Megathrust splay fault systems in accretionary prisms have been identified as conduits for long-term plate motion and significant coseismic slip during subduction earthquakes. These fault systems are important because of their role in generating tsunamis, but rarely are emergent above sea level where their long-term (million year) history can be studied. We present 32 apatite (U-Th)/He (AHe) and 27 apatite fission-track (AFT) ages from rocks along an emergent megathrust splay fault system in the Prince William Sound region of Alaska above the shallowly subducting Yakutat microplate. The data show focused exhumation along the Patton Bay megathrust splay fault system since 3–2 Ma. Most AHe ages are younger than 5 Ma; some are as young as 1.1 Ma. AHe ages are youngest at the southwest end of Montague Island, where maximum fault displacement occurred on the Hanning Bay and Patton Bay faults and the highest shoreline uplift occurred during the 1964 earthquake. AFT ages range from ca. 20 to 5 Ma. Age changes across the Montague Strait fault, north of Montague Island, suggest that this fault may be a major structural boundary that acts as backstop to deformation and may be the westward mechanical continuation of the Bagley fault system backstop in the Saint Elias orogen. The regional pattern of ages and corresponding cooling and exhumation rates indicate that the Montague and Hinchinbrook Island splay faults, though separated by only a few kilometers, accommodate kilometer-scale exhumation above a shallowly subducting plate at million year time scales. This long-term pattern of exhumation also reflects short-term seismogenic uplift patterns formed during the 1964 earthquake. The increase in rock uplift and exhumation rate ca. 3–2 Ma is coincident with increased glacial erosion that, in combination with the fault-bounded, narrow width of the islands, has limited topographic development. Increased exhumation starting ca. 3–2 Ma is interpreted to be due to rock uplift caused by increased underplating of sediments derived from the Saint Elias orogen, which was being rapidly eroded at that time.

Flat-slab subduction and collision of the Yakutat microplate have had a profound effect on southern Alaskan geology for the past ∼24 m.y. (e.g., Haeussler, 2008). Deformation from this interaction has penetrated as far as ∼900 km inland, from the Brooks Range in the north (O’Sullivan et al., 1997a, 1997b) to the Saint Elias Mountains in the southeast. Flat-slab subduction of the Yakutat microplate has resulted in slip and deformation along several fault systems throughout the region (Fig. 1), including faults that splay off the subduction megathrust (e.g., Plafker, 1967; Bruhn et al., 2004; Haeussler et al., 2011; Liberty et al., 2013). Megathrust splay faults elsewhere in the world develop in accretionary prisms at outer ridges that flank the deformation front in subduction settings (e.g., Kame et al., 2003; Ikari et al., 2009). Some megathrust splay faults have been identified as conduits for long-term plate motion and significant coseismic slip during subduction earthquakes (Park et al., 2002; Kame et al., 2003, Moore et al., 2007; Ikari et al., 2009). These megathrust splay faults can be a source of tsunami generation during large megathrust ruptures, because they are typically located offshore in deep water.

Figure 1.

Regional 300 m digital elevation model base map of southern Alaska (modified from the U.S. Geological Survey data repository, http://ned.usgs.gov). Prince William Sound study area is outlined by yellow box and shows the area of Figure 2. Major faults are after Plafker et al. (1994) and the U.S. Geological Survey data repository (http://ned.usgs.gov). Plate motion vectors (white arrows) are from Plattner et al. (2007) and Elliott et al. (2010). Interpreted region of the subducted Yakutat microplate (green boundary) and subaerial region of Yakutat microplate (green shaded portion of plate) are from Fletcher and Freymueller (2003), Eberhart-Phillips et al. (2006), and Fuis et al. (2008). CM—Chugach Mountains; KM—Kenai Mountains; SEM—Saint Elias Mountains; PZ—Pamplona fold-thrust zone; KIZ—Kayak Island zone; MG—Malaspina Glacier; BG—Bering Glacier; BF—Bagley fault; CSEF—Chugach–Saint Elias fault; MI—Montague Island; HI—Hinchinbrook Island; MSF—Montague Strait fault; MDI—Middleton Island. Modified from Arkle et al. (2013).

Figure 1.

Regional 300 m digital elevation model base map of southern Alaska (modified from the U.S. Geological Survey data repository, http://ned.usgs.gov). Prince William Sound study area is outlined by yellow box and shows the area of Figure 2. Major faults are after Plafker et al. (1994) and the U.S. Geological Survey data repository (http://ned.usgs.gov). Plate motion vectors (white arrows) are from Plattner et al. (2007) and Elliott et al. (2010). Interpreted region of the subducted Yakutat microplate (green boundary) and subaerial region of Yakutat microplate (green shaded portion of plate) are from Fletcher and Freymueller (2003), Eberhart-Phillips et al. (2006), and Fuis et al. (2008). CM—Chugach Mountains; KM—Kenai Mountains; SEM—Saint Elias Mountains; PZ—Pamplona fold-thrust zone; KIZ—Kayak Island zone; MG—Malaspina Glacier; BG—Bering Glacier; BF—Bagley fault; CSEF—Chugach–Saint Elias fault; MI—Montague Island; HI—Hinchinbrook Island; MSF—Montague Strait fault; MDI—Middleton Island. Modified from Arkle et al. (2013).

Thermochronometers allow us to place million-year time-scale constraints on the exhumation history of an area and to gain insight into structural systems, such as megathrust splay faults, as they accommodate the vertical transport of rock. Numerous studies using low-temperature thermochronology have focused on exhumational patterns across major fault systems associated with flat-slab subduction in southern Alaska, including studies in the Alaska Range (e.g., Fitzgerald et al., 1995; Haeussler et al., 2008, 2011; Benowitz et al., 2011, 2012, 2013), Chugach Mountains (Little and Naeser, 1989; Buscher et al., 2008; Arkle et al., 2013), and Saint Elias Mountains (e.g., Berger et al., 2008a, 2008b; Berger and Spotila, 2008; Meigs et al., 2008; Enkelmann et al., 2008, 2009; Spotila and Berger, 2010). Some of these studies detected loci of rapid exhumation, particularly in the Saint Elias and western Chugach Mountains, which may be the result of crustal-scale lithologic backstops to upper crustal rock deformation above the subducting Yakutat microplate.

This study targets the southern Prince William Sound region (Fig. 1), located on the overriding North American plate closest to the Aleutian Trench and ∼20 km above the megathrust décollement. Seismic imaging and thermal-mechanical models show that there is a large degree of coupling and/or underplating between the subducting Yakutat microplate and the overriding North American plate (Brocher et al., 1991; Ratchkovski and Hansen, 2002; Zweck et al., 2002; Ferris et al., 2003; Eberhart-Phillips et al., 2006; Fuis et al., 2008) below Prince William Sound, making this area susceptible to large (moment magnitude, Mw > 8.0) earthquakes like the 1964 Mw 9.2 Alaska earthquake (Plafker, 1965). Evidence that this region is actively accommodating deformation is shown by the tectonic analysis of ground breakage and surface warping during the 1964 earthquake on Montague and Hinchinbrook Islands (Plafker, 1967) in southern Prince William Sound. This study expands on Plafker’s (1967) original geologic analyses by using apatite (U-Th)/He (AHe) and fission-track (AFT) thermochronology in order to quantify long-term rock uplift and exhumation patterns across southern Prince William Sound. We target Hinchinbrook and Montague Islands (Figs. 1 and 2), which are the largest and most trenchward islands in Prince William Sound.

Figure 2.

Sample map with apatite (U-Th)/He (AHe), apatite fission-track (AFT), and zircon fission-track (ZFT) cooling ages. Base map (300 m digital elevation model) is modified from Arkle et al. (2013). Faults (solid lines), inferred faults (dashed lines), and overlain major lithologic units are from Plafker et al. (1989) and the U.S. Geological Survey fault data repository (http://ned.usgs.gov). The Patton Bay and Hanning Bay faults are highlighted in red. Transect lines are located for Figures 5 and 6. MI—Montague Island; HI—Hinchinbrook Island; HKI—Hawkins Island; LI—Latouche Island; KNI—Knight Island; NI—Naked Islands; GI—Green Island; SI—Smith Islands; PE—Port Etches; ZB—Zaikof Bay; RB—Rocky Bay; PB—Patton Bay; JC—Jeanie Cove.

Figure 2.

Sample map with apatite (U-Th)/He (AHe), apatite fission-track (AFT), and zircon fission-track (ZFT) cooling ages. Base map (300 m digital elevation model) is modified from Arkle et al. (2013). Faults (solid lines), inferred faults (dashed lines), and overlain major lithologic units are from Plafker et al. (1989) and the U.S. Geological Survey fault data repository (http://ned.usgs.gov). The Patton Bay and Hanning Bay faults are highlighted in red. Transect lines are located for Figures 5 and 6. MI—Montague Island; HI—Hinchinbrook Island; HKI—Hawkins Island; LI—Latouche Island; KNI—Knight Island; NI—Naked Islands; GI—Green Island; SI—Smith Islands; PE—Port Etches; ZB—Zaikof Bay; RB—Rocky Bay; PB—Patton Bay; JC—Jeanie Cove.

Cretaceous–Cenozoic History of Southern Alaska

The rocks along the southern Alaska margin in Prince William Sound are part of a vast accretionary complex that has developed since the early Mesozoic (e.g., Plafker et al., 1994; Bradley et al., 2003). The Yakutat terrane is the youngest in the terrane sequence and is composed mostly of a 15–30-km-thick oceanic plateau (e.g., Christeson et al., 2010; Worthington et al., 2012). Arrival of thickened Yakutat crust at the convergent boundary is inferred to have begun ca. 12–10 Ma (Plafker, 1987; Plafker et al., 1994; Zellers, 1995; Ferris et al., 2003; Eberhart-Phillips et al., 2006; Enkelmann et al., 2008, 2009) and as early as ca. 30–18 Ma (Plafker et al., 1994b; Enkelmann et al., 2008; Haeussler, 2008; Finzel et al., 2011; Benowitz et al., 2011, 2012; Arkle et al., 2013). As the collision of this relatively buoyant material progressed, a fold-thrust belt developed, leading to high topography in the eastern Chugach–Saint Elias Mountains, and a marked transition between shallow subduction beneath the Prince William Sound and relatively steeper subduction of dense oceanic Pacific plate to the southwest (Fig. 1). Sediment shed from the growing orogen also became incorporated into and deformed within the fold-thrust belt (e.g., Plafker, 1987; Meigs et al., 2008; Pavlis et al., 2012).

The accretionary complex rocks in central and southern Prince William Sound consist of the late Paleocene to Eocene Orca Group. This is a flysch deposit consisting dominantly of slate and graywacke turbidites, but it also contains interbedded conglomerate, volcanic-lithic and/or pelagic sandstone, and mudstone (Nelson et al., 1985). The Orca Group extends laterally for more than 100 km and has a structural thickness of 18–20 km (Brocher et al., 1991; Plafker and Berg, 1994; Fuis et al., 2008). It was intruded by two episodes of small granitic plutons that are between ca. 56–53 Ma (the Sanak-Baranof belt) and ca. 40–37 Ma (the Eshamy suite) (Hudson et al., 1979; Plafker and Berg, 1994; Haeussler et al., 1995; Davidson et al., 2011; Garver et al., 2012, 2013; Carlson, 2012; Johnson, 2012). Intrusions were likely formed from near-trench processes related to a slab window, which may be associated with the subduction of the Kula-Farallon-Resurrection spreading center and possibly another smaller ridge (Bradley et al., 2003; Haeussler et al., 2003; Cowan, 2003; Cole et al., 2006; Madsen et al., 2006). Based on the timing of intrusion of these plutons and detrital zircon fission-track and U-Pb ages, the depositional age for the Orca Group is ca. 35 Ma in southeasternmost Prince William Sound, ca. 40–37 Ma near Latouche and Evans Islands, and ca. 60–57 Ma in central Prince William Sound (Garver et al., 2012; Davidson et al., 2011) (Fig. 2). Rocks of the Orca Group young to the southeast, toward the convergent margin.

Regional Structures of Prince William Sound

Our study area in Prince William Sound is bound to the north by the Chugach Mountains and to the south by Hinchinbrook and Montague Islands (Fig. 1). The arcuate Contact fault strikes approximately east-west in north-central Prince William Sound and bends southward in the Chugach Mountains to form the western Chugach syntaxis, a major structural boundary to this study area. In its southern exposures the Contact fault strikes southwest and generally separates Prince William Sound from the Kenai Peninsula (Fig. 1). The Contact fault is dominantly a right-lateral strike-slip fault to the east (Bol and Roeske, 1993), but displays reverse-fault dip-slip displacement to the west in the Chugach Mountains and Prince William Sound (Bol and Gibbons, 1992). Farther toward the trench an array of faults extends southwest from the Cordova area (Fig. 2) to form the faults of Montague and Hinchinbrook Islands (Nelson et al., 1985), all of which strike northeast-southwest and dip northwest. These are the most outboard faults exposed in Prince William Sound (Fig. 2). Between these faults and the Contact fault is the Montague Strait fault, which is a high-angle normal fault that dips southeast, though the deep structural configuration of the fault is uncertain (Haeussler et al., 2014; Liberty et al., 2013). Liberty et al. (2013) interpreted the Montague Strait fault as a major structure that separates metamorphosed Orca Group rocks to the northwest from unmetamorphosed Orca Group rocks to the south (Liberty and Finn, 2010; Haeussler et al., 2014; Garver et al., 2012). It was previously recognized as a structural discontinuity (Nelson et al., 1985), but the nature of the fault was unknown. Subsequent National Oceanic and Atmospheric Administration multibeam surveys collected from 1988 to 2003 reveal a seafloor fault scarp (Liberty and Finn, 2010; Haeussler et al., 2014). New seismic reflection profiles show that the Montague Strait fault locally had southeast-side-down normal slip during the Holocene (Liberty and Finn, 2010; Haeussler et al., 2014; Liberty et al., 2013).

Hinchinbrook and Montague Islands

Hinchinbrook and Montague Islands are elongate, narrow islands with steep coastlines and numerous reverse faults that strike parallel to the trend of the islands (Plafker, 1967) (Fig. 2). Average peak elevations on Hinchinbrook and Montague Islands are consistently ∼800 m; the highest peaks are nearly 1000 m. Bedding is highly deformed and ranges from shallowly dipping to vertical and is overturned in some places (Nelson et al., 1985; Plafker, 1967). In low-lying areas, unconsolidated Quaternary glacial till with variable thicknesses is present.

There are two main reverse faults on southern Montague Island, the Patton Bay and Hanning Bay faults, both of which ruptured during the 1964 earthquake (Plafker, 1967). After the earthquake, the faults were traceable on land by large (6–9 m) fault scarps, landslides, and uplifted coastal platforms (Plafker, 1967). These faults generally strike northeast, or parallel to the long axis of the island, and dip ∼60° northwest on average (Plafker, 1967) (Fig. 2). The Patton Bay fault can be traced on land for 35 km along the southeast coast and continues southwest on the seafloor, perhaps as far south as Kodiak Island (Plafker, 1965; Liberty et al., 2013). Seismic reflection profiles and bathymetry show the Patton Bay fault continuing offshore to the southwest for ∼20 km (Plafker, 1967; Malloy and Merrill, 1972), where vertical displacements of ∼15 m associated with the 1964 earthquake are mapped along seafloor escarpments (Malloy and Merrill, 1972; Liberty and Finn, 2010; Liberty et al., 2013). To the north, the Patton Bay fault may continue offshore along the coast to near the northeast end of the island, where its trace is lost and the fault is likely broken into multiple strands (Fig. 2). The northern coastal extent of the Patton Bay fault is suggested by the straight nature of the coastline and numerous triangular facets that line the coast along northeastern Montague Island. However, there is little evidence of active faulting at the northern extent of the Patton Bay fault. Mountain-front sinuosity is nearly 1.0 and average slopes are steeper on the east coast (18°–22°) versus the west coast (10°–12°) (measurements from this study). Motion on the fault at its southern extent was dominantly dip slip with a maximum of 9 m of vertical offset on land during the 1964 earthquake, although there was a small component (∼0.5 m) of left-lateral motion (Plafker, 1967).

The Hanning Bay fault, which cuts across a small portion of the southwest coast of Montague Island at Fault Cove (Fig. 2), extends for ∼6 km on land with the same structural orientation as the Patton Bay fault. The well-defined 1964 scarp at Fault Cove has a vertical offset of 6 m (Plafker, 1967). Across both the Hanning Bay and Patton Bay faults, the northwest blocks were upthrown relative to the southeast blocks during the 1964 earthquake. The block southeast of the Patton Bay fault was upthrown ∼4.7 m relative to sea level, the block northwest of the Patton Bay fault was upthrown ∼12 m, and the block northwest of the Hanning Bay fault was upthrown ∼5 m (Plafker, 1967).

Liberty et al. (2013) showed the presence of an additional splay fault, the Cape Cleare fault, offshore and southwest of Montague Island. Bathymetry shows a 40 m fault scarp, and subsequent marine terrace ∼5 km south of the Patton Bay fault that decreases in height to the southwest and forms the hanging-wall block of the Cape Cleare fault. This fault is traced onshore south and east of the Patton Bay fault (Fig. 2).

Other geophysical evidence from Trans-Alaska Crustal Transect (TACT) studies (e.g., Fuis et al., 2008) shows that faults in the inlet between Hinchinbrook and Montague Islands near Zaikof Bay become listric and are connected at their base to the subduction décollement to the northwest. These faults are along strike with those on Hinchinbrook and Montague Islands, possibly indicating that the faults on Hinchinbrook and Montague Islands are also rooted at depth (Liberty et al., 2013; Haeussler et al., 2014). Land surfaces at Montague Island, along the footwall block of the Cape Cleare fault offshore, and at Middleton Island ∼100 km southeast toward the Aleutian megathrust (Fig. 1), were all uplifted during the 1964 earthquake, suggesting that these faults are likely rooted downward and are separately linked to the décollement at depth (Plafker, 1967; Malloy and Merrill, 1972; Haeussler et al., 2014).

An extensive data set of low-temperature thermochronometer ages generated over the past 25 years provides insights into the timing, rates, and regional exhumation patterns, and provides constraints on regions of localized rapid exhumation during the Neogene along the southern Alaska margin (e.g., O’Sullivan et al., 1997a, 1997b; Meigs et al., 2008; Berger et al., 2008a, 2008b; Armstrong et al., 2008; Buscher et al., 2008; Enkelmann et al., 2008, 2009; Spotila and Berger, 2010; Arkle et al., 2013).

In the Saint Elias region, exhumation rates in the past ∼6 m.y. are between ∼0.5 and 4 mm/yr and vary based on structural position relative to major fault systems (Berger et al., 2008a, 2008b; Berger and Spotila, 2008; Meigs et al., 2008; Enkelmann et al., 2008, 2009; Spotila and Berger, 2010; Falkowski et al., 2014). Low-temperature cooling ages are generally very young (AHe younger than 1.5 Ma) along the coast and abruptly increase north of the Bagley fault, suggesting that the Bagley fault is acting as a deformational backstop to thin-skinned folding and thrusting at the collision front (Berger et al., 2008b; Berger and Spotila, 2008; Enkelmann et al., 2008, 2009; Headley et al., 2013; Pavlis, 2013) (Fig. 1). South of the Bagley fault, young AHe ages are attributed to their position within the active fold-thrust belt coupled with extensive erosion at the coastal front due to its windward position and heavy glaciation (Spotila and Berger, 2010). This zone of focused exhumation is projected west along the Bagley-Contact backstop toward the Miles Glacier region, or Miles Corner (previously referred to as the Western or Katalla syntaxis; e.g., Chapman et al., 2011), where it curves southwest to eventually connect with the Ragged Island thrust, Kayak Island zone, and the Alaska-Aleutian megathrust (Spotila and Berger, 2010) (Fig. 1). While the Miles Corner region may represent an immature indentor corner, there have been insufficient age constraints across the Copper River delta and into Prince William Sound to show whether this zone of rapid exhumation continues west (Fig. 1).

In the western Chugach Mountains and northern Prince William Sound (Fig. 1), a bullseye of relatively rapid exhumation was identified in a syntaxial bend between the Border Ranges and Contact faults (Arkle et al., 2013). AHe and AFT ages decrease northward across the Contact fault to minimum ages (averaging ca. 5 and 10 Ma, respectively) in the core of the Chugach Mountains between the Contact and Border Ranges faults. Zircon fission-track (ZFT) ages follow a similar pattern, but with older and more scattered ages, ranging between ca. 50 and 26 Ma (transect D–D′; Figs. 1 and 3) (Little and Naeser, 1989; Arkle et al., 2013). Between the Montague Strait and Contact faults, ages for all thermochronologic systems generally decrease by 50% relative to north of the Contact fault (Fig. 3). This pattern of relatively young ages and rapid exhumation north of the Contact fault is interpreted to be the result of underplating along the décollement that has been focused by a syntaxial geometry and modulated by glacial erosion at the southward flank of the core (Arkle et al., 2013).

Figure 3.

Plot of thermochronometer ages along a southeast-northwest transect (D–D′) shown in Figure 1. Ages are projected onto the transect profile from a 100 km swath. Age uncertainties are ±1σ. Samples are shown relative to faults (vertical dashed lines). Shaded regions mark approximate bounds of maximum and minimum ages for the apatite (U-Th)/He (AHe), apatite fission-track (AFT), and zircon fission-track (ZFT) systems. Direction of Yakutat convergence is from right to left. The ZFT ages in the Chugach Mountain region are the average of the two youngest ZFT age peaks from modern glacial deposits (Arkle et al., 2013). Figure modified from Arkle et al. (2013).

Figure 3.

Plot of thermochronometer ages along a southeast-northwest transect (D–D′) shown in Figure 1. Ages are projected onto the transect profile from a 100 km swath. Age uncertainties are ±1σ. Samples are shown relative to faults (vertical dashed lines). Shaded regions mark approximate bounds of maximum and minimum ages for the apatite (U-Th)/He (AHe), apatite fission-track (AFT), and zircon fission-track (ZFT) systems. Direction of Yakutat convergence is from right to left. The ZFT ages in the Chugach Mountain region are the average of the two youngest ZFT age peaks from modern glacial deposits (Arkle et al., 2013). Figure modified from Arkle et al. (2013).

The data set from this study helps to constrain the nature of deformation west of the transition from the eastern Chugach–Saint Elias Mountains and across the Copper River delta into Prince William Sound. It also provides constraints on deformation mechanisms above the subduction megathrust, but outboard of the exhumation bullseye and syntaxial bend in the western Chugach Mountains.

This study utilizes AHe and AFT thermochronometers to track thermal histories up to effective closure temperatures of ∼130 °C. For the AHe system, the partial retention zone (PRZ) is between ∼40 °C and 70 °C (depending on the cooling rate, grain size, and effective uranium concentration), which corresponds with depths of ∼2–3 km at typical geothermal gradients and surface temperatures (Farley, 2000; Farley and Stockli, 2002; Ehlers and Farley, 2003; Reiners et al., 2004; Flowers et al., 2009). For the AFT system, tracks anneal at temperatures between 60 °C and 130 °C (e.g., Wagner and Reimer, 1972; Naeser, 1979; Gleadow et al., 1986; Dumitru, 2000; Donelick et al., 2005), which corresponds to depths of ∼3–6 km (depending on annealing kinetics and geothermal gradient). We also utilize ZFT data from other studies (Carlson, 2012; Garver et al., 2012) that track the thermal histories of rock up to ∼240 °C (e.g., Reiners and Brandon, 2006).

Sampling Strategy and Analytical Techniques

Samples of Orca Group sandstone (n = 32) were collected in southeastern Prince William Sound and used for AHe and AFT analysis (Fig. 2; Table 1). Samples were collected both along and across the structural grain of Hinchinbrook and Montague Islands and especially adjacent to known faults and along the length of topography from southern Montague Island to north of Cordova. At least 5 kg of unweathered sandstone was collected in order to ensure sufficient apatite yield. Most samples were medium- to coarse-grained sandstone with well-sorted angular to subangular clasts, composed of quartz, feldspar, lithic fragments, and minor biotite.

TABLE 1.

SUMMARY OF THERMOCHRONOLOGY DATA

AHe ages were determined for 32 samples by laser and inductively coupled plasma–mass spectrometry methods at the California Institute of Technology (Pasadena). We used 141 single apatite grains with 4–7 single grain replicates per sample for AHe analysis. Of these grains, 13 (9%) were removed from the average age calculations because they yielded outlier ages that were high (greater than a 2σ variance) relative to the other grains in the samples (Table SF1 in the Supplemental File1). Anomalously high ages are probably due to high U-bearing inclusions undetected within the crystal. To evaluate the effects of radiation damage, effective uranium concentration was compared with each single-grain age (e.g., Flowers et al., 2009), but no relationship was apparent (Fig. SF1 in the Supplemental File [see footnote 1]). An Ft (alpha ejection) correction was applied to all raw ages to account for alpha ejection effects related to the grain size and shape (Farley et al., 1996; Farley, 2002). After outlier ages were culled, a weighted average AHe age was determined for the 32 samples using the 4–7 same-sample replicates remaining and a 1σ confidence interval (see the Supplemental File [footnote 1] for details regarding weighted age calculations).

AFT ages were determined for 27 samples using the external detector method (e.g., Gleadow and Duddy, 1981) and ages were computed using Trackkey version 4.2 (Dunkl, 2002). Analytic data are reported in Table SF2 in the Supplemental File (see footnote 1). Fission tracks were counted in 35–40 grains in most samples; as few as 15 grains were counted in some samples with low apatite yield or poor polishing. The etch pit width (Dpar) varies from 0.93 to 1.75 µm and the average for all samples is 1.48 ± 0.29 µm. No systematic relationship was found between Dpar and AFT single-grain age, indicating that age variation between samples is not caused by varying kinetic properties (Table SF2 in the Supplemental File [see footnote 1]). Almost all have narrow single-grain age distributions and pass the P(χ2) (>5%) test, indicating that the grains either spent little time in the partial annealing zone and/or are kinetically invariable.

Horizontal confined track length measurements were made for three samples (Table 1). Horizontal confined tracks were generally difficult to find within grains due to low spontaneous track densities, despite undergoing Cf-252 irradiation. In 2 samples, an average of 16 measurable tracks was counted, and in 1 sample, 108 horizontal-confined tracks were counted. The range in average track lengths is 13.0–13.8 µm.

AHe Ages

New AHe ages range from 11.2 to 1.1 Ma (Table 1; Table SF1 in the Supplemental File [see footnote 1]). In samples collected across the topographic grain on Hinchinbrook and Montague Islands, young ages are found both at sea level and at high elevations, indicating no apparent age-elevation relationship. Samples north of the Montague Strait fault have AHe ages of 7.2 ± 1.4 and 11.2 ± 1.9 Ma (Figs. 2 and 4; Table 1) and are consistent with previous AHe ages in central Prince William Sound (Arkle et al., 2013) that average 12.5 Ma. Just south of the Montague Strait fault, three ages on Smith Islands and Green Island are between 6.9 and 4.7 Ma (Fig. 2). The youngest ages are on southern Montague Island and range from 6.3 to 1.1 Ma, with an average age of 2.9 Ma. On northern Montague Island, five samples have ages between 4.5 and 3.0 Ma, with an average of 3.9 Ma. On Hinchinbrook Island, 10 AHe ages range from 8.4 to 3.6 Ma, with an average age of 5.4 Ma (Fig. 2). Farther northeast, three ages are between 4.9 and 4.1 Ma on Hawkins Island and just north of Cordova (Fig. 2). All AHe ages are younger than the sample depositional age of ca. 35 Ma (Garver et al., 2012; Carlson, 2012), and are reset.

Figure 4.

Map of contoured apatite (U-Th)/He (AHe) ages. Contour interval is 2 m.y. HBF—Hanning Bay fault; PBF—Patton Bay fault; CCF—Cape Cleare fault; RRF—Rude River fault; MI—Montague Island; HI—Hinchinbrook Island; HKI—Hawkins Island; LI—Latouche Island; KNI—Knight Island; SI—Smith Islands; NI—Naked Islands; GI—Green Island.

Figure 4.

Map of contoured apatite (U-Th)/He (AHe) ages. Contour interval is 2 m.y. HBF—Hanning Bay fault; PBF—Patton Bay fault; CCF—Cape Cleare fault; RRF—Rude River fault; MI—Montague Island; HI—Hinchinbrook Island; HKI—Hawkins Island; LI—Latouche Island; KNI—Knight Island; SI—Smith Islands; NI—Naked Islands; GI—Green Island.

AFT Ages

AFT ages range from 21.5 to 4.4 Ma across southern Prince William Sound (Table 1; Table SF2 in the Supplemental File [see footnote 1]). AFT ages north of the Montague Strait fault are 16.6 ± 1.8 and 21.5 ± 2.1 Ma (Fig. 2; Table 1), and are consistent with the 37.4–10.0 Ma AFT ages of Kveton (1989) and Arkle et al. (2013) between the Contact and Montague Strait faults (Fig. 4). Three samples just south of the Montague Strait fault have AFT ages between 17.8 and 11.2 Ma. Those on southern Montague Island are, on average, 8.9 Ma and range from 18.7 to 4.4 Ma. On northern Montague Island, AFT ages range from 11.4 to 6.3 Ma and average 9.1 Ma. On Hinchinbrook Island the average AFT age is 10.6 Ma, and ranges from 13.9 to 7.5 Ma (Fig. 2). Two samples north of Cordova have AFT ages of 9.4 and 10.3 Ma. Like their corresponding AHe ages, all of the AFT ages are younger than the ca. 35 Ma depositional ages and have been reset.

Local Analysis of Thermochronometer Ages and Relationships to Faults

Our new data show that AHe and AFT ages south of the Montague Strait fault are younger than those from rocks in the core of the Chugach Mountains to the north (Fig. 3). Overall, ages decrease by ∼10–15 m.y. (∼50% for the AHe and AFT systems) southward across the Montague Strait fault, similar to the age decrease north of the Contact fault (Fig. 3). ZFT ages (Carlson, 2012), however, are the same or increase southward across the Montague Strait fault (Fig. 3). The ZFT ages (averaging ca. 52 Ma; Carlson, 2012) southeast of the Montague Strait fault are older than the 35 Ma depositional age for the Orca Group sandstone in this region (Hilbert-Wolf, 2012), indicating that these rocks were never buried deep enough to be reset.

AHe ages young southward along the strike of Hinchinbrook and Montague Islands long axes; the youngest ages are at southern Montague Island (transect A–A′; Figs. 2 and 5). However, there is the exception of two older ages on southern Montague Island and one older age on northeastern Hinchinbrook Island (open symbols in Fig. 5). The older AHe ages (5.8 and 6.3 Ma) on Montague Island are located on the footwall block of the Cape Cleare fault (Figs. 4 and 5), indicating that those rocks were not exhumed as rapidly as other southwestern Montague Island rocks. Similarly, the sample on northeastern Hinchinbrook Island has a significantly older AHe age (8.4 Ma) than adjacent samples, and it is located along strike with the Cape Cleare fault farther south (Figs. 4 and 5). We infer these relatively older ages to be part of a separate structural block that was exhumed more slowly than rocks northwest of the Cape Cleare fault and northwest of the structure on northeastern Hinchinbrook Island.

Figure 5.

Apatite (U-Th)/He (AHe) and apatite fission-track (AFT) ages projected onto line A–A′ parallel to Hinchinbrook and Montague Islands long axes (transect location shown in Fig. 2). Age uncertainties are ±1σ. Trend lines show a southward-younging of ages for the AHe system. Ages show no systematic variation from northeast-southwest for the AFT system. Hollow sample symbols are outlier ages on the footwall block of the Cape Cleare fault and southeastern Hinchinbrook Island (see text).

Figure 5.

Apatite (U-Th)/He (AHe) and apatite fission-track (AFT) ages projected onto line A–A′ parallel to Hinchinbrook and Montague Islands long axes (transect location shown in Fig. 2). Age uncertainties are ±1σ. Trend lines show a southward-younging of ages for the AHe system. Ages show no systematic variation from northeast-southwest for the AFT system. Hollow sample symbols are outlier ages on the footwall block of the Cape Cleare fault and southeastern Hinchinbrook Island (see text).

In contrast to the AHe age trends, there is no systematic northeast to southwest AFT age trend (Fig. 5). The lack of an AFT age trend suggests that exhumation was relatively uniform along the islands while rocks were cooling through the AFT closure temperature.

Distinct changes in AHe and AFT age patterns also occur across known faults (Fig. 6). AHe and AFT ages decrease southward by more than half across the Montague Strait and Hanning Bay faults in the southwest Montague Island area (transect B–B′; Figs. 2 and 6A). However, this age change is across a broad ∼25 km region and may be related to regional rock uplift and exhumation variations rather than offset slip across the Montague Strait fault. Farther southeast across the Patton Bay fault, an average ∼1.5 m.y. increase in AHe ages and average ∼4.5 m.y. increase in AFT ages from the hanging-wall block to the footwall block may indicate significant changes in rock uplift along the Patton Bay fault in the past ∼5 m.y. The contrast in ages across the Hanning Bay, Patton Bay, and Cape Cleare faults since the late Miocene indicates that these structures have been active on million-year time scales and have exhumed rocks from depths of >4 km along narrow, fault-bounded blocks.

Figure 6.

Cross sections across the Montague Strait fault and Montague and Hinchinbrook Islands (transect locations shown in Fig. 2), showing apatite (U-Th)/He (AHe) and apatite fission-track (AFT) ages relative to fault locations. (A) B–B′. (B) C–C′. Age uncertainties are ±1σ. Colored bands generally outline range in ages and red or blue line is average age for the region. Arrows along fault location markers (gray dashed lines) represent relative vertical displacement direction for that fault.

Figure 6.

Cross sections across the Montague Strait fault and Montague and Hinchinbrook Islands (transect locations shown in Fig. 2), showing apatite (U-Th)/He (AHe) and apatite fission-track (AFT) ages relative to fault locations. (A) B–B′. (B) C–C′. Age uncertainties are ±1σ. Colored bands generally outline range in ages and red or blue line is average age for the region. Arrows along fault location markers (gray dashed lines) represent relative vertical displacement direction for that fault.

Faults and structural lineaments are more dispersed farther northeast on northern Montague and Hinchinbrook Islands, where there is a more complex network of faults (Fig. 2) (Nelson et al., 1985). Both AHe and AFT ages of samples from northern Montague and Hinchinbrook Islands decrease toward the southeast across the Montague Strait fault region (transect C–C′; Figs. 2 and 6B). AHe ages are ca. 5 Ma on both sides of the Rude River fault on Hinchinbrook Island, suggesting little differential exhumation across the fault in the past 5 m.y. AFT ages decrease to ca. 2.5 Ma to the southeast of the Rude River fault (Fig. 6B), but there is no definitive break in the AFT ages across the Rude River fault.

Cooling and Exhumation Rates

Cooling and exhumation rates for single samples were derived from sample-specific closure temperatures, an averaged geothermal gradient that accounts for thermal advection of rapidly cooled samples, assumed steady-state topography, and a surface temperature of 0 °C (Péwé, 1975). For the AFT ages, a closure temperature of 110 °C was assumed (Reiners and Brandon, 2006). Note that variations in the AFT closure temperature can result from variable kinetic parameters, but Dpar for samples in this study varies little. Closure temperatures for AHe ages were determined using the program CLOSURE (Brandon et al., 1998) using average spherical radii and cooling rates specific to each sample. The closure depth (Zc) for each sample was calculated using a modified equation of Brandon et al. (1998):
graphic
where h is the sample elevation, hm is the average elevation for a 10 km radius around the sample location, Ts is the surface temperature, Tc is the effective closure temperature, and go is the geothermal gradient. The average elevation was computed to account for the effect of the long wavelength topography on the shape of shallow isotherms (Stüwe et al., 1994; Mancktelow and Grasemann, 1997).

For samples south of the Montague Strait fault, average cooling rates are ∼6.5 °C/m.y. between AFT and AHe closure temperatures, and increase to ∼16 °C/m.y. in the past 5 m.y. or less (line A, Fig. 7). On Montague Island, the average cooling rate is ∼5 °C/m.y. between AFT and AHe closure temperatures, increasing to ∼20 °C/m.y. after AHe closure (line B, Fig. 7). On the hanging-wall block of the Patton Bay fault on southern Montague Island, the average cooling rate is 6.5 °C/m.y. after AFT closure and increases to ∼35 °C/m.y. after AHe closure (line C, Fig. 7). These relationships across southern Prince William Sound demonstrate a regional increase in cooling rate in the past ∼5 m.y., or since the time of AHe closure. More locally, cooling rates increased between ca. 5 and 2 Ma for rocks on the hanging wall of the Patton Bay fault on southern Montague Island.

Figure 7.

Age and closure temperature plot for all apatite (U-Th)/He (AHe), apatite fission-track (AFT), and zircon fission-track (ZFT) data south of the Montague Strait fault. Gray lines are simple cooling paths for each sample. Average cooling paths for the AHe and AFT systems are shown by the bold black lines. Line A is the average cooling rate for all samples, line B is the average for Montague Island, and line C is the average cooling path on the hanging-wall block of the Patton Bay fault. Potential time-temperature paths are outlined by the green shaded region. Dashed line is the AFT cooling rate extrapolated back to 200 °C. Maximum ZFT age is constrained by the depositional age of the Orca Group in southern Prince William Sound from Hilbert-Wolf (2012).

Figure 7.

Age and closure temperature plot for all apatite (U-Th)/He (AHe), apatite fission-track (AFT), and zircon fission-track (ZFT) data south of the Montague Strait fault. Gray lines are simple cooling paths for each sample. Average cooling paths for the AHe and AFT systems are shown by the bold black lines. Line A is the average cooling rate for all samples, line B is the average for Montague Island, and line C is the average cooling path on the hanging-wall block of the Patton Bay fault. Potential time-temperature paths are outlined by the green shaded region. Dashed line is the AFT cooling rate extrapolated back to 200 °C. Maximum ZFT age is constrained by the depositional age of the Orca Group in southern Prince William Sound from Hilbert-Wolf (2012).

A background geothermal gradient (gi) for southern Prince William Sound was computed based on the surface heat flow and thermal conductivity (Blackwell and Richards, 2004; Huang et al., 2008; Batir et al., 2013). Assuming a background surface heat flow for Prince William Sound of 45 mW/m2 (Blackwell and Richards, 2004; Batir et al., 2013) and a thermal conductivity of 2.5 W/mK for typical fine-grained sedimentary rocks (Huang et al., 2008), we compute a gi of 18 °C/km. This background gi was then given a ±20% variability to account for variations in heat flow and thermal conductivity resulting in a range in gi values of 14.4–21.6 °C/km (see Supplemental File [footnote 1] for analysis).

Regional processes may affect the thermal structure of the crust overriding the Yakutat microplate and may influence low-temperature cooling ages. These processes include ridge subduction during the Paleocene–Eocene (e.g., Haeussler et al., 2003; Idleman et al., 2011; Benowitz et al., 2012) and later cooling related to subduction of the relatively cool Yakutat microplate. Thermal length arguments (e.g., Turcotte and Schubert, 2002) suggest that the transitory thermal effects of Paleocene–Eocene ridge subduction in the 25-km-thick overriding plate would have dissipated in ∼15–20 m.y., prior to the Miocene and younger cooling documented by our ages. The present-day regional geothermal gradient is relatively low, but it is consistent with flat-slab subduction thermal models (e.g., Gutscher and Peacock, 2003) and models of thermal effects of subduction in general (e.g., Cloos, 1985). We use the relatively low present-day geothermal gradient in our exhumation analysis, but if the slab cooling effects were greater in the past, then the exhumation rates discussed here may be a minimum. The relatively young ages in our study and the local scale of the age variations suggest that regional slab refrigeration or ridge subduction effects do not cause the age patterns we observe, thus we assume that cooling is related to exhumation.

It is well known that the advection of hotter rocks toward the surface during exhumation causes geothermal gradients to increase (e.g., Kappelmeyer and Haenel, 1974; Powell et al., 1988; Ehlers, 2005). We apply a simple correction to the background geothermal gradient by assuming erosion durations consistent with sample ages and typical exhumation rates of between ∼0.5 and 2 mm/yr. Advection corrections increase gi between 10% and 80%, resulting in sample-specific advection-corrected geothermal gradient (go) values between 23 and 38 °C/km (Tables SF3 and SF4 in the Supplemental File [see footnote 1]). The median of the two corrected end-member go values for each sample was used in Equation 1 to compute the closure depth and the resulting exhumation rates (ε = Zc/t) for each sample age (t) (Table 1).

For the AHe system, the average closure temperature for southern Prince William Sound is ∼66 °C, average Zc is ∼2.7 km, and overall average exhumation rates are 0.7 mm/yr. For the AFT system, a 110 °C closure temperature was used for all samples. The average depth to closure is ∼4.5 km, and average exhumation rates are 0.4 mm/yr (Tables SF3 and SF4 in the Supplemental File [see footnote 1]). On the hanging wall of the Patton Bay fault of southern Montague Island, exhumation rates are as high as 2.5 mm/yr based on AHe closure, but average 1.5 and 0.6 mm/yr based on AHe and AFT closure, respectively. Overall, exhumation rates increased in the past ∼5 m.y. or less (Fig. 7) across both Montague and Hinchinbrook Islands, but on southern Montague Island the exhumation rates increased in the past ∼2 m.y.

Timing and Magnitude of Rock Uplift across Faults

AHe and AFT age differences or similarities across known faults on Montague and Hinchinbrook Islands allow estimates of relative rock uplift across the faults, and therefore estimates of long-term fault offset. Based on the AHe cooling age data, samples from the Patton Bay fault hanging wall cooled at a rate of 35 °C/m.y. since ca. 2 Ma, which is the average AHe age of the hanging-wall samples (Figs. 6A and 7). Samples from the footwall block of the Patton Bay fault cooled at a rate of 14 °C/m.y. since 3.3 Ma. Assuming constant cooling rates across the Patton Bay fault since 3.3 m.y. and an average geothermal gradient of 25 °C/km, the temperature change differential between the footwall and hanging-wall blocks is 65 °C, leading to a difference in rock uplift of ∼2.6 km across the fault since 3.3 Ma. The Patton Bay fault is estimated to dip 60° based on surface ruptures from the 1964 earthquake (Plafker, 1967) and apparent dip estimates in the TACT Prince William Sound deep seismic reflection line (Haeussler et al., 2014; Liberty et al., 2013). Correcting for the 60° dip leads to a total offset of ∼3 km across the Patton Bay fault since 3.3 Ma; note that total offset amounts are greater if the fault dip is less, as suggested by Liberty et al. (2013). AFT age similarity across the Patton Bay fault indicates that cooling rates were likely the same on the footwall and hanging-wall blocks while cooling through AFT closure, suggesting minimal differential exhumation across the Patton Bay fault between ca. 10 Ma (AFT closure) and 3.3 Ma (AHe closure).

On northern Montague and Hinchinbrook Islands, the clustering of AHe ages ca. 4.5 Ma allows estimates to be placed on the maximum amount of slip on these faults because vertical fault offset could not have been greater than the depth that corresponds to the minimum temperature of the AHe partial retention zone. Assuming an average advection-corrected geothermal gradient of 25 °C/km and a minimum PRZ temperature of 40 °C, the maximum amount of differential rock uplift is ∼1.6 km in the past ∼4.5 m.y. on northern Montague and Hinchinbrook Islands.

The depositional age for Orca Group sandstone (younger than 35 Ma; Hilbert-Wolf, 2012) in southern Prince William Sound is an important constraint because it indicates that the sediments were at surface temperatures after 35 Ma. If the AHe and AFT ages are reset, but the ZFT ages are not reset (Carlson, 2012), then the Orca Group had to have been buried to depths and corresponding temperatures of between ∼110 °C and ∼200 °C, then reexhumed after ca. 35 Ma (Fig. 7). The maximum AFT age is the minimum age that the rocks at Hinchinbrook and Montague Islands were at 110–200 °C. The shaded region in Figure 7 represents the range of cooling paths rocks may have taken prior to passing through AFT closure temperature. If the average AFT cooling rate (line A, Fig. 7) is constant from 200 °C, then this rate may be extrapolated to as long ago as ca. 23 Ma (dashed line, Fig. 7). We acknowledge that there is considerable uncertainty in this analysis, but it provides loose constraints on the potential timing of maximum temperature estimates for rocks on Montague and Hinchinbrook Islands. Given that rocks were buried to temperatures as high as 200 °C, the maximum amount of rock uplift and exhumation in southern Prince William Sound (assuming a constant average geothermal gradient of 25 °C/km) is ∼8 km since ca. 23–35 Ma. In addition, the reset AFT ages indicate that the minimum exhumation magnitude on Montague and Hinchinbrook Islands is ∼4.8 km, which occurred in the past ∼7–10 m.y.

Regional Analysis

One of our goals is to examine the relationship between the zone of very young AHe ages (younger than 1 Ma) and rapid exhumation south of the Bagley fault in the Saint Elias region (Spotila and Berger, 2010) and the thermochronology data across the Copper River delta into Prince William Sound. Based on our new ages, the region of young cooling ages in the Saint Elias Mountains does not appear to extend westward into Prince William Sound (Fig. 8), but rather bends southward at the Miles Corner to connect with the Kayak Island zone and Aleutian megathrust, as suggested by Spotila and Berger (2010) (red dashed area, Fig. 8). In this interpretation, the Kayak Island zone and Ragged Mountain fault link the Miles Corner region with the Aleutian megathrust and are well-defined boundaries between transpression and convergence. Even though the band of youngest ages either ends at Miles Corner or bends south, some focused rock uplift may be transferred west into Prince William Sound, because rocks with young ages (4 Ma AHe) continue west across the Copper River delta into the Hinchinbrook and Montague Islands region. The rapid exhumation in the Saint Elias region is focused along the Bagley backstop (Berger et al., 2008b). We propose that this backstop continues westward as the Montague Strait fault (Fig. 8), but with lower exhumation rates than in the Saint Elias orogen. A broader zone of deformation extending from the Kayak Island fault system to southern Prince William Sound (area A, Fig. 8) may also accommodate the overall rock uplift differences south of the backstops in southern Prince William Sound and the Saint Elias area. Uplifted fault blocks during the 1964 earthquake and the presence of reverse faults (Haeussler et al., 2014) outboard of southern Prince William Sound to Middleton Island are consistent with a distributed deformation zone.

Figure 8.

Contour map of new and published apatite (U-Th)/He (AHe) data from southern Alaska. Area outlined by red dashes shows the possible region of rapid exhumation from the Saint Elias Mountains continuing south along the Kayak Island zone and Aleutian megathrust, as described by Spotila and Berger (2010). Region labeled A indicates a possible broad deformation region that extends from the Kayak Island fault zone to southern Prince William Sound. Green line indicates interpreted subducted region of the Yakutat microplate from Fletcher and Freymueller (2003), Eberhart-Phillips et al. (2006), and Fuis et al. (2008). White dots are sample locations from this study and others. HI—Hinchinbrook Island; MI—Montague Island; MDI—Middleton Island; KI—Kayak Island; RI—Ragged Island thrust fault; PZ—Pamplona fold-thrust zone; CSEF—Chugach–Saint Elias fault; MSF—Montague Strait fault.

Figure 8.

Contour map of new and published apatite (U-Th)/He (AHe) data from southern Alaska. Area outlined by red dashes shows the possible region of rapid exhumation from the Saint Elias Mountains continuing south along the Kayak Island zone and Aleutian megathrust, as described by Spotila and Berger (2010). Region labeled A indicates a possible broad deformation region that extends from the Kayak Island fault zone to southern Prince William Sound. Green line indicates interpreted subducted region of the Yakutat microplate from Fletcher and Freymueller (2003), Eberhart-Phillips et al. (2006), and Fuis et al. (2008). White dots are sample locations from this study and others. HI—Hinchinbrook Island; MI—Montague Island; MDI—Middleton Island; KI—Kayak Island; RI—Ragged Island thrust fault; PZ—Pamplona fold-thrust zone; CSEF—Chugach–Saint Elias fault; MSF—Montague Strait fault.

Relationships between Exhumation and Topography

Along most active orogens, high exhumation rates coincide with high elevations and high relief. Often the regions of high exhumation rate are offset from the highest elevations where high precipitation rates (Reiners et al., 2003; Willett et al., 2001) or erosive alpine glaciers (e.g., Tomkin, 2007; Berger et al., 2008a; Arkle et al., 2013) cause rapid erosion on the windward flank of the orogen. The correspondence between elevations and glacier equilibrium-line altitude (ELA) suggests that glaciers behave as buzz saws that limit orogen elevation and width (e.g., Brozović et al., 1997; Meigs and Sauber, 2000; Spotila et al., 2004). In the Saint Elias Mountains, where glaciers cover much of the windward flank of the orogen, the coincidence of the ELA with zones of rapid exhumation suggests that glaciers partly control the rock uplift and exhumation (Meigs and Sauber, 2000; Spotila et al., 2004; Berger and Spotila, 2008; Berger et al., 2008a, 2008b).

Our data from Montague and Hinchinbrook Islands show a lack of correlation between AHe age (or exhumation rates and magnitudes derived from the ages) and elevation. Computed exhumation magnitudes along the trend of Montague and Hinchinbrook Islands were derived using the AHe exhumation rates and an exhumation duration of 2 m.y. (Fig. 9); the duration is based on the average AHe age of samples from the Patton Bay fault hanging wall. In general, exhumation magnitude increases from northeast to southwest, with highest exhumation magnitudes at the south end of Montague Island (Fig. 9). Range-crest elevations along the island-parallel transect are ∼800 m on both Hinchinbrook and Montague Islands, but elevation decreases to below sea level between them at Hinchinbrook Entrance (the inlet between Hinchinbrook and Montague Islands). Exhumation magnitude is relatively constant along the transect, even across Hinchinbrook Entrance. At the southern end of Montague Island, elevation decreases to sea level whereas the exhumation magnitudes increase abruptly (Fig. 9). We expect that elevation would be greatest at the south end of Montague Island because it has the highest exhumation rate and is not a focus region of high orographic precipitation or the alpine glacier–dominated windward flank of an orogen. The lack of coincidence between high exhumation magnitude (or rate) and high-elevation regions has been documented in other areas, especially where Quaternary glaciers eroded the landscape. In central and northern Fiordland, New Zealand, AHe ages are typically 1–3 Ma, but elevations are <1500 m (House et al., 2005). House et al. (2005) interpreted the changes in ages across Fiordland to be due to differential exhumation across faults, but extensive glaciation caused regional erosion across the faults after ca. 2 Ma (Sutherland et al., 2009). Along the Fairweather corridor adjacent to the Fairweather fault in southeast Alaska, AHe ages are typically younger than 1 Ma (McAleer et al., 2009) across 50 km regions of low topography that are relatively glacially denuded. McAleer et al. (2009) suggested that glacial erosion in the Fairweather corridor was high enough to limit the development of topography even where exhumation rates were highest. Whereas Hinchinbrook and Montague Islands are not currently glacially dominated or a focus region of high orographic precipitation, Pleistocene glaciers extended ∼100 km south of their present location (Kaufman and Manley, 2004). Thus, we infer that glaciers were able to erode Montague and Hinchinbrook Islands rapidly enough to limit topographic growth even where rock uplift rates were the highest, attesting to the buzz saw potential of glaciers (e.g., Brozović et al., 1997; Meigs and Sauber, 2000; Spotila et al., 2004).

Figure 9.

Plot comparing island-parallel topographic profile (gray dashed line, transect A–A′ from Fig. 2) and sample exhumation magnitudes (green triangles). Exhumation magnitudes represent exhumation for past 2 m.y. at sample-specific exhumation rates. Elev.—elevation.

Figure 9.

Plot comparing island-parallel topographic profile (gray dashed line, transect A–A′ from Fig. 2) and sample exhumation magnitudes (green triangles). Exhumation magnitudes represent exhumation for past 2 m.y. at sample-specific exhumation rates. Elev.—elevation.

Although glacial erosion likely limited topographic growth, the maximum elevations are probably also limited by the narrowness of rock uplift along the splay faults. Both Hinchinbrook and Montague Islands are at most 20 km wide, and <10 km in many locations. For example, AHe ages on the Yucaipa Ridge block along the San Andreas fault in southern California are 0.7–1.6 Ma across a 5–10-km-wide ridge between fault strands (Spotila et al., 1998). Elevations along the ridge are ∼1000 m above base level. In this case, where glaciers have not eroded the landscape, oversteepening of the slopes between the fault strands regulated the maximum elevations along the rapidly exhuming narrow ridge (Spotila et al., 1998). If rock uplift on Montague and Hinchinbrook Islands is mostly focused along megathrust fault splays, then the lack of high topography may be partly due to the narrowness of the uplifted region.

Causes of Rock Uplift and Exhumation

The AHe age patterns (Fig. 4) clearly indicate that long-term exhumation rates increase to the southwest and are highest at the southwest end of Montague Island. The southwest increase in exhumation rate and magnitude also mimics the southwest increase in the amount of uplift and fault offset in the 1964 earthquake (Plafker, 1967, 1969). There was no measured offset on the Cape Cleare fault onshore after the 1964 earthquake, but seismic data of Liberty et al. (2013) show a 40 m scarp offshore to the southwest. Thus the long-term pattern of exhumation reflects the short-term seismogenic uplift patterns. Given (1) the narrow geometry of Montague and Hinchinbrook Islands; (2) the relatively young thermochronometer ages from samples across the islands that are adjacent to relatively older ages north of the Montague Strait fault; (3) a well-defined topographic expression of faults onshore and their seismic and bathymetric expression offshore; and (4) the correlation between long-term exhumation and coseismic deformation, we infer that exhumation is controlled dominantly by rock uplift along faults. We also infer that Hinchinbrook and Montague Islands have remained the focus of exhumation for at least the past 2–3 m.y., with higher rates to the southwest.

Even though we interpret the majority of exhumation to be on narrow fault-bounded blocks on Montague and Hinchinbrook Islands, we cannot rule out the possibility that rock uplift is spread over a broader region offshore to the southeast. AHe ages on the footwall of the Cape Cleare fault are ca. 6 Ma, indicating late Miocene and younger exhumation, but at a lower long-term rate than rocks on the hanging-wall block. In addition, the shorelines on the Cape Cleare fault footwall and on Middleton Island located ∼100 km to the southeast were uplifted in the 1964 earthquake (Plafker, 1969). Thus the exhumation focused along fault splays may be part of broader region of rock uplift caused by underplating along the megathrust. Liberty et al. (2013) reprocessed the TACT deep seismic reflection data and interpreted each of the splay faults to sole into the subduction megathrust separately; they showed a subhorizontal megathrust located 18–20 km beneath Montague Island and a lens-shaped zone of reflections below the megathrust, interpreted as thickening due to underplating and duplexing and coincident with where the Patton Bay, Hanning Bay, and Cape Cleare faults splay off the megathrust (Haeussler et al., 2014). Liberty et al. (2013) inferred that the thickened region causes locking of the megathrust below the western part of Prince William Sound (Zweck et al., 2002), which initiates the splay faults that project to the surface parallel to one another. Underplating and duplexing along the megathrust may also cause broad rock uplift that extends southward and away from the more focused rock uplift and exhumation on Montague and Hinchinbrook Islands. Increased rock cooling starting ca. 2–3 Ma on southern Montague Island is coincident with increased mountain glacial erosion worldwide (Herman et al., 2013) and with the onset of glacial sedimentation in the Saint Elias region (Lagoe et al., 1993; Lagoe and Zellers, 1996; Cowan et al., 2013). Climate cooling and glacier erosion may have enhanced erosion rates on Montague and Hinchinbrook Islands during the Pleistocene, but if glacial erosion was the sole cause of increased rock uplift in southern Prince William Sound, then other parts of Prince William Sound should have had the same rapid uplift during this time. Pavlis et al. (2012) suggested that sediments originally shed from the Saint Elias orogen 2–3 Ma in response to cooling climate and glacial erosion caused duplex stacking and underplating under the Yakataga segment farther to the southeast. Mankhemthong et al. (2013) used gravity and magnetic data from the Chugach Mountains north of Prince William Sound to suggest that sediments shed from the Saint Elias Mountains were carried along and underplated above the Yakutat microplate. Thus, the increased volume of subducting sediments starting ca. 2–3 Ma may have also enhanced underplating along the megathrust under southern Prince William Sound, which then increased rock uplift along the megathrust splay faults. We infer that the high rock uplift rate since 2–3 Ma on Montague Island is due mainly to splay faulting and related underplating. Recent glaciation at the surface has accommodated this accelerated exhumation across a narrow region, but has also masked the topographic effects of increased rock uplift.

The thermochronology data from this study provide insight into the style of deformation above the subduction décollement in the Prince William Sound of southern Alaska. Our ages, combined with previously published ages, show that southern Prince William Sound, between the Cape Cleare and Montague Strait faults, is a region of focused exhumation and deformation likely caused by Yakutat flat slab subduction. AHe and AFT ages on Montague and Hinchinbrook Islands are as young as 1.1 and 4.4 Ma, respectively; the youngest ages are at the southwest end of Montague Island. These ages vary across major faults, especially on southwestern Montague Island across the Hanning Bay, Patton Bay, and Cape Cleare faults. Exhumation rates across the Patton Bay fault are ∼2 times higher on the hanging-wall block than on the footwall block, leading to as much as 3 km of slip across the Patton Bay fault in the past 3.3 m.y., with decreasing slip to the northeast. The northeast to southwest increase in exhumation rate is coincident with the trend of increasing coseismic uplift from the 1964 earthquake, suggesting that fault-related rock uplift is long lived. Thermochronometer ages are 2–5 times greater north of the Montague Strait fault than to the south, suggesting that this fault is part of a major structural transition that acts as a mechanically strong backstop to deformation, and faster exhumation to the south on Montague and Hinchinbrook Islands. The Montague Strait fault backstop may be a westward mechanical continuation of the Bagley fault system backstop in the Saint Elias orogen, but exhumation is slower in the Montague and Hinchinbrook Islands area, where deformation may be distributed between the Aleutian Trench and southern Prince William Sound.

Splay faulting above the subduction décollement is interpreted as the primary cause for rapid exhumation in southern Prince William Sound. More specifically, rock is being uplifted via splay faulting that is rooted to the Yakutat–North America plate interface. Underplating at the plate interface in the past ∼5 m.y., with increased effects since ca. 3–2 Ma, may be enhancing or driving splay fault formation in southern Prince William Sound. The lack of correlation between exhumation rates or magnitudes and topography suggests that a cooling climate and glacial erosion played a role in limiting topographic growth. Notably, this study shows that splay faults with historic coseismic rupture separated by only a few kilometers can facilitate kilometer-scale exhumation above shallowly subducting plates at million-year time scales.

We thank K. Farley and L. Hedges (California Institute of Technology, Pasadena) for (U-Th)/He analyses. We also thank Matan Salmon for his help as field assistant in the Prince William Sound. Insightful reviews by J. Benowitz, C. Davidson, Associate Editor T. Pavlis, and an anonymous reviewer helped us focus and improve this paper. Funding was provided by Donors of the Petroleum Research Fund administered by the American Chemical Society and the John T. Dillon Alaska Research Fund administered by the Geologic Society of America.

1Supplemental File. PDF file that outlines methods for determining inter-grain age variability using the effective uranium content of samples from this study and a corresponding figure, our fission-track analysis, methods for reporting weighted mean AHe ages, and methods for estimating geothermal gradient specific to our study area and samples. It also contains tables with detailed AHe and AFT analytical data and AHe/AFT exhumation rate calculations for all thermochronometer data reported in this study. These supplemental tables and figure will be denoted throughout this manuscript with an “SF” in front of them. If you are viewing the PDF of this paper or reading it offline, please visit http://dx.doi.org/10.1130/GES01036.S1 or the full-text article on www.gsapubs.org to view the Supplemental File.
1.
Arkle
J.C.
Armstrong
P.A.
Haeussler
P.J.
Prior
M.G.
Hartman
S.
Sendziak
K.L.
Brush
J.A.
,
2013
,
Mechanisms of rock uplift above flat slab subduction in the western Chugach Mountains and Prince William Sound of the southern Alaska syntaxis
:
Geological Society of America Bulletin
 , v.
125
, p.
776
793
,
doi:10.1130/B30738.1
.
2.
Armstrong
P.A.
Haeussler
P.J.
Sendziak
K.L.
Arkle
J.C.
,
2008
,
The western Chugach core: Locus of subduction-related exhumation? [abs.]
, in
Garver
J.I.
Montario
M.J.
, eds.,
FT2008: Proceedings, 11th International Conference on Thermochronometry, Anchorage, Alaska, 2008, Abstracts with Programs
 , p.
8
10
.
3.
Batir
J.F.
Blackwell
D.D.
Richards
M.C.
,
2013
,
Updated surface heat flow map of Alaska
:
Geothermal Resources Council Transactions
 , v.
37
, p.
2
23
.
4.
Benowitz
J.A.
Layer
P.W.
Armstrong
P.A.
Perry
S.E.
Haeussler
P.J.
Fitzgerald
P.G.
VanLaningham
S.
,
2011
,
Spatial variations in focused exhumation along a continental-scale strike-slip fault: The Denali fault of the eastern Alaska Range
:
Geosphere
 , v.
7
, p.
455
467
,
doi:10.1130/GES00589.1
.
5.
Benowitz
J.A.
Haeussler
P.J.
Layer
P.W.
O’Sullivan
P.B.
Wallace
W.K.
Gillis
R.J.
,
2012
,
Cenozoic tectono-thermal history of the Tordrillo Mountains, Alaska: Paleocene–Eocene ridge subduction, decreasing relief, and late Neogene faulting
:
Geochemistry Geophysics Geosystems
 , v.
13
,
Q04009
,
doi:10.1029/2011GC003951
.
6.
Benowitz
J.A.
Layer
P.W.
VanLaningham
S.
,
2013
,
Persistent long-term (c. 24 Ma) exhumation in the Eastern Alaska Range constrained by stacked thermochronology
, in
Jourdan
F.
et al
., eds.,
Advances in 40Ar/39Ar dating: From archaeology to planetary sciences: Geological Society of London Special Publication 378
 , p.
225
243
,
doi:10.1144/SP378.12
.
7.
Berger
A.L.
Spotila
J.A.
,
2008
,
Denudation and deformation in a glaciated orogenic wedge: The St. Elias orogen, Alaska
:
Geology
 , v.
36
, p.
523
526
,
doi:10.1130/G24883A.1
.
8.
Berger
A.L.
10 others
,
2008a
,
Quaternary tectonic response to intensified glacial erosion in an orogenic wedge
:
Nature Geoscience
 , v.
1
, p.
793
799
,
doi:10.1038/ngeo334
.
9.
Berger
A.L.
Spotila
J.A.
Chapman
J.B.
Pavlis
T.L.
Enkelmann
E.
Ruppert
N.A.
Buscher
J.T.
,
2008b
,
Architecture, kinematics, and exhumation of a convergent orogenic wedge: A thermochronological investigation of tectonic-climatic interactions within the central St. Elias orogen, Alaska
:
Earth and Planetary Science Letters
 , v.
270
, p.
13
24
,
doi:10.1016/j.epsl.2008.02.034
.
10.
Blackwell
D.D.
Richards
M.
,
2004
,
Geothermal map of North America
:
American Association of Petroleum Geologists, scale 1:6,500,000
 .
11.
Bol
A.J.
Gibbons
H.
,
1992
,
Tectonic implications of out-of-sequence faults in an accretionary prism, Prince William Sound, Alaska
:
Tectonics
 , v.
11
, p.
1288
1300
,
doi:10.1029/92TC01327
.
12.
Bol
A.J.
Roeske
S.M.
,
1993
,
Strike-slip faulting and block rotation along the contact fault system, eastern Prince William Sound, Alaska
:
Tectonics
 , v.
12
, p.
49
62
,
doi:10.1029/92TC01324
.
13.
Bradley
D.
Kusky
T.
Haeussler
P.
Goldfarb
R.
Miller
M.L.
Dumoulin
J.
Nelson
S.W.
Karl
S.
,
2003
,
Geologic signature of early Tertiary ridge subduction in Alaska
, in
Sisson
V.E.
et al
., eds.,
Geology of a transpressional orogen developed during ridge-trench interaction along the North Pacific margin: Geological Society of America Special Paper 371
 , p.
19
49
,
doi:10.1130/0-8137-2371-X.19
.
14.
Brandon
M.T.
Roden-Tice
M.K.
Garver
J.I.
,
1998
,
Late Cenozoic exhumation of the Cascadia accretionary wedge in the Olympic Mountains, northwest Washington State
:
Geological Society of America Bulletin
 , v.
110
, p.
985
1009
,
doi:10.1130/0016-7606(1998)110<0985:LCEOTC>2.3.CO;2
.
15.
Brocher
T.M.
Moses
M.A.
Fisher
M.A.
Stephens
C.D.
Geist
E.L.
,
1991
,
Images of the plate boundary beneath southern Alaska
, in
Meissner
R.
et al
., eds.,
Continental lithosphere: Deep seismic reflections: American Geophysical Union Geodynamics Series 22
 , p.
241
246
.
16.
Brozović
N.
Burbank
D.W.
Meigs
A.J.
,
1997
,
Climatic limits on landscape development in the northwestern Himalaya
:
Science
 , v.
276
, p.
571
574
,
doi:10.1126/science.276.5312.571
.
17.
Bruhn
R.L.
Pavlis
T.L.
Plafker
G.
Serpa
L.
,
2004
,
Deformation during terrane accretion in the Saint Elias orogen, Alaska
:
Geological Society of America Bulletin
 , v.
116
, p.
771
787
,
doi:10.1130/B25182.1
.
18.
Buscher
J.T.
Berger
A.L.
Spotila
J.A.
,
2008
,
Exhumation in the Chugach-Kenai Mountain belt above the Aleutian subduction zone, southern Alaska
, in
Freymueller
J.T.
et al
., eds.,
Active tectonics and seismic potential of Alaska: American Geophysical Union Geophysical Monograph 179
 , p.
151
166
,
doi:10.1029/179GM08
.
19.
Carlson
B.M.
,
2012
,
Cooling and provenance revealed through detrital zircon fission track dating of the Upper Cretaceous Valdez Group and Paleogene Orca Group in Western Prince William Sound, Alaska
, in
Varga
R.
, ed.,
Proceedings of the Twenty-Fifth Keck Research Symposium in Geology, Amherst, Massachusetts
 :
Pomona College, Claremont, California
,
Keck Geology Consortium
, p.
8
16
.
20.
Chapman
J.B.
Worthington
L.L.
Pavlis
T.L.
Bruhn
R.L.
Gulick
S.P.
,
2011
,
The Suckling Hills fault, Kayak Island zone, and accretion of the Yakutat microplate, Alaska
:
Tectonics
 , v.
30
,
TC6011
,
doi:10.1029/2011TC002945
.
21.
Christeson
G.L.
Gulick
S.P.
van Avendonk
H.J.
Worthington
L.L.
Reece
R.S.
Pavlis
T.L.
,
2010
,
The Yakutat terrane: Dramatic change in crustal thickness across the Transition fault, Alaska
:
Geology
 , v.
38
, p.
895
898
,
doi:10.1130/G31170.1
.
22.
Cloos
M.
,
1985
,
Thermal evolution of convergent plate margins: Thermal modeling and reevaluation of isotopic Ar-ages for blueschists in the Franciscan Complex of California
:
Tectonics
 , v.
4
, p.
421
433
,
doi:10.1029/TC004i005p00421
.
23.
Cole
R.B.
Nelson
S.W.
Layer
P.W.
Oswald
P.J.
,
2006
,
Eocene volcanism above a depleted mantle slab window in southern Alaska
:
Geological Society of America Bulletin
 , v.
118
, p.
140
158
,
doi:10.1130/B25658.1
.
24.
Cowan
D.S.
,
2003
,
Revisiting the Baranof–Leech River hypothesis for early Tertiary coastwise transport of the Chugach–Prince William terrane
:
Earth and Planetary Science Letters
 , v.
213
, p.
463
475
,
doi:10.1016/S0012-821X(03)00300-5
.
25.
Cowan
E.A.
Forwick
M.
Bahlburg
H.
Childress
L.B.
Moy
C.M.
Muller
J.
Ribeiro
F.
Ridgway
K.D.
,
2013
,
Southern Alaska glaciations recorded in deep-sea diamicts: Preliminary results from IODP Expedition 341
:
American Geophysical Union, fall meeting abs. T22C-07
 .
26.
Davidson
C.
Garver
J.I.
Hilbert-Wolf
H.L.
Carlson
B.
,
2011
,
Maximum depositional age of the Paleocene to Eocene Orca Flysch, Prince William Sound, Alaska
:
Geological Society of America Abstracts with Programs
 , v.
43
, no.
5
, p.
439
.
27.
Donelick
R.A.
O’Sullivan
P.B.
Ketcham
R.A.
,
2005
,
Apatite fission-track dating
, in
Reiners
P.W.
Ehlers
T.A.
, eds.,
Low-temperature thermochronology: Techniques, interpretations, and applications: Reviews in Mineralogy and Geochemistry Volume 58
 , p.
49
94
,
doi:10.2138/rmg.2005.58.3
.
28.
Dumitru
T.A.
,
2000
,
Fission-track geochronology in Quaternary geology
, in
Noller
J.S.
et al
., eds.,
Quaternary geochronology: Methods and applications
 :
Washington, D.C.
,
American Geophysical Union Reference Shelf
, v.
4
, p.
131
155
,
doi:10.1029/RF004p0131
.
29.
Dunkl
I.
,
2002
,
Trackkey: A Windows program for calculation and graphical presentation of fission track data
:
Computers & Geosciences
 , v.
28
, p.
3
12
,
doi:10.1016/S0098-3004(01)00024-3
.
30.
Eberhart-Phillips
D.
Christensen
D.J.
Brocher
T.M.
Hansen
R.
Ruppert
N.A.
Haeussler
P.J.
Abers
G.A.
,
2006
,
Imaging the transition from Aleutian subduction to Yakutat collision in central Alaska, with local earthquakes and active source data
:
Journal of Geophysical Research
 , v.
111
,
B11303
,
doi:10.1029/2005JB004240
.
31.
Ehlers
T.A.
,
2005
,
Crustal thermal processes and the interpretation of thermochronometer data
, in
Reiners
P.W.
Ehlers
T.A.
, eds.,
Low-temperature thermochronology: Techniques, interpretations, and applications: Reviews in Mineralogy and Geochemistry Volume 58
 , p.
315
350
,
doi:10.2138/rmg.2005.58.12
.
32.
Ehlers
T.A.
Farley
K.A.
,
2003
,
Apatite (U-Th)/He thermochronometry: Methods and applications to problems in tectonic and surface processes
:
Earth and Planetary Science Letters
 , v.
206
, p.
1
14
,
doi:10.1016/S0012-821X(02)01069-5
.
33.
Elliott
J.L.
Larsen
C.F.
Freymueller
J.T.
Motyka
R.J.
,
2010
,
Tectonic block motion and glacial isostatic adjustment in southeast Alaska and adjacent Canada constrained by GPS measurements
:
Journal of Geophysical Research
 , v.
115
,
B09407
,
doi:10.1029/2009JB007139
.
34.
Enkelmann
E.
Garver
J.I.
Pavlis
T.L.
,
2008
,
Rapid exhumation of ice-covered rocks of the Chugach–St. Elias orogen, southeast Alaska
:
Geology
 , v.
36
, p.
915
918
,
doi:10.1130/G2252A.1
.
35.
Enkelmann
E.
Zeitler
P.K.
Pavlis
T.L.
Garver
J.I.
Ridgway
K.D.
,
2009
,
Intense localized rock uplift and erosion in the St Elias orogen of Alaska
:
Nature Geoscience
 , v.
2
, p.
360
363
,
doi:10.1038/ngeo502
.
36.
Falkowski
S.
Enkelmann
E.
Ehlers
T.A.
,
2014
,
Constraining the area of rapid and deep-seated exhumation at the St. Elias syntaxis, southeast Alaska, with detrital zircon fission-track analysis
:
Tectonics
 , v.
33
, p.
597
616
,
doi:10.1002/2013TC003408
.
37.
Farley
K.A.
,
2000
,
Helium diffusion from apatite: General behavior as illustrated by Durango fluorapatite
:
Journal of Geophysical Research
 , v.
105
, p.
2903
2914
,
doi:10.1029/1999JB900348
.
38.
Farley
K.A.
,
2002
,
(U-Th)/He dating: Techniques, calibrations, and applications
, in
Porcelli
D.
et al
., eds.,
Noble gases in geochemistry and cosmochemistry: Mineralogical Society of America Reviews of Mineralogy Volume 47
 , p.
819
844
,
doi:10.2138/rmg.2002.47.18
.
39.
Farley
K.A.
Stockli
D.F.
,
2002
,
(U-Th)/He dating of phosphates: Apatite, monazite, and xenotime
, in
Kohn
M.
et al
., eds.,
Phosphates: Mineralogical Society of America Reviews of Mineralogy Volume 48
 , p.
559
578
,
doi:10.2138/rmg.2002.48.15
.
40.
Farley
K.A.
Wolf
R.A.
Silver
L.T.
,
1996
,
The effects of long alpha-stopping distances on (U-Th)/He ages
:
Geochimica et Cosmochimica Acta
 , v.
60
, p.
4223
4229
,
doi:10.1016/S0016-7037(96)00193-7
.
41.
Ferris
A.
Abers
G.A.
Christensen
D.H.
Veenstra
E.
,
2003
,
High resolution image of the subducted Pacific (?) plate beneath central Alaska, 50–150 km depth
:
Earth and Planetary Science Letters
 , v.
214
, p.
575
588
,
doi:10.1016/S0012-821X(03)00403-5
.
42.
Finzel
E.S.
Trop
J.M.
Ridgway
K.D.
Enkelmann
E.
,
2011
,
Upper plate proxies for flat-slab subduction processes in southern Alaska
:
Earth and Planetary Science Letters
 , v.
303
, p.
348
360
,
doi:10.1016/j.epsl.2011.01.014
.
43.
Fitzgerald
P.
Sorkhabi
R.
Redfield
T.F.
Stump
E.
,
1995
,
Uplift and denudation of the central Alaska Range: A case study in the use of apatite fission track thermochronology to determine absolute uplift parameters
:
Journal of Geophysical Research
 , v.
100
, p.
20,175
20,191
,
doi:10.1029/95JB02150
.
44.
Fletcher
H.J.
Freymueller
J.T.
,
2003
,
New constraints on the motion of the Fairweather fault, Alaska, from GPS observations
:
Geophysical Research Letters
 , v.
30
, p.
1139
,
doi:10.1029/2002GL016476
.
45.
Flowers
R.M.
Ketcham
R.A.
Shuster
D.L.
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
.
46.
Fuis
G.S.
13 others
,
2008
,
Trans-Alaska Crustal Transect and continental evolution involving subduction underplating and synchronous foreland thrusting
:
Geology
 , v.
36
, p.
267
270
,
doi:10.1130/G24257A.1
.
47.
Garver
J.I.
Davidson
C.
Hilbert-Wolf
H.
Carlson
B.
,
2012
,
Provenance and thermal evolution of flysch of the Chugach-Prince William terrane, Alaska
:
Geological Society of America Abstracts with Programs
 , v.
44
, no.
7
, p.
72
.
48.
Garver
J.I.
Davidson
C.M.
DeLuca
M.J.
Pettiette
R.A.
Roe
C.F.
Hilbert-Wolf
H.
,
2013
,
Constraints of the original setting of the flysch of the Chugach and Prince William terranes in Alaska using detrital zircon
: Cordilleran Tectonics Workshop, Kingston, Ontario, Abstracts with Program, 27–30 October, session 84–2, p. 21–23, http://minerva.union.edu/garverj/alaska/garver_CTW_2013_abstracts.pdf.
49.
Gleadow
A.J.
Duddy
I.R.
,
1981
,
A natural long-term annealing experiment for apatite
:
Nuclear Tracks and Radiation Measurements
 , v.
5
, p.
169
174
,
doi:10.1016/0191-278X(81)90039-1
.
50.
Gleadow
A.J.
Duddy
I.R.
Green
P.F.
Laslett
G.M.
Lovering
J.F.
,
1986
,
Confined fission track lengths in apatite—A diagnostic tool for thermal history analysis
:
Contributions to Mineralogy and Petrology
 , v.
94
, p.
405
415
,
doi:10.1007/BF00376334
.
51.
Gutscher
M.A.
Peacock
S.M.
,
2003
,
Thermal models of flat subduction and the rupture zone of great subduction earthquakes
:
Journal of Geophysical Research
 , v.
108
,
2009
,
doi:10.1029/2001JB000787
.
52.
Haeussler
P.J.
,
2008
,
An overview of the neotectonics of interior Alaska: Far-field deformation from the Yakutat microplate collision
, in
Freymueller
J.T.
et al
., eds.,
Active tectonics and seismic potential of Alaska: American Geophysical Union Geophysical Monograph 179
 , p.
83
108
,
doi:10.1029/179GM05
.
53.
Haeussler
P.J.
Bradley
D.C.
Goldfarb
R.J.
Snee
L.W.
Taylor
C.
,
1995
,
Link between ridge subduction and gold mineralization in southern Alaska
:
Geology
 , v.
23
, p.
995
998
,
doi:10.1130/0091-7613(1995)023<0995:LBRSAG>2.3.CO;2
.
54.
Haeussler
P.J.
Bradley
D.C.
Wells
R.E.
Miller
M.L.
,
2003
,
Life and death of the Resurrection plate: Evidence for its existence and subduction in the northeastern Pacific in Paleocene–Eocene time
:
Geological Society of America Bulletin
 , v.
115
, p.
867
880
,
doi:10.1130/0016-7606(2003)115<0867:LADOTR>2.0.CO;2
.
55.
Haeussler
P.J.
O’Sullivan
P.
Berger
A.L.
Spotila
J.A.
,
2008
,
Neogene exhumation of the Tordrillo Mountains, Alaska, and correlations with Denali (Mount McKinley)
, in
Freymueller
J.T.
et al
., eds.,
Active tectonics and seismic potential of Alaska: American Geophysical Union Geophysical Monograph 179
 , p.
269
285
,
doi:10.1029/179GM158
.
56.
Haeussler
P.J.
Armstrong
P.A.
Liberty
L.
Ferguson
K.
Finn
S.
Arkle
J.
Pratt
T.
,
2011
,
Focused exhumation along megathrust splay faults in Prince William Sound, Alaska
:
American Geophysical Union fall meeting, abs. T41A-06
 .
57.
Haeussler
P.J.
Finn
S.P.
Armstrong
P.A.
Arkle
J.C.
Liberty
L.M.
Pratt
T.L.
,
2014
,
Focused exhumation along megathrust splay faults in Prince William Sound, Alaska
:
Quaternary Science Reviews
 ,
doi:10.1016/j.quascirev.2014.10.013 (in press)
.
58.
Headley
R.M.
Enkelmann
E.
Hallet
B.
,
2013
,
Examination of the interplay between glacial processes and exhumation in the Saint Elias Mountains, Alaska
:
Geosphere
 , v.
9
, p.
229
241
,
doi:10.1130/GES00810.1
.
59.
Herman
F.
Seward
D.
Valla
P.G.
Carter
A.
Kohn
B.
Willett
S.D.
Ehlers
T.A.
,
2013
,
Worldwide acceleration of mountain erosion under a cooling climate
:
Nature
 , v.
504
, p.
423
426
,
doi:10.1038/nature12877
.
60.
Hilbert-Wolf
H.L.
,
2012
,
U/Pb detrital zircon provenance of the flysch of the Paleogene Orca Group, Chugach–Prince William terrane, Alaska
, in
Varga
R.
, ed.,
Proceedings of the Twenty-Fifth Keck Research Symposium in Geology, Amherst, Massachusetts
 :
Pomona College, Claremont, California
,
Keck Geology Consortium
, p.
23
32
.
61.
Huang
S.P.
Pollack
H.N.
Shen
P.Y.
,
2008
,
A late Quaternary climate reconstruction based on borehole heat flux data, borehole temperature data, and the instrumental record
:
Geophysical Research Letters
 , v.
35
,
L13703
,
doi:10.1029/2008GL034187
.
62.
House
M.A.
Gurnis
M.
Sutherland
R.
Kamp
P.J.J.
,
2005
,
Patterns of late Cenozoic exhumation deduced from apatite and zircon U-He ages from Fiordland, New Zealand
:
Geochemistry Geophysics Geosystems
 , v.
6
,
Q09013
,
doi:10.1029/2005GC000968
.
63.
Hudson
T.
Plafker
G.
Peterman
Z.E.
,
1979
,
Paleogene anatexis along the Gulf of Alaska margin
:
Geology
 , v.
7
, p.
573
577
,
doi:10.1130/0091-7613(1979)7<573:PAATGO>2.0.CO;2
.
64.
Idleman
B.
Trop
J.M.
Ridgway
K.D.
,
2011
,
Geochronological evidence for rapid forearc subsidence and sedimentation during Paleogene spreading ridge subduction along the southern Alaska convergent margin
:
Geological Society of America Abstracts with Programs
 , v.
43
, no.
5
, p.
439
.
65.
Ikari
M.J.
Saffer
D.M.
Marone
C.
,
2009
,
Frictional and hydrologic properties of clay-rich fault gouge
:
Journal of Geophysical Research
 , v.
114
,
B05409
,
doi:10.1029/2008JB006089
.
66.
Johnson
E.
,
2012
,
Origin of Late Eocene granitoids in western Prince William Sound, Alaska
, in
Varga
R.
, ed.,
Proceedings of the Twenty-Fifth Keck Research Symposium in Geology, Amherst, Massachusetts
 :
Pomona College, Claremont, California
,
Keck Geology Consortium
, p.
33
39
.
67.
Kame
N.
Rice
J.R.
Dmowska
R.
,
2003
,
Effects of pre-stress state and rupture velocity on dynamic fault branching
:
Journal of Geophysical Research
 , v.
108
,
2265
,
doi:10.1029/2002JB002189
.
68.
Kappelmeyer
G.
Haenel
R.
,
1974
,
Geothermics with special reference to application
:
Berlin
,
Gebruder Borntraege
,
238
p.
69.
Kaufman
D.S.
Manley
W.F.
,
2004
,
Pleistocene maximum and late Wisconsin glacier extents across Alaska, U.S.A.
, in
Ehlers
J.
Gibbard
P.L.
, eds.,
Quaternary glaciations—Extent and chronology, Part II: North America: Developments in Quaternary Science Volume 2
 :
Amsterdam
,
Elsevier
, p.
9
27
.
70.
Kveton
K.J.
,
1989
,
Structure, thermochronology, provenance and tectonic history of the Orca Group in southwestern Prince William Sound, Alaska [Ph.D. thesis]
:
Seattle
,
University of Washington
,
402
p.
71.
Lagoe
M.B.
Zellers
S.D.
,
1996
,
Depositional and microfaunal response to Pliocene climate change and tectonics in the eastern Gulf of Alaska
:
Marine Micropaleontology
 , v.
27
, p.
121
140
,
doi:10.1016/0377-8398(95)00055-0
.
72.
Lagoe
M.B.
Eyles
C.H.
Eyles
N.
Hale
C.
,
1993
,
Timing of late Cenozoic tidewater glaciation in the far North Pacific
:
Geological Society of America Bulletin
 , v.
105
, p.
1542
1560
,
doi:10.1130/0016-7606(1993)105<1542:TOLCTG>2.3.CO;2
.
73.
Liberty
L.M.
Finn
S.
,
2010
,
High resolution imaging of megathrust splay faults in Prince William Sound, Alaska, Department of Geosciences, Boise State University
,
U.S. Geological Survey Project Award G09AP00049
 ,
19
p.
74.
Liberty
L.M.
Finn
S.
Haeussler
P.J.
Pratt
T.
Peterson
A.
,
2013
,
Megathrust splay faults at the focus of the Prince William Sound asperity, Alaska
:
Journal of Geophysical Research
 , v.
118
, p.
5428
5441
,
doi:10.1002/jgrb.50372
.
75.
Little
T.
Naeser
C.
,
1989
,
Tertiary tectonics of the Border Ranges fault system, Chugach Mountains, Alaska: Deformation and uplift in a forearc setting
:
Journal of Geophysical Research
 , v.
94
, p.
4333
4359
,
doi:10.1029/JB094iB04p04333
.
76.
Madsen
J.K.
Thorkelson
D.J.
Friedman
R.M.
Marshall
D.D.
,
2006
,
Cenozoic to recent plate configurations in the Pacific Basin: Ridge subduction and slab window magmatism in western North America
:
Geosphere
 , v.
2
, p.
11
34
,
doi:10.1130/GES00020.1
.
77.
Malloy
R.J.
Merrill
G.F.
,
1972
,
Vertical crustal movement on the sea floor
, in
The great Alaska earthquake of 1964: Volume 6, Oceanography and Coastal Engineering
 :
Washington, D.C.
,
National Academy of Sciences
, p.
252
265
.
78.
Mancktelow
N.S.
Grasemann
B.
,
1997
,
Time-dependent effects of heat advection and topography on cooling histories during erosion
:
Tectonophysics
 , v.
270
, p.
167
195
,
doi:10.1016/S0040-1951(96)00279-X
.
79.
Mankhemthong
N.
Doser
D.I.
Pavlis
T.L.
,
2013
,
Interpretation of gravity and magnetic data and development of two-dimensional cross-sectional models for the Border Ranges fault system, south-central Alaska
:
Geosphere
 , v.
9
, p.
242
259
,
doi:10.1130/GES00833.1
.
80.
McAleer
R.J.
Spotila
J.A.
Enkleman
E.
Berger
A.L.
,
2009
,
Exhumation along the Fairweather fault, southeastern Alaska, based on low-temperature thermochronometry
:
Tectonics
 , v.
28
,
TC1007
,
doi:10.1029/2007TC002240
.
81.
Meigs
A.
Sauber
J.
,
2000
,
Southern Alaska as an example of the long-term consequences of mountain building under the influence of glaciers
:
Quaternary Science Reviews
 , v.
19
, p.
1543
1562
,
doi:10.1016/S0277-3791(00)00077-9
.
82.
Meigs
A.
Johnston
S.
Garver
J.
Spotila
J.
,
2008
,
Crustal-scale structural architecture, shortening, and exhumation of an active, eroding orogenic wedge (Chugach/St Elias Range, southern Alaska)
:
Tectonics
 , v.
27
,
TC4003
,
doi:10.1029/2007TC002168
.
83.
Moore
G.F.
Bangs
N.L.
Taira
A.
Kuramoto
S.
Pangborn
E.
Tobin
H.J.
,
2007
,
Three-dimensional splay fault geometry and implications for tsunami generation
:
Science
 , v.
318
, p.
1128
1131
,
doi:10.1126/science.1147195
.
84.
Naeser
C.W.
,
1979
,
Thermal history of sedimentary basins: Fission track dating of subsurface rocks
, in
Scholle
P.
Schluger
R.
, eds.,
Aspects of diagenesis: Society of Economic Paleontologists and Mineralogists Special Publication 26
 , p.
109
112
,
doi:10.2110/pec.79.26.0109
.
85.
Nelson
S.W.
Dumoulin
J.A.
Miller
M.L.
,
1985
,
Geologic map of the Chugach National Forest, Alaska
:
U.S. Geological Survey Miscellaneous Field Studies Map MF-1645-B
 ,
16
p., scale 1:250,000.
86.
O’Sullivan
P.B.
Plafker
G.
Murphy
J.M.
,
1997a
,
Apatite fission-track thermotectonic history of crystalline rocks in the northern St. Elias Mountains, Alaska
, in
Domoulin
J.A.
Gray
J.E.
, eds.,
Geological studies in Alaska by the U.S. Geological Survey, 1995: U.S. Geological Survey Professional Paper 1574
 , p.
283
293
.
87.
O’Sullivan
P.B.
Murphy
J.M.
Blythe
A.E.
,
1997b
,
Late Mesozoic and Cenozoic thermotectonic evolution of the central Brooks Range and adjacent North Slope foreland basin, Alaska: Including fission track results from the Trans-Alaska Crustal Transect (TACT)
:
Journal of Geophysical Research
 , v.
102
, no.
B9
, p.
20,821
20,845
,
doi:10.1029/96JB03411
.
88.
Park
J.O.
Tsuru
T.
Kodaira
S.
Cummins
P.R.
Kaneda
Y.
,
2002
,
Splay fault branching along the Nankai subduction zone
:
Science
 , v.
297
, p.
1157
1160
,
doi:10.1126/science.1074111
.
89.
Pavlis
T.L.
,
2013
,
Kinematic model for out-of-sequence thrusting: Motion of two ramp-flat faults and the production of upper plate duplex systems
:
Journal of Structural Geology
 , v.
51
, p.
132
143
,
doi:10.1016/j.jsg.2013.02.003
.
90.
Pavlis
T.L.
Chapman
J.B.
Bruhn
R.L.
Ridgway
K.
Worthington
L.L.
Gulick
S.P.S.
Spotila
J.
,
2012
,
Structure of the actively deforming fold-thrust belt of the St. Elias orogen with implications for glacial exhumation and three dimensional tectonic processes
:
Geosphere
 , v.
8
, p.
991
1019
,
doi:10.1130/GES00753.1
.
91.
Péwé
T.L.
,
1975
,
Quaternary geology of Alaska
:
U.S. Geological Survey Professional Paper 835
 , p.
B1
B145
, scale 1:500,000.
92.
Plafker
G.
,
1965
,
Tectonic deformation associated with the 1964 Alaska earthquake
:
Science
 , v.
148
, p.
1675
1687
,
doi:10.1126/science.148.3678.1675
.
93.
Plafker
G.
,
1967
,
Surface faults on Montague Island associated with the 1964 earthquake
, in
The Alaska earthquake, March 27, 1964: Regional effects: U.S. Geological Survey Professional Paper 543
 , p.
G1
G42
, 2 sheets, scales 1:31,680, ∼1:20,000.
94.
Plafker
G.
,
1969
,
Tectonics of the March 27, 1964 Alaska earthquake
, in
The Alaska earthquake, March 27, 1964: Regional effects: U.S. Geological Survey Professional Paper 543
 , p.
I1
I74
p., 2 sheets, scales 1:2,000,000, 1:500,000.
95.
Plafker
G.
,
1987
,
Regional geology and petroleum potential of the northern Gulf of Alaska continental margin
, in
Scholl
D.W.
et al
., eds.,
Geology and resource potential of the continental margin of western North America and adjacent ocean basins–Beaufort Sea to Baja California: Circum-Pacific Council for Energy and Mineral Resources Earth Sciences Series
 , v.
6
, p.
299
268
.
96.
Plafker
G.
Berg
H.C.
,
1994
,
Overview of the geology and tectonic evolution of Alaska
, in
Plafker
G.
Berg
H.C.
, eds.,
The geology of Alaska
 :
Boulder, Colorado
,
Geological Society of America, Geology of North America
, v.
G-1
, p.
989
1021
.
97.
Plafker
G.
Nokleberg
W.
Lull
J.
,
1989
,
Bedrock geology and tectonic evolution of the Wrangellia, Peninsular, and Chugach terranes along the Trans-Alaska Crustal Transect in the Chugach Mountains and southern Copper River Basin, Alaska
:
Journal of Geophysical Research
 , v.
94
, p.
4255
4295
,
doi:10.1029/JB094iB04p04255
.
98.
Plafker
G.
Moore
J.C.
Winkler
G.
,
1994
,
Geology of the southern Alaska margin
, in
Plafker
G.
Berg
H.C.
, eds.,
The geology of Alaska
 :
Boulder, Colorado
,
Geological Society of America, Geology of North America
, v.
G-1
, p.
389
449
.
99.
Plattner
C.
Malservisi
R.
Dixon
T.H.
LaFemina
P.
Sella
G.F.
Fletcher
J.
Suarez-Vidal
F.
,
2007
,
New constraints on relative motion between the Pacific plate and Baja California microplate (Mexico) from GPS measurements
:
Geophysical Journal International
 , v.
170
, p.
1373
1380
,
doi:10.1111/j.1365-246X.2007.03494.x
.
100.
Powell
W.G.
Chapman
D.S.
Balling
N.
Beck
A.E.
,
1988
,
Continental heat flow density
, in
Haenel
R.
et al
., eds.,
Handbook of terrestrial heat-flow density determinations
 :
Boston, Massachusetts
,
Kluwer Academic
, p.
167
222
.
101.
Ratchkovski
N.A.
Hansen
R.A.
,
2002
,
New evidence for segmentation of the Alaska subduction zone
:
Seismological Society of America Bulletin
 , v.
92
, p.
1754
1765
,
doi:10.1785/0120000269
.
102.
Reiners
P.W.
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
.
103.
Reiners
P.W.
Ehlers
T.A.
Mitchell
S.G.
Montgomery
D.R.
,
2003
,
Coupled spatial variations in precipitation and long-term erosion rates across the Washington Cascades
:
Nature
 , v.
426
, p.
645
647
,
doi:10.1038/nature02111
.
104.
Reiners
P.W.
Spell
T.L.
Nicolescu
S.
Zanetti
K.A.
,
2004
,
Zircon (U-Th)/He thermochronometry: He diffusion and comparisons with 40Ar/39Ar dating
:
Geochimica et Cosmochimica Acta
 , v.
68
, p.
1857
1887
,
doi:10.1016/j.gca.2003.10.021
.
105.
Spotila
J.A.
Berger
A.L.
,
2010
,
Exhumation at orogenic indentor corners under long-term glacial conditions: Example of the St. Elias orogen, southern Alaska
:
Tectonophysics
 , v.
490
, p.
241
256
,
doi:10.1016/j.tecto.2010.05.015
.
106.
Spotila
J.A.
Farley
K.A.
Sieh
K.
,
1998
,
Uplift and erosion of the San Bernardino Mountains associated with transpression along the San Andreas fault, California, as constrained by radiogenic helium thermochronometry
:
Tectonics
 , v.
17
, p.
360
378
,
doi:10.1029/98TC00378
.
107.
Spotila
J.A.
Buscher
J.T.
Meigs
A.J.
Reiners
P.W.
,
2004
,
Long-term glacial erosion of active mountain belts: Example of the Chugach–St. Elias Range, Alaska
:
Geology
 , v.
32
, p.
501
504
,
doi:10.1130/G20343.1
.
108.
Stüwe
K.
White
L.
Brown
R.
,
1994
,
The influence of eroding topography on steady-state isotherms. Application to fission track analysis
:
Earth and Planetary Science Letters
 , v.
124
, p.
63
74
,
doi:10.1016/0012-821X(94)00068-9
.
109.
Sutherland
R.
Gurnis
M.
Kamp
P.J.J.
House
M.A.
,
2009
,
Regional exhumation history of brittle crust during subduction initiation, Fiordland, southwest New Zealand, and implications for thermochronologic sampling and analysis strategies
:
Geosphere
 , v.
5
, p.
409
425
,
doi:10.1130/GES00225.SA2
.
110.
Tomkin
J.H.
,
2007
,
Coupling glacial erosion and tectonics at active orogens: A numerical modeling study
:
Journal of Geophysical Research
 , v.
112
,
F02015
,
doi:10.1029/2005JF000332
.
111.
Turcotte
D.
Schubert
G.
,
2002
,
Geodynamics (second edition)
:
Cambridge, UK
,
Cambridge University Press
,
472
p.
112.
Wagner
G.A.
Reimer
G.M.
,
1972
,
Fission track tectonics: The tectonic interpretation of fission track ages
:
Earth and Planetary Science Letters
 , v.
14
, p.
263
268
,
doi:10.1016/0012-821X(72)90018-0
.
113.
Willett
S.D.
Slingerland
R.
Hovius
N.
,
2001
,
Uplift, shortening, and steady state topography in active mountain belts
:
American Journal of Science
 , v.
301
, p.
455
485
,
doi:10.2475/ajs.301.4-5.455
.
114.
Worthington
L.L.
van Avendonk
H.J.A.
Gulick
S.P.S.
Christeson
G.L.
Pavlis
T.L.
,
2012
,
Crustal structure of the Yakutat terrane and the evolution of subduction and collision in southern Alaska
:
Journal of Geophysical Research
 , v.
117
,
B01102
,
doi:10.1029/2011JB008493
.
115.
Zellers
S.D.
,
1995
,
Foraminiferal sequence biostratigraphy and seismic stratigraphy of a tectonically active margin: The Yakataga Formation, northeastern Gulf of Alaska
:
Marine Micropaleontology
 , v.
26
, p.
255
271
,
doi:10.1016/0377-8398(95)00031-3
.
116.
Zweck
C.
Freymueller
J.T.
Cohen
S.C.
,
2002
,
Three-dimensional dislocation modeling of the postseismic response to the 1964 Alaska earthquake
:
Journal of Geophysical Research
 , v.
107
,
2064
,
doi:10.1029/2001JB000409
.