswa profile shows a second rapid cooling event ca. 3 Ma (Fig. 6), possibly due to thrusting along the MBT.

The interpretation of the final stages of exhumation is supported by aspects of the geomorphic analysis. For example, the high ksn values in the hanging wall of the MBT in the Neelum valley may indicate recent motion along this structure, but the sharp lithological contrast across its trace may also explain the change in the steepness index (Figs. 2 and 7). We interpret the low ksn parts in the headwaters of almost all the small streams as areas where the incision has not yet propagated into an uplifted region. This is consistent with the Deosai Plateau being the remnant of an Eocene rock and surface uplift event. The high ksn in the main channel suggests that the entire Neelum River catchment may be the product of a young river piracy event by the Jhelum River, possibly due to the formation of the Kashmir Basin ca. 5 Ma (Alam et al., 2015) and the resultant drainage convergence into the Jhelum River. Rapid cooling ca. 3 Ma as documented predominantly for the Leswa profile may be related to the incision of ∼1000 m (Fig. 7B) due to the passing of a knickpoint along the Neelum River. Our interpretation is also consistent with the slight increase in AFT age toward the headwaters of the catchment.

Cause of Exhumation

The AFT data can be combined with previously published ages from the Nanga Parbat region to make a substantial improvement on the interpretation of the nature of exhumation around the western syntaxis. According to the interpretation of Zeitler (1985), contours of AFT age are continuous across the syntaxis and are perpendicular to the major structures in the region, with ages at base level in the Neelum valley region predicted to be older than 5 Ma (Fig. 1C). For tens of kilometers around Nanga Parbat, the topology of these contours remains consistent with the AFT data from Treloar et al. (2000), van der Beek et al. (2009), Wilke et al. (2012), and other cooling age data (e.g., Schneider et al., 2001). Zeitler (1985) inferred a region of extreme exhumation only in the region at, and north of, Nanga Parbat, which has remained the basis for many crustal exhumation models since (e.g., Zeitler et al., 2001a, 2001b; Koons et al., 2013).

In order to broaden the interpretation of the published AFT cooling ages to the larger syntaxis region yet remain compatible with previous studies, we follow the method of Zeitler (1985) and show only the low-altitude samples K10, N5, N7, and N8 (yellow dots in Fig. 9; Table 2). AFT ages of these samples range from 3.9 ± 0.4 to 2.9 ± 0.3 Ma, but given that samples from higher elevations are not substantially older (Fig. 4), we consider the new contours, and thus the interpretation, to be robust. Combining our new data with published AFT cooling ages shows that the age contours south and east of Nanga Parbat region are broadly parallel to the major thrust structures around the syntaxis. It appears that the contours west of the syntaxis likely make a sharp bend southward at the MBT. Generally, the exhumation through the apatite partial annealing zone temperatures appear to be governed by movement on the major thrust zones (MBT, MCT; Fig. 9) with the youngest ages being located near the MCT and MBT. The extent to which the tectonic aneurysm model of Zeitler et al. (2001a, 2001b) can be applied appears to be spatially limited. The distribution of higher temperature cooling ages and the occurrence of low-pressure granulites clearly document the unusual exhumation at Nanga Parbat (Koons et al., 2013), but this region may be small and cannot be extended to the regions of the Neelum valley and further south.

Figure 9.

Map showing previously published apatite fission track ages (in Ma) plus those derived for this study (yellow dots). Following the logic of Zeitler (1985) we have selected from our own data only base-level samples from the lowest points of the topography along the Neelum River. As such, they are comparable to the data of Zeitler (1985), allowing a reinterpretation of the contours from Figure 1C. MKT—Main Karakoram thrust; MMT—Main Mantle thrust; MCT—Main Central thrust; MBT—Main Boundary thrust; STDZ—South Tibet detachment zone.

Figure 9.

Map showing previously published apatite fission track ages (in Ma) plus those derived for this study (yellow dots). Following the logic of Zeitler (1985) we have selected from our own data only base-level samples from the lowest points of the topography along the Neelum River. As such, they are comparable to the data of Zeitler (1985), allowing a reinterpretation of the contours from Figure 1C. MKT—Main Karakoram thrust; MMT—Main Mantle thrust; MCT—Main Central thrust; MBT—Main Boundary thrust; STDZ—South Tibet detachment zone.

The fact that the AFT cooling age contours for all ages older than ca. 2 Ma are parallel to the major thrusts in the western syntaxis supports an exhumation model that advocates tectonics as the principal driving mechanism for at least the last stages of exhumation (Fig. 9). This is also supported by the slight trend in AFT ages from our low-altitude samples that increase up river, along with the ranges of AFT ages from the two profiles, Kel and Leswa. The Leswa profile is close to the main faults in the downstream parts of Neelum River and has the youngest AFT ages, whereas the Kel profile, which is further from the regional faults, shows somewhat older AFT ages (Table 2; Fig. 3). However, the final stage of exhumation is only related to the incision of the Neelum River catchment into a plateau formed ca. 10 Ma due to activity along the MBT (Fig. 8). This interpretation is supported by stream power analysis (Fig. 6), although the signal from the AHe ages is not clear. Nevertheless, it is consistent with the interpretation of van der Beek et al. (2009), who argued that the Deosai Plateau in the northeastern part of the region is a remnant of the Tibetan Plateau. As such, our interpretation may be of tectonic importance to a much larger region than investigated here.

CONCLUSIONS

The results from a multiple thermochronometric dating and thermal modeling approach combined with geomorphic stream power analysis allow us to conclude the following.

Apatite U-Pb data constrain the position of the MCT in the Neelum valley region, which has been the subject of controversy. Samples with Proterozoic U-Pb ages all are part of the Leswa profile. The boundary between the samples unaffected by Himalayan tectonics and all other samples is interpreted to represent the trace of MCT along the Leswa profile.

Average ZHe, AFT, and average AHe ages are generally 16–9 Ma, 7–3 Ma, and 6–3 Ma, respectively (Fig. 4). The ages from the two apatite low-temperature thermochronology systems are largely indistinguishable for both profiles, indicating exhumation rates of 1 mm/yr to 0.3 mm/yr, with only a short residence time in the apatite partial annealing zone and AHe partial retention zone.

Thermal history modeling of our data is consistent with thrusting on the MBT ca. 10 Ma in both the Kel and Leswa profiles (Fig. 7). The MCT is also suggested to have been inactive since the early-middle Miocene, as samples across the MCT trace show the same thermal history for the last 11–10 m.y., even when modeled as separate groups of hanging-wall and footwall samples.

The Neelum River is characterized by a steepness index of ksn > 500 m0.9, but both the lowest reaches (where it joins the Jhelum River) as well as the headwaters of the catchment have significantly lower steepness indices, ksn = ∼20–500 m0.9. We interpret this as evidence for strong geomorphic disequilibrium caused by recent motion on the MBT and/or MCT and continuous catchment capture in the headwaters. Knickpoints have been identified along the channel profiles of the Kunhar and Neelum Rivers at a distance of ∼90 and ∼110 km, respectively, upstream of their junction with Jhelum River (Fig. 6). This indicates a wave of erosion propagating upstream that may have started as a result of base-level fall at 5–3 Ma due to the formation of Kashmir Basin and resultant drainage convergence into Jhelum River.

In combination with AFT ages from the literature, our data define AFT cooling age contours around the entire western syntaxis region. The contours do not close in the south of Nanga Parbat, but extend toward the southeast, trending parallel to regional-scale thrust faults (Fig. 9). The distribution of exhumation around the syntaxis thus follows the well-established pattern known from much of the Himalayan front, rather than representing an isolated region of extreme exhumation.

ACKNOWLEDGMENTS

This work was supported by the Higher Education Commission (HEC) of Pakistan and Austrian Agency for International Cooperation in Education and Research (OeAD-GmbH) at different levels. Partial support for field work was provided by the Heinrich-Jörg Stiftung funding scheme of the University of Graz, Austria. We thank Luigia Di Nicola, Mahmoud Hassan, Gustav Hanke, Tamer Abu-Alam, Jamil Hassan, Daniel Döpke, and Katarzyna Luszczak for providing help at various stages. David Wallis, Peter van der Beek, and four anonymous reviewers helped to improve earlier versions of this manuscript. We thank Damian Nance for his editorial handling of the manuscript.

1GSA Data Repository Item 2017319, which includes details about the Standard lab procedures followed during the thermochronologic analysis, apatite U-Pb ages of all of the samples as Tera-Wasserburg Concordia diagrams (Fig. S1), and thermal history modeling results as predicted vs observed ages of two profiles (Fig. S2), is available at http://www.geosociety.org/datarepository/2017, or on request from editing@geosociety.org.

REFERENCES CITED

Alam
,
A.
,
Ahmad
,
S.
,
Bhat
,
M.S.
, and
Ahmad
,
B.
,
2015
,
Tectonic evolution of Kashmir basin in northwest Himalayas
:
Geomorphology
 , v.
239
, p.
114
126
, doi:10.1016/j.geomorph.2015.03.025.
Bollinger
,
L.
,
Avouac
,
J.P.
,
Beyssac
,
O.
,
Catlos
,
E.J.
,
Harrison
,
T.M.
,
Grove
,
M.
,
Goffe
,
B.
, and
Sapkota
,
S.
,
2004
,
Thermal structure and exhumation history of the Lesser Himalaya in central Nepal
:
Tectonics
 , v.
23
,
TC5015
, doi:10.1029/2003TC001564.
Bollinger
,
L.
,
Henry
,
P.
, and
Avouac
,
J.P.
,
2006
,
Mountain building in the Nepal Himalaya: Thermal and kinematic model
:
Earth and Planetary Science Letters
 , v.
244
, p.
58
71
, doi:10.1016/j.epsl.2006.01.045.
Bouilhol
,
P.
,
Jagoutz
,
O.
,
Hanchar
,
J.M.
, and
Dudas
,
F.O.
,
2013
,
Dating the India-Eurasia collision through arc magmatic records
:
Earth and Planetary Science Letters
 , v.
366
, p.
163
175
, doi:10.1016/j.epsl.2013.01.023.
Burbank
,
D.W.
, and
Johnson
,
G.D.
,
1982
,
Intermontane-basin development in the past 4 Myr in the north-west Himalaya
:
Nature
 , v.
298
, p.
432
436
, doi:10.1038/298432a0.
Burbank
,
D.W.
,
Leland
,
J.
,
Fielding
,
E.
,
Anderson
,
R.S.
,
Brozovic
,
N.
,
Reid
,
M.R.
, and
Duncan
,
C.
,
1996
,
Bedrock incision, rock uplift and threshold hillslopes in the northwestern Himalayas
:
Nature
 , v.
379
, p.
505
510
, doi:10.1038/379505a0.
Burg
,
J.-P.
,
Chaudhry
,
M.N.
,
Ghazanfar
,
M.
,
Anczkiewicz
,
R.
, and
Spencer
,
D.
,
1996
,
Structural evidence for back sliding of the Kohistan arc in the collisional system of northwest Pakistan
:
Geology
 , v.
24
, p.
739
742
, doi:10.1130/0091-7613(1996)024<0739:SEFBSO>2.3.CO;2.
Butler
,
R.W.H.
,
Prior
,
D.J.
, and
Knipe
,
R.J.
,
1989
,
Neotectonics of the Nanga Parbat Syntaxis, Pakistan, and crustal stacking in the northwest Himalayas
:
Earth and Planetary Science Letters
 , v.
94
, p.
329
343
, doi:10.1016/0012-821X(89)90150-7.
Calkins
,
J.A.
,
Offield
,
T.W.
,
Abdullah
,
S.K.M.
, and
Tayyab Ali
,
S.
,
1975
,
Geology of the Southern Himalaya in Hazara, Pakistan, and adjacent areas
:
U.S. Geological Survey Professional Paper 716C
,
29
p.
Catlos
,
E.J.
,
Harrison
,
T.M.
,
Kohn
,
M.J.
,
Grove
,
M.
,
Ryerson
,
F.J.
,
Manning
,
C.E.
, and
Upreti
,
B.N.
,
2001
,
Geochronologic and thermobarometric constraints on the evolution of the Main Central thrust, Central Nepal Himalaya
:
Journal of Geophysical Research
 , v.
106
, no.
B8
, p.
16,177
16,204
, doi:10.1029/2000JB900375.
Chamberlain
,
C.P.
,
Koon
,
P.O.
,
Meltzer
,
A.S.
,
Park
,
S.K.
,
Craw
,
D.
,
Zeitler
,
P.
, and
Poage
,
M.A.
,
2002
,
Overview of hydrothermal activity associated with active orogenesis and metamorphism: Nanga Parbat, Pakistan Himalaya
:
American Journal of Science
 , v.
302
, p.
726
748
, doi:10.2475/ajs.302.8.726.
Chamberlain
,
K.R.
, and
Bowring
,
S.A.
,
2000
,
Apatite-feldspar U-Pb thermochronometer: A reliable, mid-range (∼450 °C), diffusion-controlled system
:
Chemical Geology
 , v.
172
, p.
173
200
, doi:10.1016/S0009-2541(00)00242-4.
Craw
,
D.
,
Koons
,
P.O.
,
Winslow
,
D.
,
Chamberlain
,
C.P.
, and
Zeitler
,
P.
,
1994
,
Boiling fluids in a region of rapid uplift, Nanga Parbat Massif, Pakistan
:
Earth and Planetary Science Letters
 , v.
128
, p.
169
182
, doi:10.1016/0012-821X(94)90143-0.
Ding
,
L.
,
Qasim
,
M.
,
Jadoon
,
I.A.K.
,
Khan
,
M.A.
,
Xu
,
Q.
,
Cai
,
F.
,
Wang
,
H.
,
Baral
,
U.
, and
Yue
,
Y.
,
2016
,
The India-Asia collision in north Pakistan: Insight from the U-Pb detrital zircon provenance of Cenozoic foreland basin
:
Earth and Planetary Science Letters
 , v.
455
, p.
49
61
, doi:10.1016/j.epsl.2016.09.003.
DiPietro
,
J.A.
, and
Pogue
,
K.R.
,
2004
,
Tectonostratigraphic subdivisions of the Himalaya: A view from the west
:
Tectonics
 , v.
23
, TC5001, doi:10.1029/2003TC001554.
Dobson
,
K.J.
,
Stuart
,
F.M.
, and
Dempster
,
T.J.
,
2008
,
U and Th zonation in Fish Canyon Tuff zircons: Implications for a zircon (U-Th)/He standard
:
Geochimica et Cosmochimica Acta
 , v.
72
, p.
4745
4755
, doi:10.1016/j.gca.2008.07.015.
Donelick
,
R.A.
,
O’Sullivan
,
P.B.
, and
Ketcham
,
R.A.
,
2005
,
Apatite fission-track analysis
, in
Reiners
,
P.W.
, and
Ehlers
,
T.E.
, eds.,
Low-temperature thermochronology: Techniques, interpretations, and applications
 :
Mineralogical Society of America Reviews in Mineralogy and Geochemistry Volume 58
, p.
49
94
, doi:10.2138/rmg.2005.58.3.
Farley
,
K.A.
,
2002
,
(U-Th)/He dating: Techniques, calibrations, and applications
, in
Porcelli
,
D.
,
Ballentine
,
C.J.
, and
Wieler
,
R.
, eds.,
Noble gases in geochemistry and cosmochemistry
 :
Mineralogical Society of America Reviews in Mineralogy and Geochemistry Volume 47
, p.
819
844
, doi:10.2138/rmg.2002.47.18.
Flowers
,
R.M.
,
Ketcham
,
R.A.
,
Shuster
,
D.L.
, and
Farley
,
K.A.
,
2009
,
Apatite (U-Th)/He thermochronometry using a radiation damage accumulation and annealing model
:
Geochimica et Cosmochimica Acta
 , v.
73
, p.
2347
2365
, doi:10.1016/j.gca.2009.01.015.
Fontan
,
D.
,
Schouppe
,
M.
,
Hunziker
,
C.J.
,
Martinotti
,
G.
, and
Verkaeren
,
J.
,
2000
,
Metamorphic evolution, 40Ar-39Ar chronology and tectonic model for the Neelum valley, Azad Kashmir, NE Pakistan
, in
Khan
,
M.A.
, et al. 
., eds.,
Tectonics of the Nanga Parbat syntaxis and the Western Himalaya
 :
Geological Society
,
London
, Special Publication 170, p. 431–453, doi:10.1144/GSL.SP.2000.170.01.23.
Galbraith
,
R.F.
,
1981
,
On statistical models for fission track counts
:
Mathematical Geology
 , v.
13
, p.
471
478
, doi:10.1007/BF01034498.
Gallagher
,
K.
,
2012
,
Transdimensional inverse thermal history modeling for quantitative thermochronology
:
Journal of Geophysical Research
 , v.
117
,
B02408
, doi:10.1029/2011JB008825.
Garcia-Castellanos
,
D.
, and
Jiménez-Munt
,
I.
,
2015
,
Topographic evolution and climate aridification during continental collision: Insights from computer simulations
:
PLoS ONE
 , v.
10
, no.
8
,
e0132252
, doi:10.1371/journal.pone.0132252.
Greco
,
A.
, and
Spencer
,
D.A.
,
1993
,
A section through the Indian Plate, Kaghan Valley, NW Himalaya, Pakistan
, in
Treloar
,
P.J.
, and
Searle
,
M.P.
, eds.,
Himalayan tectonics
 :
Geological Society
,
London
, Special Publication 74, p. 221–236, doi:10.1144/GSL.SP.1993.074.01.16.
Guenthner
,
W.R.
,
Reiners
,
P.W.
,
Ketcham
,
R.A.
,
Nasdala
,
L.
, and
Giester
,
G.
,
2013
,
Helium diffusion in natural zircon: Radiation damage, anisotropy, and the interpretation of zircon (U-Th)/He thermochronology
:
American Journal of Science
 , v.
313
, p.
145
198
, doi:10.2475/03.2013.01.
Guillot
,
S.
,
Mahéo
,
G.
,
de Sigoyer
,
J.
,
Hattori
,
K.H.
, and
Pêcher
,
A.
,
2008
,
Tethyan and Indian subduction viewed from the Himalayan high- to ultrahigh-pressure metamorphic rocks
:
Tectonophysics
 , v.
451
, p.
225
241
, doi:10.1016/j.tecto.2007.11.059.
Herman
,
F.
, et al. 
.,
2010
,
Exhumation, crustal deformation, and thermal structure of the Nepal Himalaya derived from the inversion of thermochronological and thermobarometric data and modeling of the topography
:
Journal of Geophysical Research
 , v.
115
, no.
B6
,
B06407
, doi:10.1029/2008JB006126
Hodges
,
K.V.
,
Parrish
,
R.R.
,
Housh
,
T.B.
,
Lux
,
D.R.
,
Burchfield
,
B.C.
,
Royden
,
L.H.
, and
Chen
,
Z.
,
1992
,
Simultaneous Miocene extension and shortening in the Himalayan Orogen
:
Science
 , v.
258
, p.
1466
1470
, doi:10.1126/science.258.5087.1466.
Hodges
,
K.V.
,
Wobus
,
C.
,
Ruhl
,
K.
,
Schildgen
,
T.
, and
Whipple
,
K.
,
2004
,
Quaternary deformation, river steepening, and heavy precipitation at the front of the Higher Himalayan ranges
:
Earth and Planetary Science Letters
 , v.
220
, p.
379
389
, doi:10.1016/S0012-821X(04)00063-9.
Kazmi
,
A.H.
, and
Jan
,
M.Q.
,
1997
,
Geology and tectonics of Pakistan
:
Karachi
,
Graphic Publishers
,
554
p.
Ketcham
,
R.A.
,
Carter
,
A.
,
Donelick
,
R.A.
,
Barbarand
,
J.
, and
Hurford
,
A.J.
,
2007
,
Improved modeling of fission-track annealing in apatite
:
American Mineralogist
 , v.
92
, p.
799
810
, doi:10.2138/am.2007.2281.
Khan
,
M.A.
, et al. 
.,
2008
,
Preliminary geodetic constraints on plate boundary deformation on the western edge of the Indian plate from TriGGnet (Tri-University GPS Geodesy Network)
:
Journal of Himalayan Earth Sciences
 , v.
41
, p.
71
87
.
King
,
G.E.
,
Herman
,
F.
, and
Guralnik
,
B.
,
2016
,
Northward migration of the eastern Himalayan syntaxis revealed by OSL thermochronometry
:
Science
 , v.
353
, p.
800
804
, doi:10.1126/science.aaf2637.
Koons
,
P.O.
,
Zeitler
,
P.K.
,
Chamberlain
,
C.P.
,
Craw
,
D.
, and
Meltzer
,
A.S.
,
2002
,
Mechanical links between erosion and metamorphism in Nanga Parbat, Pakistan Himalaya
:
American Journal of Science
 , v.
302
, p.
749
773
, doi:10.2475/ajs.302.9.749.
Koons
,
P.O.
,
Zeitler
,
P.K.
, and
Hallet
,
B.
,
2013
,
Tectonic aneurysms and mountain building
, in
Shroder
,
J.
, and
Owen
,
L.A.
, eds.,
Treatise on geomorphology Volume 5
 :
San Diego, California
,
Academic Press
, p.
318
349
, doi:10.1016/B978-0-12-374739-6.00094-4.
Malik
,
R.H.
,
Schouppe
,
M.
,
Fontan
,
D.
,
Verkaeren
,
J.
,
Martinotti
,
G.
,
Ahmed
,
K.S.
, and
Qureshi
,
S.
,
1996
,
Geology of the Neelum valley, district Muzaffarabad, Azad Kashmir, Pakistan
:
University of Peshawar Geological Bulletin
 , v.
29
, p.
91
111
.
Meigs
,
A.J.
,
Burbank
,
D.W.
, and
Beck
,
R.A.
,
1995
,
Middle-late Miocene (>10 Ma) formation of the Main Boundary thrust in the western Himalaya
:
Geology
 , v.
23
, p.
423
426
, doi:10.1130/0091-7613(1995)023<0423:MLMMFO>2.3.CO;2.
Patriat
,
P.
, and
Achache
,
J.
,
1984
,
India-Eurasia collision chronology has implications for crustal shortening and driving mechanism of plates
:
Nature
 , v.
311
, p.
615
621
, doi:10.1038/311615a0.
Pêcher
,
A.
,
Giuliani
,
G.
,
Garnier
,
V.
,
Maluski
,
H.
,
Kausar
,
A.B.
,
Malik
,
R.H.
, and
Muntaz
,
H.R.
,
2002
,
Geology, geochemistry and Ar-Ar geochronology of the Nangimali ruby deposit, Nanga Parbat Himalaya (Azad Kashmir, Pakistan)
:
Journal of Asian Earth Sciences
 , v.
21
, p.
265
282
, doi:10.1016/S1367-9120(02)00041-X.
Pêcher
,
A.
, et al. 
.,
2008
,
Stress field evolution in the northwest Himalayan syntaxis, northern Pakistan
:
Tectonics
 , v.
27
, TC6005, doi:10.1029/2007TC002252.
Reiners
,
P.W.
,
2005
,
Zircon (U-Th)/He Thermochronometry
, in
Reiners
,
P.W.
, and
Ehlers
,
T.E.
, eds.,
Low-temperature thermochronology: Techniques, interpretations, and applications
 :
Mineralogical Society of America Reviews in Mineralogy and Geochemistry Volume 58
, p.
151
179
, doi:10.2138/rmg.2005.58.6.
Reiners
,
P.W.
, and
Brandon
,
M.T.
,
2006
,
Using thermochronology to understand orogenic erosion
:
Annual Review of Earth and Planetary Sciences
 , v.
34
, p.
419
466
, doi:10.1146/annurev.earth.34.031405.125202.
Schneider
,
D.A.
,
Zeitler
,
P.K.
,
Kidd
,
W.S.F.
, and
Edwards
,
M.A.
,
2001
,
Geochronologic constraints on the tectonic evolution and exhumation of Nanga Parbat, western Himalaya syntaxis, revisited
:
The Journal of Geology
 , v.
109
, p.
563
583
, doi:10.1086/322764.
Searle
,
M.P.
,
Law
,
R.D.
,
Godin
,
L.
,
Larson
,
K.P.
,
Streule
,
M.J.
,
Cottle
,
J.M.
, and
Jessup
,
M.J.
,
2008
,
Defining the Himalayan Main Central Thrust in Nepal
:
Journal of the Geological Society [London]
 , v.
165
, p.
523
534
, doi:10.1144/0016-76492007-081.
Seeber
,
L.
, and
Pêcher
,
A.
,
1998
,
Strain partitioning along the Himalayan arc and the Nanga Parbat antiform
:
Geology
 , v.
26
, p.
791
794
, doi:10.1130/0091-7613(1998)026<0791:SPATHA>2.3.CO;2.
Shah
,
S.M.I.
,
2009
,
Stratigraphy of Pakistan
:
Geological Survey of Pakistan Memoir 22
 ,
381
p.
Stacey
,
J.S.
, and
Kramers
,
J.D.
,
1975
,
Approximation of terrestrial lead isotope evolution by a two-stage model
:
Earth and Planetary Science Letters
 , v.
26
, p.
207
221
, doi:10.1016/0012-821X(75)90088-6.
Treloar
,
P.J.
,
Rex
,
D.C.
,
Guise
,
P.G.
,
Coward
,
M.P.
,
Searle
,
M.P.
,
Windley
,
B.F.
,
Petterson
,
M.G.
,
Jan
,
M.Q.
, and
Luff
,
I.W.
,
1989
,
K-Ar and Ar-Ar geochronology of the Himalayan collision in NW Pakistan: Constraints on the timing of suturing, deformation, metamorphism and uplift
:
Tectonics
 , v.
8
, p.
881
909
, doi:10.1029/TC008i004p00881.
Treloar
,
P.J.
,
Coward
,
M.P.
,
Chambers
,
A.F.
,
Izatt
,
C.N.
, and
Jackson
,
K.C.
,
1992
,
Thrust geometries, interferences and rotations in the Northwest Himalaya
, in
McClay
,
K.R.
, ed.,
Thrust tectonics
 :
London
,
Chapman and Hall
, p.
325
342
, doi:10.1007/978-94-011-3066-0_30.
Treloar
,
P.J.
,
Rex
,
D.C.
,
Guise
,
P.G.
,
Wheeler
,
J.
,
Hurford
,
A.J.
, and
Carter
,
A.
,
2000
,
Geochronological constraints on the evolution of the Nanga Parbat syntaxis, Pakistan Himalaya
, in
Khan
,
M.A.
, et al. 
., eds.,
Tectonics of the Nanga Parbat syntaxis and the Western Himalaya
 :
Geological Society
,
London
, Special Publication 170, p. 137–162, doi:10.1144/GSL.SP.2000.170.01.08.
van der Beek
,
P.
,
Van Melle
,
J.
,
Guillot
,
S.
,
Pêcher
,
A.
,
Reiners
,
P.W.
,
Nicolescu
,
S.
, and
Latif
,
M.
,
2009
,
Eocene Tibetan plateau remnants preserved in the northwest Himalaya
:
Nature Geoscience
 , v.
2
, p.
364
368
, doi:10.1038/ngeo503.
Vannay
,
J-C.
,
Grasemann
,
B.
,
Rahn
,
M.
,
Frank
,
W.
,
Carter
,
A.
,
Baudraz
,
V.
, and
Cosca
,
M.
,
2004
,
Miocene to Holocene exhumation of metamorphic crustal wedges in the NW Himalaya: Evidence for tectonic extrusion coupled to fluvial erosion
:
Tectonics
 , v.
23
, TC1014, doi:10.1029/2002TC001429.
Wang
,
P.
,
Scherler
,
D.
,
Liu-Zeng
,
J.
,
Mey
,
J.
,
Avouac
,
J.P.
,
Zhang
,
Y.
, and
Shi
,
D.
,
2014
,
Tectonic control of Yarlung Tsangpo Gorge revealed by a buried canyon in Southern Tibet
:
Science
 , v.
346
, p.
978
981
, doi:10.1126/science.1259041.
Whipp
,
D.M.
, Jr
,
Ehlers
,
T.A.
,
Blythe
,
A.E.
,
Huntington
,
K.W.
,
Hodges
,
K.V.
, and
Burbank
,
D.W.
,
2007
,
Plio-Quaternary exhumation history of the central Nepalese Himalaya: 2. Thermokinematic and thermochronometer age prediction model
:
Tectonics
 , v.
26
, TC3003, doi:10.1029/2006TC001991.
Whipp
,
D.M.
, Jr
,
Beaumont
,
C.
, and
Braun
,
J.
,
2014
,
Feeding the “aneurysm”: Orogen-parallel mass transport into Nanga Parbat and the western Himalayan syntaxis
:
Journal of Geophysical Research
 , v.
119
, p.
5077
5096
, doi:10.1002/2013JB010929.
Whipple
,
K.
,
Wobus
,
C.
,
Crosby
,
B.
,
Kirby
,
E.
, and
Sheehan
,
D.
,
2007
,
New tools for quantitative geomorphology: Extraction and interpretation of stream profiles from digital topographic data
:
Boulder
,
Colorado
,
26
p., (accessed October 2016).
Whittaker
,
A.C.
,
2012
,
How do landscapes record tectonics and climate?
:
Lithosphere
 , v.
4
, p.
160
164
, doi:10.1130/RF.L003.1.
Wilke
,
F.D.H.
,
Sobel
,
E.R.
,
O’Brien
,
P.J.
, and
Stockli
,
D.F.
,
2012
,
Apatite fission track and (U-Th)/He ages from the Higher Himalayan Crystallines, Kaghan Valley, Pakistan: Implications for an Eocene Plateau and Oligocene to Pliocene exhumation
:
Journal of Asian Earth Sciences
 , v.
59
, p.
14
23
, doi:10.1016/j.jseaes.2012.06.014.
Wobus
,
C.
,
Whipple
,
K.X.
,
Kirby
,
E.
,
Snyder
,
N.
,
Johnson
,
J.
,
Spyropolou
,
K.
,
Crosby
,
B.
, and
Sheehan
,
D.
,
2006
,
Tectonics from topography: Procedures, promise, and pitfalls
, in
Willet
,
S.D.
, et al. 
., eds.,
Tectonics, climate, and landscape evolution
 :
Geological Society of America Special Paper 398
, p.
55
74
, doi:10.1130/2006.2398(04).
Zeitler
,
P.K.
,
1985
,
Cooling history of the NW Himalaya, Pakistan
:
Tectonics
 , v.
4
, p.
127
151
, doi:10.1029/TC004i001p00127.
Zeitler
,
P.K.
,
Johnson
,
N.M.
,
Naeser
,
C.W.
, and
Tahirkheli
,
R.A.K.
,
1982
,
Fission-track evidence for Quaternary uplift of the Nanga Parbat region, Pakistan
:
Nature
 , v.
298
, p.
255
257
, doi:10.1038/298255a0.
Zeitler
,
P.K.
, et al. 
.,
2001a
,
Crustal reworking at Nanga Parbat, Pakistan: Metamorphic consequences of thermal-mechanical coupling facilitated by erosion
:
Tectonics
 , v.
20
, p.
712
728
, doi:10.1029/2000TC001243.
Zeitler
,
P.K.
, et al. 
.,
2001b
,
Erosion, Himalayan geodynamics, and the geomorphology of metamorphism
:
GSA Today
 , v.
11
, no.
1
, p.
4
9
, doi:10.1130/1052-5173(2001)011<0004:EHGATG>2.0.CO;2.