---
title: "Thrust Belts and Orogenic Wedges"
book: "University Earth and Space Sciences — Year 3"
subject: earth
language: en
chapter: 10
exercises: 12
source: https://one-course.com/books/earth/5/en/chapter/10-thrust-belts-and-orogenic-wedges
license: CC-BY-NC-SA-4.0
credit: "One Earth and Space Sciences Book, One Course (one-course.com)"
---

# Chapter 10 — Thrust Belts and Orogenic Wedges

Push a bulldozer into wet sand or snow, and a wedge of material piles up in front of the blade. It deforms until its surface reaches a certain slope; from then on it slides forward as a whole and grows at the same shape, taking in new material at its toe. The outer parts of mountain belts, from Taiwan to the foothills of the Alps, behave in the same way: they are wedges of rock scraped off a plate and pushed over a weak base, and their surface slope and the dip of their base tell how weak that base is and how high the pressure of the fluids within it. This chapter builds the geometry of thrust belts, the mechanics of the wedge, and the clocks that measure how fast its rocks come up to the surface.

**You already know.**

Thrusts, vergence and fold geometry are in the Year 1 volume, in its chapter on faults, folds and fabrics; the Coulomb criterion, Byerlee’s law, the effective stress and the pore-pressure ratio $\lambda = P/\sigma_v$ in its chapter on stress, strain and rheology; closure temperature and cooling age in its chapter on radiometric dating methods. The décollement, the fold-and-thrust belt, thin- and thick-skinned tectonics and the balanced cross-section are in the Year 2 volume, in its chapter on the anatomy of a mountain belt; exhumation and its rate in its chapter on P–T–t paths. The kink construction and the excess area $A = Sh$ of a fold above a detachment are in [Chapter 8](https://one-course.com/books/earth/5/en/chapter/8-structural-analysis#ch-b3-structural-analysis); the [thermal Péclet number](https://one-course.com/books/earth/5/en/chapter/5-thermal-models-of-the-lithosphere#def-b3-lithosphere-thermal-models-peclet) in [Chapter 5](https://one-course.com/books/earth/5/en/chapter/5-thermal-models-of-the-lithosphere#ch-b3-lithosphere-thermal-models).

## 10.1 The geometry of thrusts

A thrust does not cut through a layered sequence along one straight plane. It follows a weak layer, a shale or an evaporite, for long distances, then climbs steeply through the strong layers above to the next weak one. The staircase it draws controls the folds of the hanging wall.

**Definition 10.1 (Ramp, flat, duplex, out-of-sequence thrust).**

A *flat (thrust)* is a segment of a thrust that runs parallel to the bedding, usually in a weak layer; a *ramp (thrust)* is a segment that cuts across the bedding, typically at 20 to $30{}^{\circ}$, joining a lower flat to an upper one. A *duplex (thrust)* is a stack of fault-bounded slices, the horses, enclosed between a floor thrust below and a roof thrust above, each horse cut off by a ramp that joins the two. Thrusts usually form in sequence, each new one in the footwall of the previous one, closer to the foreland; an *out-of-sequence thrust* is one that forms or slips again behind the active front, cutting older thrusts.

As the hanging wall moves over a bend in the fault, it must fold to stay in contact with it: a syncline forms where it enters the ramp and an anticline where it leaves it.

**Definition 10.2 (Fault-bend, fault-propagation and detachment folds).**

A *fault-bend fold* is a fold of the hanging wall of a thrust produced as it slides over a bend of the fault, a ramp between two flats. A *fault-propagation fold* grows above the tip of a thrust that is still propagating upward: the shortening that the fault no longer carries is taken up by folding in front of its tip, which gives a steep or overturned forelimb. A *detachment fold* grows above a flat with no ramp: the shortening is taken up by folding and by a weak layer, salt or shale, that flows into its core.

The figure below builds a [fault-bend fold](#def-b3-orogenic-wedges-thrust-folds). Here the hanging wall moves parallel to the fault segment beneath it and folds at axial surfaces that bisect each bend, a kinematic model called fault-parallel flow; the classic model of constant layer thickness and length gives the same flat-topped anticline with a steeper forelimb, at the cost of a longer construction (admitted here). Both models are bound by the conservation of area.

![(a) A thrust with a lower flat, a ramp dipping 30 and an upper flat, before slip (schematic, vertical and horizontal scales equal). (b) The same after a slip of 2.5 times the ramp height, computed by fault-parallel flow: a syncline at the foot of the ramp, a back limb parallel to the ramp, a flat crest lifted by the ramp height r, a forelimb, and an excess area Sr above the regional level of every bed above the upper flat.](https://one-course.com/images/onecourse/chapters/earth-5/b3-orogenic-wedges/fig-e4bcdd341d2d.svg)

*(a) A thrust with a lower flat, a ramp dipping $30{}^{\circ}$ and an upper flat, before slip (schematic, vertical and horizontal scales equal). (b) The same after a slip of 2.5 times the ramp height, computed by fault-parallel flow: a syncline at the foot of the ramp, a back limb parallel to the ramp, a flat crest lifted by the ramp height $r$, a forelimb, and an excess area $Sr$ above the regional level of every bed above the upper flat.*

**Proposition 10.3 (Excess area of a fault-bend fold).**

Let a thrust carry its hanging wall up a ramp of height $r$ from a lower flat to an upper flat, with the slip $S$ on the lower flat. For any bed of the hanging wall that lies above the upper flat, the area enclosed between the folded bed and its original level is $A = Sr$, the same for every such bed.

**Proof.** Rock is neither created nor destroyed, and its volume is kept. Take a section parallel to the slip, bounded by two vertical lines far behind and far in front of the ramp. Through the rear line, the hanging wall between the lower flat and a bed at the height $y_0$ above it has moved in by $S$: the area $Sy_0$ has entered. Through the front line, the rock between the upper flat and the same bed, of thickness $y_0 - r$, has moved out by the slip on the upper flat, also $S$ when the rock keeps its area: the area $S(y_0 - r)$ has left. The difference, $Sr$, has stayed between the two lines, and lifts the bed above its original level. ∎

The excess area of a [fault-bend fold](#def-b3-orogenic-wedges-thrust-folds) measures the slip times the height of the ramp, not times the depth to the décollement, as it would for a [detachment fold](#def-b3-orogenic-wedges-thrust-folds) ([Chapter 8](https://one-course.com/books/earth/5/en/chapter/8-structural-analysis#ch-b3-structural-analysis)). The two kinds of fold must be told apart before an area is turned into shortening.

A duplex (the figure below) grows when the thrust, instead of carrying its hanging wall ever farther along the same ramp, abandons it and cuts a new ramp in its footwall, ahead of the old one. The slice between the old and the new ramp becomes a horse, carried up the new ramp and stacked beneath the roof; the next ramp forms ahead again. Each horse is shortened from its original length to the length it now occupies along the floor, and the shortening of the duplex is the sum over its horses. [Out-of-sequence thrusts](#def-b3-orogenic-wedges-thrust-geometry) cut this order: they form when the wedge behind the front must thicken, a case the mechanics of the next section predicts.

![A duplex (schematic): four horses (blue and green) cut off by ramps between a floor and a roof thrust, ahead of them the footwall not yet cut, the arrow giving the sense of transport; the cover above the roof is folded over the stack.](https://one-course.com/images/onecourse/chapters/earth-5/b3-orogenic-wedges/fig-6dfdb73d6e08.svg)

*A duplex (schematic): four horses (blue and green) cut off by ramps between a floor and a roof thrust, ahead of them the footwall not yet cut, the arrow giving the sense of transport; the cover above the roof is folded over the stack.*

## 10.2 The critical taper

A fold-and-thrust belt in cross-section is a wedge: thin at its front, where the décollement reaches the surface, and thickening towards the hinterland. Its upper surface slopes towards the foreland at the angle $\alpha$; its base, the décollement, dips towards the hinterland at the angle $\beta$. The taper of the wedge is the angle between them, $\alpha + \beta$.

**Definition 10.4 (Critical taper).**

The *critical taper* of a wedge pushed from behind over a base is the taper at which the wedge is everywhere on the verge of failure, inside and along its base, under horizontal compression. A wedge at its critical taper slides over its base without deforming internally; a wedge below it (subcritical) deforms and thickens until it reaches it; a wedge above it (supercritical) slides without deforming.

![A wedge of surface slope resting on a décollement of dip and pushed from behind; x is measured from the toe towards the hinterland. On a vertical slice, the push F(x + dx) from behind exceeds the push F(x) from the front by what the base takes: its friction _b and the horizontal part of its normal stress _n, which leans towards the hinterland on a base dipping that way (schematic, angles exaggerated).](https://one-course.com/images/onecourse/chapters/earth-5/b3-orogenic-wedges/fig-02fd0c7f4201.svg)

*A wedge of surface slope $\alpha$ resting on a décollement of dip $\beta$ and pushed from behind; $x$ is measured from the toe towards the hinterland. On a vertical slice, the push $F(x + \mathrm dx)$ from behind exceeds the push $F(x)$ from the front by what the base takes: its friction $\tau_b$ and the horizontal part of its normal stress $\sigma_n$, which leans towards the hinterland on a base dipping that way (schematic, angles exaggerated).*

**Theorem 10.5 (Critical-taper equation).**

Consider a subaerial wedge of uniform density $\rho$ made of cohesionless Coulomb material of internal friction $\mu = \tan\phi$, with the pore-pressure ratio $\lambda$, on a base of friction $\mu_b$ and pore-pressure ratio $\lambda_b$. If $\alpha$ and $\beta$ are small and $\sigma_1$ is horizontal, the *critical-taper equation* is

$$
\alpha + \beta = \frac{\beta + \mu_b(1 - \lambda_b)}{1 + K(1 - \lambda)},
  \qquad K = \frac{2\sin\phi}{1 - \sin\phi},
$$

with the angles in radians.

**Proof.** Let $z$ be the depth below the surface. With small slopes, the vertical stress is the weight of the rock above, $\sigma_{zz} = \rho g z$, and the pore pressure is $\lambda\rho g z$, so that the effective vertical stress is $(1 - \lambda)\rho g z$. Everywhere at failure with $\sigma_1$ horizontal, the Coulomb criterion for a cohesionless material gives the ratio of the effective principal stresses $\sigma'_1/\sigma'_3 = (1 + \sin\phi)/(1 -
\sin\phi) = 1 + K$, hence the total horizontal stress

$$
\sigma_{xx} = (1 + K)(1 - \lambda)\rho g z + \lambda\rho g z
  = \bigl(1 + K(1 - \lambda)\bigr)\rho g z .
$$

At the distance $x$ from the toe the wedge has the thickness $H = (\alpha +
\beta)x$, and the horizontal force per unit length of the belt on a vertical section is $F = \int_0^H \sigma_{xx}\,\mathrm dz = \bigl(1 + K(1 -
\lambda)\bigr)\rho g H^2/2$. On the slice between $x$ and $x + \mathrm dx$ (the figure above), the surface carries no stress and the push from behind exceeds the push from the front by $(\mathrm dF/\mathrm dx)\,\mathrm dx$. The base holds the slice back in two ways: the friction $\mu_b(1 -
\lambda_b)\rho g H$ per unit length, and its normal stress $\rho g H$, which is perpendicular to a base dipping $\beta$ towards the hinterland and so leans that way by $\beta$, giving the horizontal part $\beta\rho g H$. Equilibrium of the slice requires

$$
\bigl(1 + K(1 - \lambda)\bigr)\rho g H(\alpha + \beta)
  = \bigl(\beta + \mu_b(1 - \lambda_b)\bigr)\rho g H ,
$$

which is the equation. Since $H$ cancels, a wedge at failure keeps the same taper as it grows. ∎

The equation says, first, that the taper is set by the ratio of the strength of the base, in the numerator, to the strength of the wedge, in the denominator: a weak base gives a thin wedge, a strong base a thick one. Second, the surface slope falls as the base dips more steeply. Third, fluid pressure lowers the taper: raising $\lambda = \lambda_b$ takes from the strength of the base more, in proportion, than from the strength of the wedge. The figure below shows the critical surface slope for the friction coefficients fitted in western Taiwan. Points below each line are subcritical wedges, which thicken; points above are supercritical, which slide.

![Critical surface slope against basal dip for the friction coefficients of western Taiwan, = 1.03 inside and _b = 0.85 on the base, for three pore-pressure ratios = _b; “subcritical” and “supercritical” refer to the = 0.7 line. The shaded bands are the tapers of the Jura thrust wedge, 3 to 4, and of the wedge to its south, 12 to 13.](https://one-course.com/images/onecourse/chapters/earth-5/b3-orogenic-wedges/fig-f204eb42023d.svg)

*Critical surface slope against basal dip for the friction coefficients of western Taiwan, $\mu = 1.03$ inside and $\mu_b =
0.85$ on the base, for three pore-pressure ratios $\lambda = \lambda_b$; “subcritical” and “supercritical” refer to the $\lambda = 0.7$ line. The shaded bands are the tapers of the Jura thrust wedge, 3 to $4{}^{\circ}$, and of the wedge to its south, 12 to $13{}^{\circ}$.*

A wedge is not a static object: material is added to it and removed from it, and each change pushes it off its [critical taper](#def-b3-orogenic-wedges-critical-taper).

**Definition 10.6 (Frontal accretion, tectonic underplating).**

*Frontal accretion* is the addition of material to a wedge at its toe, as the décollement propagates into the undeformed sediments of the foreland and a new thrust slice is cut. *Tectonic underplating* is the addition of material to the base of the wedge, behind its toe, as slices of the lower plate are detached and stacked beneath it, often as duplexes.

[Frontal accretion](#def-b3-orogenic-wedges-accretion) lengthens the wedge at constant taper. Underplating thickens its rear and steepens its surface: the wedge becomes supercritical there and may extend by normal faulting until the taper falls back. Erosion does the opposite: it lowers the surface slope, the wedge becomes subcritical, and it thickens by out-of-sequence thrusting behind the front. Erosion and deformation are thus coupled: a wedge eroded fast keeps its taper by moving rock upward faster, and the rocks it brings to the surface are younger in the sense of the next section.

**In the lab — Sandbox models.**

![](https://one-course.com/images/onecourse/chapters/earth-5/b3-orogenic-wedges/img-15999da766ce.jpg)

*A sandbox model before shortening: coloured sand layers in a glass-sided box, a motor-driven wall at the left, a camera on a tripod (AI-generated illustration).*

In an analogue sandbox model, layers of dry sand of different colours are laid flat in a long glass-sided box. A motor slowly pushes a vertical wall into them, or pulls a sheet out from beneath them; a camera beside the glass photographs the section at regular steps. The sand fails along thrusts, grows a wedge that keeps a constant taper, and develops ramps, duplexes and back-thrusts like those of real belts. A layer of glass beads or of a silicone putty beneath the sand plays the part of a weak décollement, and the wedge then grows thinner and wider. Davis, Suppe and Dahlen found that their experiments with dry sand matched the critical-taper theory. Correlating the successive photographs gives the displacement field inside the model.

## 10.3 Real wedges

In the active fold-and-thrust belt of western Taiwan, the surface slope, the dip of the décollement and the pore pressures are all known, from topography, seismic sections and wells. Davis, Suppe and Dahlen used them to solve the [critical-taper equation](#thm-b3-orogenic-wedges-critical-taper) for the strength of the wedge and found $\mu = 1.03$ inside and $\mu_b = 0.85$ on the base: Byerlee’s friction on the base, and a wedge stronger than its own faults, because they are not all oriented to slip easily. With these two coefficients they turned the observed tapers of other active wedges, on land and under the sea, into pore-pressure ratios, and found them everywhere above hydrostatic, in line with drilling. They also found where the theory stops: the taper drops abruptly where wedges grow thicker than about $15\,\mathrm{km}$, the depth at which quartz-rich rocks become plastic for common geotherms, and the base no longer obeys a frictional law.

At the front of the western Alps, the Jura is a thrust wedge with a narrow angle of only 3 to $4{}^{\circ}$. Its décollement lies mostly in halite-bearing layers of Triassic age, and the fluids there are not overpressured: the weakness of salt alone explains the narrow taper. South of the Jura, where the Triassic layers hold no halite, the same front has a taper of 12 to $13{}^{\circ}$, with stacks of thrust slices, although fluid pressures measured there are high. In the Central Alps, critical-taper analysis of the surface slope gives a basal strength $\mu_b(1 - \lambda_b)$ (with a small cohesion term) below 0.1, and even 0.05 in evaporites and shales near the front, increasing towards the hinterland, with pore-pressure ratios above 0.54. The base of a wedge is often far weaker than Byerlee’s law would make it, by its rock type and by its fluids.

## 10.4 Flux through a wedge

A wedge at its [critical taper](#def-b3-orogenic-wedges-critical-taper) grows by accretion, at fixed shape: its length and height increase together. Erosion removes rock from its surface. When the two balance, the wedge keeps its size, and rock flows through it.

**Proposition 10.7 (Steady-state flux balance).**

A wedge of width $W$ along the transport direction receives, per unit length of the belt, the accretionary flux $F_a = v h$, where $v$ is the convergence rate and $h$ the thickness of the incoming layer above the décollement. It loses the erosional flux $F_e = \bar e W$, where $\bar e$ is the mean erosion rate over its surface. Its cross-sectional area changes at the rate $F_a -
F_e$; at steady state, $\bar e = vh/W$.

**Proof.** In unit time, a length $v$ of the incoming layer, of thickness $h$, passes into the wedge across its toe, and the thickness $e(x)$ is removed at each point of its surface; the area is conserved, so the area of the section changes by $vh - \int_0^W e\,\mathrm dx = F_a - F_e$. At steady state the change is zero. ∎

With $v = 10\,\mathrm{mm}/\mathrm{yr}$, $h = 4\,\mathrm{km}$ and $W = 60\,\mathrm{km}$, the erosion rate needed for steady state is $0.67\,\mathrm{mm}/\mathrm{yr}$. Exhumation in the sense of the Year 2 volume is the removal of the rock above a given rock: at steady state, rocks reach the surface at the rate at which erosion lowers it, and the wedge brings them up from depths where they were hot. Measuring how fast requires a clock that starts at a known temperature.

## 10.5 Thermochronology

**Definition 10.8 (Thermochronology, thermochronometer).**

*Thermochronology* is the use of radiometric cooling ages to date the time at which a rock passed through a given temperature, and so to reconstruct its thermal history. A *thermochronometer* is a pair of a mineral and a dating method with its closure temperature: for instance apatite with the (U–Th)/He method, or zircon with fission tracks.

The table below orders the main [thermochronometers](#def-b3-orogenic-wedges-thermochronology) by closure temperature; the depths assume a mean surface temperature of $10\,{}^{\circ}\mathrm{C}$ and a uniform gradient of $30\,{}^{\circ}\mathrm{C}/\mathrm{km}$. A rock that cools as it is exhumed passes them in turn, and its ages grow from the low-temperature methods to the high-temperature ones. The physics of fission tracks and of helium diffusion, which sets these temperatures, is in [Chapter 13](https://one-course.com/books/earth/5/en/chapter/13-advanced-geochronology#ch-b3-advanced-geochronology).

| [thermochronometer](#def-b3-orogenic-wedges-thermochronology) | closure temperature (${}^{\circ}\mathrm{C}$) | depth ($\mathrm{km}$) |
| --- | --- | --- |
| apatite (U–Th)/He | 50–80 | 1.3–2.3 |
| apatite fission track | 90–120 | 2.7–3.7 |
| zircon (U–Th)/He | 160–200 | 5.0–6.3 |
| zircon fission track | about 280 | 9 |
| 40Ar/39Ar on biotite | 350–400 | 11–13 |
| 40Ar/39Ar on muscovite | about 425 | 14 |
| U–Pb on zircon | above 900 | — |

These depths are only a first guess, because erosion changes the geotherm.

**Proposition 10.9 (Steady-state geotherm with erosion).**

Let rock rise at the constant speed $v$ through a layer of thickness $L$ whose surface ($z = 0$) is held at $T_s$ and base at $T_L$, with no heat production. The steady temperature is

$$
T(z) = T_s + (T_L - T_s)\,\frac{1 - e^{-\mathrm{Pe}\,z/L}}{1 - e^{-\mathrm{Pe}}},
  \qquad \mathrm{Pe} = \frac{vL}{\kappa},
$$

and the gradient at the surface is $\mathrm{Pe}/(1 - e^{-\mathrm{Pe}})$ times the conductive gradient $(T_L - T_s)/L$.

**Proof.** A rock particle at the depth $z$ moves upward, toward smaller $z$: the temperature it carries changes as $\partial T/\partial t - v\,\partial
T/\partial z$, and the diffusion equation becomes $\partial T/\partial t - v
T' = \kappa T''$. At steady state, $T'' = -(v/\kappa)T'$, so $T' = C
e^{-vz/\kappa}$ and $T = T_s + C(\kappa/v)(1 - e^{-vz/\kappa})$, which meets $T(0) = T_s$. Setting $T(L) = T_L$ fixes $C$ and gives the formula. At $z =
0$, $T' = (T_L - T_s)(\mathrm{Pe}/L)/(1 - e^{-\mathrm{Pe}})$. ∎

For $\mathrm{Pe} \ll 1$ the factor tends to 1: conduction wins and the geotherm stays straight. For $v = 1\,\mathrm{mm}/\mathrm{yr}$ across $30\,\mathrm{km}$, with $\kappa = 10^{-6}\,\mathrm{m}^{2}/\mathrm{s}$, $\mathrm{Pe} = 0.95$ and the surface gradient rises from 30 to $46\,{}^{\circ}\mathrm{C}/\mathrm{km}$: the isotherms crowd towards the surface and every [thermochronometer](#def-b3-orogenic-wedges-thermochronology) closes shallower.

**Definition 10.10 (Age–elevation relationship).**

The *age–elevation relationship* of a [thermochronometer](#def-b3-orogenic-wedges-thermochronology) is the plot of the cooling ages of samples collected over a range of elevations, usually along a steep slope or a vertical profile, against their elevations.

**Proposition 10.11 (Slope of the age–elevation relationship).**

Let rocks rise vertically at the constant speed $v$ under a steady topography, and let the closure isotherm lie at the elevation $e(x) = e_0 +
f\,h(x)$, where $h(x)$ is the surface elevation and $0 \le f < 1$. A sample collected at the surface at the elevation $h$ has the age $t = (h - e)/v$, and the [age–elevation relationship](#def-b3-orogenic-wedges-age-elevation) is a straight line of slope

$$
\frac{\mathrm dh}{\mathrm dt} = \frac{v}{1 - f}.
$$

With a flat isotherm, $f = 0$ and the slope is the exhumation rate.

**Proof.** The rock now at the surface at $x$ crossed the closure isotherm directly below, at the elevation $e(x)$, and has risen $h - e$ since, at the speed $v$: $t = (h - e_0 - fh)/v = ((1 - f)h - e_0)/v$. Hence $\mathrm dt/\mathrm dh =
(1 - f)/v$. ∎

![Steady exhumation under a sinusoidal relief of wavelength 20\, km and amplitude 1\, km, for three rates, line styles as in the legend of (b) (first-order model; layer 30\, km thick, surface at 10\, C, 30\, C/ km without erosion, = 10-6\, m2/ s, lapse rate 6.5\, C/ km, closure at 65\, C). (a) Age against elevation: the slopes are 0.59, 2.5 and 14\, mm/ yr, not 0.3, 1 and 3. (b) The 65\, C isotherm follows the topography more closely the faster the exhumation, as it rises nearer to the surface.](https://one-course.com/images/onecourse/chapters/earth-5/b3-orogenic-wedges/fig-07f742b8f471.svg)

*Steady exhumation under a sinusoidal relief of wavelength $20\,\mathrm{km}$ and amplitude $1\,\mathrm{km}$, for three rates, line styles as in the legend of (b) (first-order model; layer $30\,\mathrm{km}$ thick, surface at $10\,{}^{\circ}\mathrm{C}$, $30\,{}^{\circ}\mathrm{C}/\mathrm{km}$ without erosion, $\kappa = 10^{-6}\,\mathrm{m}^{2}/\mathrm{s}$, lapse rate $6.5\,{}^{\circ}\mathrm{C}/\mathrm{km}$, closure at $65\,{}^{\circ}\mathrm{C}$). (a) Age against elevation: the slopes are 0.59, 2.5 and $14\,\mathrm{mm}/\mathrm{yr}$, not 0.3, 1 and 3. (b) The $65\,{}^{\circ}\mathrm{C}$ isotherm follows the topography more closely the faster the exhumation, as it rises nearer to the surface.*

Isotherms are not flat beneath a relief: the surface is colder on the peaks than in the valleys, by the atmospheric lapse rate, but much less so than the rock would be at the same elevation underground, and the shallow isotherms follow the topography in a subdued way. For a sinusoidal topography of wavelength $\Lambda$ and a lapse rate $\Gamma$, a first-order solution of the steady equation gives

$$
f = \frac{(G_0 - \Gamma)\,e^{-mz_c}}{G(z_c)},\qquad
  m = \frac{v}{2\kappa} + \sqrt{\Bigl(\frac{v}{2\kappa}\Bigr)^2 +
  \Bigl(\frac{2\pi}{\Lambda}\Bigr)^2},
$$

where $z_c$ is the depth of the closure isotherm below the mean surface, $G_0$ the surface gradient and $G(z_c)$ the gradient at $z_c$ (admitted; the script tests it). The perturbation dies away with depth over the distance $1/m$, at most $\Lambda/2\pi$: low-temperature [thermochronometers](#def-b3-orogenic-wedges-thermochronology), which close shallow, feel the relief most. The figure above shows the effect for apatite (U–Th)/He.

An age–elevation profile measures the exhumation rate only where the closure isotherm is flat beneath the relief. Elsewhere it overestimates it, by the factor $1/(1 - f)$, which reaches two or more for apatite (U–Th)/He in a relief of $20\,\mathrm{km}$ wavelength. Ages from several [thermochronometers](#def-b3-orogenic-wedges-thermochronology) on the same samples, and thermal models of the relief, correct for it.

## 10.6 Exercises

**Exercise 10.1 ★.**

Compute $K$ and the ratio $\sigma'_1/\sigma'_3$ at failure for a wedge with $\phi = 30{}^{\circ}$.

**Solution of Exercise 10.1.**

$\sin30{}^{\circ} = 0.5$: $K = 2\times0.5/0.5 = 2$ and $\sigma'_1/\sigma'_3 = 1 +
K = 3$.

**Exercise 10.2 ★.**

A sandbox wedge of dry sand ($\lambda = \lambda_b = 0$) has $\mu = 0.6$ inside and $\mu_b = 0.3$ on its base. Compute its critical surface slope on a horizontal base, then on a base dipping $3{}^{\circ}$.

**Solution of Exercise 10.2.**

$\phi = \arctan0.6 = 31.0{}^{\circ}$, $\sin\phi = 0.514$, $K = 2.12$. On a horizontal base, $\alpha = 0.3/3.12 = 0.0962\,\mathrm{rad} = 5.5{}^{\circ}$. On a base dipping $3{}^{\circ} = 0.0524\,\mathrm{rad}$, $\alpha + \beta = 0.352/3.12 =
0.113\,\mathrm{rad} = 6.5{}^{\circ}$, so $\alpha = 3.5{}^{\circ}$.

**Exercise 10.3 ★.**

With a surface at $10\,{}^{\circ}\mathrm{C}$ and a gradient of $30\,{}^{\circ}\mathrm{C}/\mathrm{km}$, check the depths of the table of closure temperatures for apatite (U–Th)/He, apatite fission track and zircon fission track. Which [thermochronometer](#def-b3-orogenic-wedges-thermochronology) would you use to date exhumation from $5\,\mathrm{km}$?

**Solution of Exercise 10.3.**

Depth $= (T - 10)/30$: apatite (U–Th)/He 1.3 to $2.3\,\mathrm{km}$; apatite fission track 2.7 to $3.7\,\mathrm{km}$; zircon fission track $270/30 = 9.0\,\mathrm{km}$. At $5\,\mathrm{km}$ the rock was at $10 + 150 = 160\,{}^{\circ}\mathrm{C}$: zircon (U–Th)/He, which closes at 160 to $200\,{}^{\circ}\mathrm{C}$, 5.0 to $6.3\,\mathrm{km}$ deep.

**Exercise 10.4 ★.**

A ramp $2\,\mathrm{km}$ high dips $30{}^{\circ}$. Compute its horizontal length and its length along the dip. By how much is a bed of the hanging wall lifted once it has crossed the whole ramp, and what slip brings the cut-off of the lowest bed from the foot of the ramp to the upper flat?

**Solution of Exercise 10.4.**

Horizontal length $2/\tan30{}^{\circ} = 3.46\,\mathrm{km}$; along the dip $2/\sin30{}^{\circ} = 4.0\,\mathrm{km}$. The bed is lifted by the ramp height, $2\,\mathrm{km}$. The cut-off must travel the whole ramp: a slip of $4.0\,\mathrm{km}$.

**Exercise 10.5 ★★.**

With the Taiwan coefficients, compute the critical surface slope on a base dipping $6{}^{\circ}$ for $\lambda = \lambda_b = 0.4$ and $0.9$. What does an increase of the fluid pressure do to a wedge that was at its [critical taper](#def-b3-orogenic-wedges-critical-taper)?

**Solution of Exercise 10.5.**

$\phi = \arctan1.03 = 45.8{}^{\circ}$, $K = 5.08$; $\beta = 0.105\,\mathrm{rad}$. For $\lambda = 0.4$: $\alpha + \beta = (0.105 + 0.85\times0.6)/(1 +
5.08\times0.6) = 0.615/4.05 = 0.152\,\mathrm{rad} = 8.7{}^{\circ}$, $\alpha =
2.7{}^{\circ}$. For $\lambda = 0.9$: $0.190/1.51 = 0.126\,\mathrm{rad} = 7.2{}^{\circ}$, $\alpha = 1.2{}^{\circ}$. Raising the fluid pressure lowers the [critical taper](#def-b3-orogenic-wedges-critical-taper): the wedge becomes supercritical, slides forward on its base without thickening, and its front advances until accretion and erosion bring it back to the new taper.

**Exercise 10.6 ★★.**

A [fault-bend fold](#def-b3-orogenic-wedges-thrust-folds) lies above a ramp $1.5\,\mathrm{km}$ high; a bed above the upper flat shows an excess area of $6.0\,\mathrm{km}^{2}$. Compute the slip. A colleague reads the same fold as a [detachment fold](#def-b3-orogenic-wedges-thrust-folds), the bed lying $3.0\,\mathrm{km}$ above the décollement. What shortening would he find?

**Solution of Exercise 10.6.**

$S = A/r = 6.0/1.5 = 4.0\,\mathrm{km}$. Read as a [detachment fold](#def-b3-orogenic-wedges-thrust-folds), $S = A/h =
6.0/3.0 = 2.0\,\mathrm{km}$: half the true value. The two readings must be told apart by the shape of the fold and the presence of a ramp.

**Exercise 10.7 ★★.**

Take $\mu = 0.6$ inside both the Jura wedge (taper $3.5{}^{\circ}$) and the wedge to its south (taper $12.5{}^{\circ}$), a hydrostatic $\lambda = 0.4$ inside both, and a basal dip of $2{}^{\circ}$ for both. Compute the basal strength $\mu_b(1 -
\lambda_b)$ that each taper requires, and compare it with Byerlee’s $0.85$ at hydrostatic pressure. Is the result consistent with the décollement in halite beneath the Jura?

**Solution of Exercise 10.7.**

$K = 2.12$ and $1 + K(1 - 0.4) = 2.27$. The equation gives $\mu_b(1 -
\lambda_b) = (\alpha + \beta)\times2.27 - \beta$, with $\beta =
0.0349\,\mathrm{rad}$. Jura: $0.0611\times2.27 - 0.0349 = 0.10$. South: $0.218\times2.27 - 0.0349 = 0.46$. Byerlee at hydrostatic pressure: $0.85\times0.6 = 0.51$. The base to the south is close to Byerlee’s; the Jura base is almost five times weaker, as expected of a décollement in halite, whose friction is low, under fluids that are not overpressured.

**Exercise 10.8 ★★.**

Rock rises at $1\,\mathrm{mm}/\mathrm{yr}$ through a layer $30\,\mathrm{km}$ thick, from $910\,{}^{\circ}\mathrm{C}$ at its base to $10\,{}^{\circ}\mathrm{C}$ at the surface, with $\kappa = 10^{-6}\,\mathrm{m}^{2}/\mathrm{s}$. Compute the Péclet number, the surface gradient, and the depth of the $65\,{}^{\circ}\mathrm{C}$ isotherm. Compare with the depth without erosion.

**Solution of Exercise 10.8.**

$\kappa = 10^{-6}\,\mathrm{m}^{2}/\mathrm{s} = 31.6\,\mathrm{km}^{2}/\mathrm{Myr}$, and $v =
1\,\mathrm{km}/\mathrm{Myr}$: $\mathrm{Pe} = 30/31.6 = 0.951$. The factor $0.951/(1 -
e^{-0.951}) = 1.55$ raises the gradient from 30 to $46.5\,{}^{\circ}\mathrm{C}/\mathrm{km}$. For $65\,{}^{\circ}\mathrm{C}$: $1 - e^{-\mathrm{Pe}\,z/L} = (55/900)(1 - e^{-0.951})
= 0.0375$, so $\mathrm{Pe}\,z/L = 0.0382$ and $z = 1.21\,\mathrm{km}$, against $55/30 = 1.83\,\mathrm{km}$ without erosion.

**Exercise 10.9 ★★.**

Two samples from the same slope, at 1200 and $2000\,\mathrm{m}$, have apatite (U–Th)/He ages of 3.4 and $4.6\,\mathrm{Myr}$. Compute the apparent exhumation rate. A thermal model of the relief gives $f = 0.5$: what is the true rate?

**Solution of Exercise 10.9.**

$\mathrm dh/\mathrm dt = 0.8\,\mathrm{km}/1.2\,\mathrm{Myr} = 0.67\,\mathrm{mm}/\mathrm{yr}$. With $f = 0.5$, $v = 0.67\times(1 - 0.5) = 0.33\,\mathrm{mm}/\mathrm{yr}$.

**Exercise 10.10 ★★★.**

Show that, for $\lambda = \lambda_b$, the critical surface slope vanishes at a basal dip $\beta^* = \mu_b/K$ that does not depend on $\lambda$. Compute it for Taiwan. What happens to a wedge whose base dips more steeply?

**Solution of Exercise 10.10.**

With $\alpha = 0$ and $u = 1 - \lambda$: $\beta(1 + Ku) = \beta + \mu_b u$, so $\beta Ku = \mu_b u$ and $\beta^* = \mu_b/K$, whatever $u$. For Taiwan, $0.85/5.08 = 0.167\,\mathrm{rad} = 9.6{}^{\circ}$. On a steeper base, the critical surface slope is negative: any wedge with a level or foreland-sloping surface is already supercritical, and it slides on its base without thickening. A thrust belt cannot grow its normal shape there.

**Exercise 10.11 ★★★.**

Show that, for a very long wavelength and a very slow exhumation, $f$ tends to $1 - \Gamma/G$, where $G$ is the uniform gradient; evaluate it for $G =
30\,{}^{\circ}\mathrm{C}/\mathrm{km}$ and $\Gamma = 6.5\,{}^{\circ}\mathrm{C}/\mathrm{km}$. What is then the slope of the [age–elevation relationship](#def-b3-orogenic-wedges-age-elevation)? For $v = 1\,\mathrm{mm}/\mathrm{yr}$ and the values of exercise 8 ($z_c = 1.21\,\mathrm{km}$, $G_0 = 46.5\,{}^{\circ}\mathrm{C}/\mathrm{km}$, $G(z_c) = 44.7\,{}^{\circ}\mathrm{C}/\mathrm{km}$), compute $f$ for wavelengths of 5 and $20\,\mathrm{km}$.

**Solution of Exercise 10.11.**

As $\Lambda \to \infty$ and $v \to 0$, $m \to 0$, so $e^{-mz_c} \to 1$, and the geotherm is straight, $G_0 = G(z_c) = G$: $f \to (G - \Gamma)/G = 1 -
\Gamma/G = 1 - 6.5/30 = 0.78$. The slope is then $v/(1 - f) = vG/\Gamma =
4.6v$. For $v = 1\,\mathrm{mm}/\mathrm{yr}$, $v/2\kappa = 0.0158\,\mathrm{km}^{-1}$. At $5\,\mathrm{km}$: $m = 0.0158 + \sqrt{0.0158^2 + 1.257^2} = 1.273\,\mathrm{km}^{-1}$, $e^{-1.273\times1.21} = 0.215$, $f = 40.0\times0.215/44.7 = 0.19$. At $20\,\mathrm{km}$: $m = 0.0158 + 0.3146 = 0.330\,\mathrm{km}^{-1}$, $e^{-0.399} =
0.671$, $f = 40.0\times0.671/44.7 = 0.60$.

**Exercise 10.12 ★★★.**

A wedge grows at its [critical taper](#def-b3-orogenic-wedges-critical-taper) $\alpha + \beta$ by [frontal accretion](#def-b3-orogenic-wedges-accretion) alone, without erosion, from the flux $F_a$. Show that its width grows as $W = \sqrt{2F_at/\tan(\alpha + \beta)}$. With $F_a = 40\,\mathrm{km}^{2}/\mathrm{Myr}$ and a taper of $6{}^{\circ}$, how wide is it after $2\,\mathrm{Myr}$, and how long does it take to reach $60\,\mathrm{km}$?

**Solution of Exercise 10.12.**

The section is a triangle of base $W$ and height $W\tan(\alpha + \beta)$: $A = W^2\tan(\alpha + \beta)/2$. With $\mathrm dA/\mathrm dt = F_a$ and $A =
0$ at $t = 0$, $A = F_at$, which gives $W$. With $\tan6{}^{\circ} = 0.105$: $W = \sqrt{2\times40\times2/0.105} = 39\,\mathrm{km}$ after $2\,\mathrm{Myr}$; $t =
60^2\times0.105/(2\times40) = 4.7\,\mathrm{Myr}$ to reach $60\,\mathrm{km}$.

## 10.7 Problem: The Front of the Kestrel Wedge

**Problem 10.1.**

Weekend problem — the shortening, mechanics, flux and exhumation of an invented thrust wedge

The Kestrel Range is the invented front of a mountain belt, a subaerial fold-and-thrust belt $60\,\mathrm{km}$ wide pushed at $10\,\mathrm{mm}/\mathrm{yr}$ over a foreland whose sedimentary layer is $4.0\,\mathrm{km}$ thick above a shale décollement. Its frontal thrust follows the décollement $4.5\,\mathrm{km}$ below the surface, climbs a ramp dipping $25{}^{\circ}$ and runs along an upper flat $1.5\,\mathrm{km}$ deep. At the front the surface stands $0.3\,\mathrm{km}$ above sea level and the décollement $4.0\,\mathrm{km}$ below it; $60\,\mathrm{km}$ behind the front the surface stands at $2.4\,\mathrm{km}$ and the décollement lies $8.2\,\mathrm{km}$ below sea level. Take, as in Taiwan, $\mu = 1.03$ and $\mu_b =
0.85$, a rock density of $2500\,\mathrm{kg}/\mathrm{m}^{3}$, water at $1000\,\mathrm{kg}/\mathrm{m}^{3}$ and $g = 9.81\,\mathrm{m}/\mathrm{s}^{2}$.

**Part I — Thrust geometry.**

1. Compute the height of the ramp, its horizontal length and its length along the dip.
2. By how much has a bed of the hanging wall been lifted once it has crossed the whole ramp?
3. Above the ramp, a bed lying above the upper flat shows an excess area of $16.5\,\mathrm{km}^{2}$ above its regional level. Compute the slip.
4. What excess area do you predict for a shallower bed? Had the fold been read as a [detachment fold](#def-b3-orogenic-wedges-thrust-folds) over the décollement, with the bed $4.0\,\mathrm{km}$ above it, what shortening would have been found?
5. Behind the ramp, a seismic section shows a duplex of four horses, each now $2.5\,\mathrm{km}$ long along the floor thrust, cut from slices $6.0\,\mathrm{km}$ long. Compute the shortening taken up by the horses, and compare it with the slip on the frontal ramp.
6. The horses formed in sequence. Which is the youngest, and why is the roof thrust folded?

**Part II — The taper.**

7. Compute the surface slope $\alpha$ , the basal dip $\beta$ and the taper.
8. Compute the thickness of the wedge $60\,\mathrm{km}$ behind the front. Can the Coulomb wedge theory be used?
9. Compute $K$ . What surface slope would a dry wedge have on this base?
10. What surface slope would it have with hydrostatic fluid pressure in the wedge and on its base? Is the wedge consistent with it?
11. Solve the [critical-taper equation](#thm-b3-orogenic-wedges-critical-taper) for $\lambda = \lambda_b$ .
12. Compute the vertical stress, the fluid pressure and the hydrostatic pressure at the base of the wedge $60\,\mathrm{km}$ behind the front.
13. Drainage lowers $\lambda$ to 0.7. Compute the new critical surface slope. How does the wedge respond?

**Part III — The flux.**

14. Compute the accretionary flux per kilometre of the belt.
15. What mean erosion rate keeps the wedge at steady state?
16. Compute the volume and the mass of rock eroded per year from $100\,\mathrm{km}$ of the belt.
17. If erosion stopped, how fast would the wedge widen at first?
18. If half the incoming layer were underplated beneath the rear of the wedge instead of accreted at its front, would the steady-state mean erosion rate change? Where would erosion concentrate?

**Part IV — The clock.** Take the layer $30\,\mathrm{km}$ thick, $10\,{}^{\circ}\mathrm{C}$ at the mean surface ($2.0\,\mathrm{km}$ above sea level) and $910\,{}^{\circ}\mathrm{C}$ at its base, $\kappa
= 10^{-6}\,\mathrm{m}^{2}/\mathrm{s}$, a closure temperature of $65\,{}^{\circ}\mathrm{C}$ for apatite (U–Th)/He, a lapse rate of $6.5\,{}^{\circ}\mathrm{C}/\mathrm{km}$ and a relief of wavelength $20\,\mathrm{km}$. Five samples collected on one valley side give:

| elevation ($\mathrm{km}$) | 1.30 | 1.65 | 2.00 | 2.35 | 2.70 |
| --- | --- | --- | --- | --- | --- |
| apatite (U–Th)/He age ($\mathrm{Myr}$) | 1.60 | 1.83 | 2.07 | 2.30 | 2.54 |

19. With the erosion rate of question 15 as the exhumation rate, compute the Péclet number and the surface gradient.
20. Compute the depth of the closure isotherm below the mean surface and the gradient there.
21. With a flat closure isotherm, what age would a sample at the mean elevation have? Compare with the data.
22. Compute $m$ and the deflection factor $f$ .
23. Fit a straight line to the age–elevation data. What apparent exhumation rate does its slope give?
24. Correct it for the deflection of the isotherm.
25. Compare with Part III, and give the exhumation rate of the Kestrel wedge.

**Solution of Problem 10.1.**

**1.** $4.5 - 1.5 = 3.0\,\mathrm{km}$ high; $3.0/\tan25{}^{\circ} =
6.43\,\mathrm{km}$ long horizontally; $3.0/\sin25{}^{\circ} = 7.10\,\mathrm{km}$ along the dip.

**2.** By the ramp height, $3.0\,\mathrm{km}$.

**3.** $S = A/r = 16.5/3.0 = 5.5\,\mathrm{km}$.

**4.** The same, $16.5\,\mathrm{km}^{2}$: in a [fault-bend fold](#def-b3-orogenic-wedges-thrust-folds) the excess area of every bed above the upper flat is $Sr$. As a [detachment fold](#def-b3-orogenic-wedges-thrust-folds), $16.5/4.0 =
4.1\,\mathrm{km}$: a quarter too little.

**5.** $4\times(6.0 - 2.5) = 14.0\,\mathrm{km}$, two and a half times the $5.5\,\mathrm{km}$ of slip on the frontal ramp.

**6.** The frontal horse, the one nearest the foreland: each new ramp forms in the footwall ahead of the last. Each horse, carried up its ramp, lifts the roof thrust and the cover above it as a [fault-bend fold](#def-b3-orogenic-wedges-thrust-folds) lifts its hanging wall, so the roof is folded over the stack.

**7.** $\alpha = \arctan(2.1/60) = 2.00{}^{\circ}$; $\beta =
\arctan(4.2/60) = 4.00{}^{\circ}$; taper $6.0{}^{\circ}$.

**8.** $2.4 + 8.2 = 10.6\,\mathrm{km}$, less than about $15\,\mathrm{km}$: the base is still frictional, and the Coulomb theory applies.

**9.** $\phi = 45.8{}^{\circ}$, $\sin\phi = 0.717$, $K = 5.08$. Dry: $\alpha + \beta = (0.0699 + 0.85)/6.08 = 0.151\,\mathrm{rad} = 8.7{}^{\circ}$, $\alpha = 4.7{}^{\circ}$.

**10.** $\lambda = 1000/2500 = 0.40$: $(0.0699 + 0.51)/4.05 =
0.143\,\mathrm{rad} = 8.2{}^{\circ}$, $\alpha = 4.2{}^{\circ}$. The observed $2.0{}^{\circ}$ would make the wedge strongly subcritical, thickening rather than advancing: the fluids must be overpressured.

**11.** With $T = 0.1049\,\mathrm{rad}$ and $u = 1 - \lambda$, $T(1 + Ku) =
\beta + \mu_bu$ gives $u = (\beta - T)/(TK - \mu_b) = (0.0699 -
0.1049)/(0.5327 - 0.85) = 0.110$: $\lambda = 0.89$.

**12.** $\sigma_v = 2500\times9.81\times10\,600 = 260\,\mathrm{MPa}$; $P =
0.89\times260 = 231\,\mathrm{MPa}$; hydrostatic $1000\times9.81\times10\,600 =
104\,\mathrm{MPa}$. The fluids carry $127\,\mathrm{MPa}$ more than a column of water would.

**13.** $(0.0699 + 0.85\times0.3)/(1 + 5.08\times0.3) = 0.325/2.52 =
0.129\,\mathrm{rad} = 7.4{}^{\circ}$, $\alpha = 3.4{}^{\circ}$. The wedge, at $2.0{}^{\circ}$, is now subcritical: it stops advancing and thickens by out-of-sequence thrusting behind its front until its surface slope reaches $3.4{}^{\circ}$.

**14.** $F_a = 10\,\mathrm{km}/\mathrm{Myr}\times4.0\,\mathrm{km} = 40\,\mathrm{km}^{2}/\mathrm{Myr}$, that is $4.0 \times 10^{4}\,\mathrm{m}^{3}/\mathrm{yr}$ per kilometre of the belt.

**15.** $\bar e = 40/60 = 0.67\,\mathrm{km}/\mathrm{Myr} = 0.67\,\mathrm{mm}/\mathrm{yr}$.

**16.** $40\times100 = 4000\,\mathrm{km}^{3}/\mathrm{Myr} = 4.0 \times 10^{6}\,\mathrm{m}^{3}/\mathrm{yr}$, or $1.0 \times 10^{10}\,\mathrm{kg}/\mathrm{yr}$ (10 million tonnes a year).

**17.** $\mathrm dW/\mathrm dt = F_a/(W\tan(\alpha + \beta)) =
40/(60\times0.105) = 6.3\,\mathrm{km}/\mathrm{Myr}$.

**18.** No: at steady state the erosion must still remove the whole incoming flux, so the mean rate stays $0.67\,\mathrm{mm}/\mathrm{yr}$. But the rock added beneath the rear is lifted there: erosion and exhumation would be fastest over the rear, where the youngest cooling ages would be found.

**19.** $v = 0.667\,\mathrm{km}/\mathrm{Myr}$: $\mathrm{Pe} = 0.667\times30/31.6 =
0.634$; $G_0 = 30\times0.634/(1 - e^{-0.634}) = 30\times1.35 =
40.5\,{}^{\circ}\mathrm{C}/\mathrm{km}$.

**20.** $1 - e^{-\mathrm{Pe}\,z/L} = (55/900)(1 - e^{-0.634}) = 0.0287$, so $\mathrm{Pe}\,z/L = 0.0291$ and $z_c = 1.38\,\mathrm{km}$; $G(z_c) =
40.5\,e^{-0.0291} = 39.3\,{}^{\circ}\mathrm{C}/\mathrm{km}$.

**21.** $1.38/0.667 = 2.07\,\mathrm{Myr}$, the age of the sample at $2.00\,\mathrm{km}$: at the mean elevation the deflection of the isotherm is zero.

**22.** $v/2\kappa = 0.667/63.1 = 0.0106\,\mathrm{km}^{-1}$, $2\pi/\Lambda =
0.314\,\mathrm{km}^{-1}$: $m = 0.0106 + 0.3143 = 0.325\,\mathrm{km}^{-1}$; $e^{-0.325\times1.38} = 0.639$; $f = (40.5 - 6.5)\times0.639/39.3 = 0.552$.

**23.** The mean elevation is $2.00\,\mathrm{km}$ and the mean age $2.068\,\mathrm{Myr}$; $\sum\Delta t\,\Delta h = 0.823$ and $\sum\Delta t^2 =
0.552$, so the slope is $1.49\,\mathrm{km}/\mathrm{Myr}$: an apparent rate of $1.49\,\mathrm{mm}/\mathrm{yr}$.

**24.** $v = 1.49\times(1 - 0.552) = 0.667\,\mathrm{mm}/\mathrm{yr}$.

**25.** The [thermochronometer](#def-b3-orogenic-wedges-thermochronology) and the flux balance agree: the wedge is at steady state, and taking the apparent slope at face value would have overestimated the rate more than twofold. The exhumation rate of the Kestrel wedge is **$0.67\,\mathrm{mm}/\mathrm{yr}$**.