---
title: "Planetary Atmospheres and Habitability"
book: "University Earth and Space Sciences — Year 3"
subject: earth
language: en
chapter: 27
exercises: 12
source: https://one-course.com/books/earth/5/en/chapter/27-planetary-atmospheres-and-habitability
license: CC-BY-NC-SA-4.0
credit: "One Earth and Space Sciences Book, One Course (one-course.com)"
---

# Chapter 27 — Planetary Atmospheres and Habitability

Venus and the Earth are near twins: almost the same size, similar mean densities, neighbouring orbits. Yet Venus keeps $92\,\mathrm{bar}$ of carbon dioxide over a surface at $737\,\mathrm{K}$, and so little water that, spread over its surface, it would make a layer about a centimetre deep. The mass spectrometer of the Pioneer Venus probe, falling through its clouds, measured the ratio of deuterium to hydrogen in that water: $0.016$, a hundred times the ratio in the Earth’s oceans. Light hydrogen escapes to space more easily than heavy deuterium; what is left of a large reservoir that has lost most of its hydrogen is rich in deuterium. The ratio is the trace of water that Venus once had, and lost. This chapter asks how a planet holds on to its air and its water, and how it loses them.

**You already know.**

The scale height, the barometric formula, the Maxwell–Boltzmann distribution, the escape velocity, the mean free path and the greenhouse effect are in the physics books. The habitable zone of a star is in the school books. The equilibrium temperature and the Bond albedo are in the Year 1 volume, in its chapter on comparative planetology; the optical depth, in its chapter on telescopes and photometry; the lapse rates, in its chapter on the structure of the atmosphere and the ocean; the outgoing longwave radiation (OLR) and the emission temperature, in its chapter on radiation and heat transport. The moist adiabat is in the Year 2 volume, in its chapter on atmospheric thermodynamics; the snow line, in its chapter on planet formation; the long-term carbon cycle and the silicate-weathering thermostat, in its chapter on climate over geological time. [Rayleigh distillation](https://one-course.com/books/earth/5/en/chapter/14-stable-isotope-geochemistry#prop-b3-stable-isotopes-rayleigh-distillation) is in this volume, in its chapter on stable isotopes.

## 27.1 The structure of an atmosphere

An isothermal atmosphere of molecular mass $m$ at temperature $T$ thins with height as $p = p_0\,e^{-z/H}$, with the scale height $H = kT/mg$. At the surface of the Earth $H$ is about $8\,\mathrm{km}$; at the surface of Titan, where gravity is weak and the air cold, about $20\,\mathrm{km}$.

The temperature, though, is not uniform. Sunlight that reaches the ground warms it; the air above, which absorbs and emits in the infrared, is warmed from below. Radiation alone would make the lower atmosphere so steep in temperature that it would overturn.

**Definition 27.1 (Radiative–convective equilibrium).**

A column of atmosphere is in *radiative–convective equilibrium* when, at every level, the net flux of radiation is balanced, except in a lower layer where convection carries heat upwards and holds the temperature gradient at the adiabatic one. The lower, convective layer is the troposphere; the upper layer, in radiative equilibrium, the stratosphere; the tropopause is the level where they meet.

The simplest atmosphere in which this can be followed is *grey*: it is transparent to sunlight and absorbs every infrared wavelength alike, with an optical depth $\tau$ counted downwards from the top.

**Proposition 27.2 (Grey radiative equilibrium).**

In a grey atmosphere in radiative equilibrium that emits the flux $F$ to space, the temperature at the optical depth $\tau$ obeys

$$
\sigma T^4(\tau) = \frac F2\,(1 + D\tau),
$$

where $D \approx 1.66$ accounts for the slant paths of the radiation. The top of the atmosphere is at the *skin temperature* $T_\mathrm{skin} = 2^{-1/4}\,T_e$, where $T_e = (F/\sigma)^{1/4}$ is the emission temperature.

The proposition is admitted; it follows from the two-stream equations for the upward and downward fluxes. Where $\tau$ is large, near the ground, the radiative temperature changes fast with $\tau$, and $\tau$ itself grows quickly with depth because the absorbing gas is densest there: the radiative profile is steeper than the adiabat, and convection takes over. High up, $\tau$ is small and the temperature tends to the skin temperature. The Earth emits about $239\,\mathrm{W}\,\mathrm{m}^{-2}$ to space, an emission temperature of $255\,\mathrm{K}$ and a skin temperature of $214\,\mathrm{K}$; the standard atmosphere sets its tropopause at $11\,\mathrm{km}$ and $216.65\,\mathrm{K}$. The grey model, crude as it is, places the cold top of the troposphere about right.

![The layers of a planetary atmosphere (schematic, not to scale). Left: a temperature profile like the Earth’s, with the troposphere held at the adiabat by convection, a stratosphere in radiative equilibrium, and a thermosphere heated from above by extreme-ultraviolet sunlight. Right: above the exobase a particle meets nothing; one moving upwards faster than the escape velocity leaves the planet, a slower one falls back on a ballistic arc.](https://one-course.com/images/onecourse/chapters/earth-5/b3-planetary-atmospheres/fig-21d5a432958a.svg)

*The layers of a planetary atmosphere (schematic, not to scale). Left: a temperature profile like the Earth’s, with the troposphere held at the adiabat by convection, a stratosphere in radiative equilibrium, and a thermosphere heated from above by extreme-ultraviolet sunlight. Right: above the [exobase](#def-b3-planetary-atmospheres-exobase) a particle meets nothing; one moving upwards faster than the escape velocity leaves the planet, a slower one falls back on a ballistic arc.*

High in the atmosphere the air is so thin that a molecule may travel far between collisions. Where it can travel farther than a scale height, it no longer belongs to a fluid.

**Definition 27.3 (Exobase; exosphere).**

The *exobase* of an atmosphere is the level at which the mean free path of its particles equals the scale height. Above it, the *exosphere*, a particle moving upwards is unlikely to meet another, and one faster than the local escape velocity leaves the planet.

**Proposition 27.4 (Exobase condition).**

In an isothermal atmosphere of particles of collision cross-section $\sigma_c$, a particle moving vertically upwards from the level of density $n$ escapes every collision with the probability $e^{-n\sigma_c H}$. At the [exobase](#def-b3-planetary-atmospheres-exobase) $n\sigma_c H = 1$: the probability is $1/e$.

**Proof.** Along a path $\mathrm dz$ the particle meets on average $n(z)\sigma_c\,
\mathrm dz$ others. The probability of meeting none on the way up from $z_0$ is $\exp(-\sigma_c\int_{z_0}^\infty n\,\mathrm dz)$, and in an isothermal atmosphere $\int_{z_0}^\infty n_0\,e^{-(z-z_0)/H}\,\mathrm dz
= n_0 H$. The mean free path is $\ell = 1/n\sigma_c$; the condition $\ell
= H$ is $n\sigma_c H = 1$. ∎

The [exobase](#def-b3-planetary-atmospheres-exobase) lies at about $500\,\mathrm{km}$ on the Earth, $200\,\mathrm{km}$ on Venus and on Mars, and near $1500\,\mathrm{km}$ on Titan, more than half the radius of the moon.

## 27.2 Atmospheric escape

At the [exobase](#def-b3-planetary-atmospheres-exobase) the particles keep the Maxwell–Boltzmann distribution of speeds of the gas below. Its tail always holds some particles faster than the escape velocity.

**Definition 27.5 (Jeans escape; escape parameter).**

*Jeans escape* is the loss to space of the particles of the Maxwell–Boltzmann tail that move upwards at the [exobase](#def-b3-planetary-atmospheres-exobase) faster than the escape velocity. The *escape parameter* of particles of mass $m$ at the [exobase](#def-b3-planetary-atmospheres-exobase), of radius $r$ and temperature $T$, on a planet of mass $M$, is

$$
\lambda = \frac{GMm}{kTr} = \frac{v_\mathrm{esc}^2}{u^2},
\qquad u = \sqrt{\frac{2kT}m},
$$

the ratio of their gravitational binding energy to $kT$, and also the square of the escape velocity over the most probable thermal speed $u$.

**Theorem 27.6 (Jeans flux).**

At an [exobase](#def-b3-planetary-atmospheres-exobase) of density $n$, the number of particles that escape per unit area and per unit time is

$$
\Phi_\mathrm J = \frac{n\,u}{2\sqrt\pi}\,(1 + \lambda)\,e^{-\lambda}.
$$

**Proof.** The Maxwell–Boltzmann distribution of velocities is $f(\vec v) =
n\,(\pi u^2)^{-3/2}\,e^{-v^2/u^2}$. A particle of speed $v$ moving at the angle $\theta$ from the vertical crosses a horizontal unit area at the rate $v\cos\theta$. Counting only upward velocities ($0 \le \theta \le
\pi/2$) faster than $v_\mathrm{esc}$,

$$
\Phi_\mathrm J = \frac{n}{\pi^{3/2}u^3}\int_0^{2\pi}\!\!\mathrm d\varphi
\int_0^{\pi/2}\!\!\cos\theta\sin\theta\,\mathrm d\theta
\int_{v_\mathrm{esc}}^\infty v^3e^{-v^2/u^2}\,\mathrm dv
= \frac{n}{\pi^{3/2}u^3}\cdot2\pi\cdot\frac12\cdot
\frac{u^4}2\,(1 + \lambda)\,e^{-\lambda},
$$

where the last integral follows from the substitution $s = v^2/u^2$ and one integration by parts: $\int_\lambda^\infty s\,e^{-s}\,\mathrm ds =
(1 + \lambda)e^{-\lambda}$. Collecting, $\Phi_\mathrm J = n u (1 +
\lambda) e^{-\lambda}/(2\sqrt\pi)$. ∎

The factor $n u/2\sqrt\pi$ is the flux of all the particles that cross the [exobase](#def-b3-planetary-atmospheres-exobase) upwards; $(1 + \lambda)e^{-\lambda}$ is the fraction of them that escape. It falls exponentially with the mass of the particle, since $\lambda \propto m$. At the Earth’s [exobase](#def-b3-planetary-atmospheres-exobase), at $1000\,\mathrm{K}$, hydrogen has $\lambda = 7.0$ and escapes at the rate of 0.7 % of its upward flux; deuterium, $\lambda = 14$, at $1.2 \times 10^{-5}$; helium, $\lambda = 28$, at $2 \times 10^{-11}$; oxygen, $\lambda = 111$, not at all. At the [exobase](#def-b3-planetary-atmospheres-exobase) of Venus, colder and as deep in the gravity well, $\lambda = 22$ even for hydrogen; at Mars $\lambda = 5.4$; at Titan $\lambda = 1.5$ for hydrogen and 3.0 for molecular hydrogen.

![(a) The escape parameter at the exobase against the mass of the particle, for Venus (290\, K), the Earth (1000\, K; dashed: 800 and 1600\, K, the range of the solar cycle), Mars (270\, K) and Titan (180\, K); below 2.5 (shaded) escape turns hydrodynamic. (b) The fraction (1 + )e- of the upward flux that escapes, with hydrogen, deuterium and helium at the Earth’s exobase; oxygen, at = 111, is far off the scale.](https://one-course.com/images/onecourse/chapters/earth-5/b3-planetary-atmospheres/fig-2f0d1cfb882a.svg)

*(a) The [escape parameter](#def-b3-planetary-atmospheres-jeans-escape) at the [exobase](#def-b3-planetary-atmospheres-exobase) against the mass of the particle, for Venus ($290\,\mathrm{K}$), the Earth ($1000\,\mathrm{K}$; dashed: 800 and $1600\,\mathrm{K}$, the range of the solar cycle), Mars ($270\,\mathrm{K}$) and Titan ($180\,\mathrm{K}$); below $\lambda \approx 2.5$ (shaded) escape turns hydrodynamic. (b) The fraction $(1 +
\lambda)e^{-\lambda}$ of the upward flux that escapes, with hydrogen, deuterium and helium at the Earth’s [exobase](#def-b3-planetary-atmospheres-exobase); oxygen, at $\lambda = 111$, is far off the scale.*

When $\lambda$ falls to a few, the picture of particles leaking one by one from a static atmosphere fails: the upper atmosphere expands and flows away as a wind. Models place the transition at $\lambda$ between about 1.5 and 3.

**Definition 27.7 (Hydrodynamic, non-thermal and diffusion-limited escape).**

*Hydrodynamic escape* is the loss of an upper atmosphere that flows away as a whole, heated from above, when its [escape parameter](#def-b3-planetary-atmospheres-jeans-escape) is small; the flow may drag heavier particles with it. *Non-thermal escape* is the loss of particles accelerated by processes other than heat: photochemical reactions that give fragments more than the escape energy, ions picked up by the electric field of the solar wind, sputtering by ions that strike the upper atmosphere, and the outflow of ions along magnetic field lines. *Diffusion-limited escape* is escape whose rate is set not at the [exobase](#def-b3-planetary-atmospheres-exobase) but lower down, by the rate at which the escaping gas can diffuse up through the heavier gas above the *homopause*, the level above which molecular diffusion, not turbulence, controls the mixture.

**Proposition 27.8 (Diffusion limit).**

A light gas of mixing ratio $f$ and molecular mass $m_i$, diffusing through a heavier gas of molecular mass $m_a$ and scale height $H_a =
kT/m_a g$ with the binary diffusion parameter $b$, cannot rise faster than

$$
\Phi_\mathrm{DL} = b\,f\left(\frac1{H_a} - \frac1{H_i}\right)
= \frac{b\,f\,(m_a - m_i)\,g}{kT} \approx \frac{b\,f}{H_a}.
$$

**Proof.** Kinetic theory (admitted) gives the upward flux of the light gas relative to the heavy one, in an isothermal column, as $\Phi = -b\,f\,
[\,(1/f)\,\mathrm df/\mathrm dz + 1/H_i - 1/H_a\,]$: the light gas diffuses down its own gradient, and its own scale height $H_i$ is larger than $H_a$. The flux is largest when the mixing ratio is uniform, $\mathrm
df/\mathrm dz = 0$; the escaping gas cannot be drawn faster without its mixing ratio falling with height. With $1/H = mg/kT$ the two forms follow. ∎

For molecular hydrogen rising through carbon dioxide, $b \approx
1.2 \times 10^{19}\,\mathrm{cm}^{-1}\,\mathrm{s}^{-1}$ at $200\,\mathrm{K}$, and with the Earth’s gravity the limit is $\Phi_\mathrm{DL} \approx
3.0 \times 10^{13}\,f\,(200\,\mathrm{K}/T)^{1/4}$ molecules of $\ce{H2}$ per square centimetre and per second, $f$ counting all the hydrogen as $\ce{H2}$. On the Earth today the escape of hydrogen is diffusion-limited: at solar minimum, when the [exobase](#def-b3-planetary-atmospheres-exobase) is colder and [Jeans escape](#def-b3-planetary-atmospheres-jeans-escape) slower, escape by charge exchange with ions takes up the slack, and the total stays about the same. The supply, not the [exobase](#def-b3-planetary-atmospheres-exobase), sets the rate.

## 27.3 Venus and the runaway greenhouse

Venus receives $2601\,\mathrm{W}\,\mathrm{m}^{-2}$ from the Sun, 1.91 times the Earth’s share. Its clouds of sulfuric acid reflect 77 % of it, so it absorbs less than the Earth; yet its surface is at $737\,\mathrm{K}$ under $92\,\mathrm{bar}$ of an atmosphere 96.5 % carbon dioxide. It holds $6 \times 10^{15}\,\mathrm{kg}$ of water, against $1.4 \times 10^{21}\,\mathrm{kg}$ on the Earth, about 30 parts per million by volume below the clouds.

A planet with an ocean is held in balance by its outgoing radiation. If it warms, more water evaporates; water vapour is a greenhouse gas, so the outgoing radiation grows less than $\sigma T^4$, but it grows, and the warming stops. There is a limit to that growth.

**Proposition 27.9 (Radiation limit of a moist atmosphere).**

When the surface of an ocean planet is hot enough for water vapour to dominate its upper atmosphere, the temperature there follows the saturation curve of water, and the infrared radiation to space comes from a level of fixed pressure. Its temperature, and the outgoing radiation, stop growing with the surface temperature.

**Proof.** In a saturated column dominated by vapour, the pressure $p$ at every level is the saturation pressure at the local temperature, $p =
p_\mathrm{sat}(T)$. The radiation to space leaves from around the level where the optical depth from the top is about one. For a grey gas of mass absorption coefficient $\kappa$ the optical depth above the pressure $p$ is $D\kappa p/g$, so that level sits at $p_1 = g/D\kappa$, whatever the surface temperature, and its temperature is the one at which $p_\mathrm{sat}(T) = p_1$. Warming the surface only adds vapour below it. ∎

**Definition 27.10 (Runaway greenhouse; runaway greenhouse limit; moist greenhouse).**

The *runaway greenhouse limit* is the largest flux of infrared radiation that a planet with an ocean can send to space. A *runaway greenhouse* is the state of a planet that absorbs more sunlight than that limit: it cannot balance its budget until the whole ocean has evaporated and the surface has heated far beyond it. A *moist greenhouse* is the state of a planet, short of the runaway, whose surface is warm enough for its stratosphere to hold a large mixing ratio of water vapour, which ultraviolet light splits and whose hydrogen escapes.

Simple models such as that of the proposition give such a limit; with the real lines of water vapour, a cloud-free line-by-line calculation puts it at $291\,\mathrm{W}\,\mathrm{m}^{-2}$ for an Earth-like planet, and reviews quote about $300\,\mathrm{W}\,\mathrm{m}^{-2}$. Beyond about $2000\,\mathrm{K}$ the outgoing flux grows again, as the hot lower atmosphere radiates in the visible and near infrared, where water absorbs little: a planet in a [runaway greenhouse](#def-b3-planetary-atmospheres-runaway) settles at a very high temperature, once its ocean is all vapour.

![Outgoing infrared radiation of an Earth-like ocean planet against its surface temperature, in an illustrative grey model (a saturated moist adiabat over 1 bar of nitrogen, a stratosphere at 200\, K, water vapour the only absorber; its absorption coefficient, broadened by pressure, is chosen to land on the line-by-line limit). Horizontal lines: sunlight absorbed by Venus today and by a young Venus with an albedo of 0.193, the albedo of a hot cloud-free steam atmosphere, and by the Earth today with its albedo of 0.3. Where the absorbed flux lies above the plateau, no surface temperature balances it: the greenhouse runs away.](https://one-course.com/images/onecourse/chapters/earth-5/b3-planetary-atmospheres/fig-20fbf64bebbd.svg)

*Outgoing infrared radiation of an Earth-like ocean planet against its surface temperature, in an illustrative grey model (a saturated moist adiabat over 1 bar of nitrogen, a stratosphere at $200\,\mathrm{K}$, water vapour the only absorber; its absorption coefficient, broadened by pressure, is chosen to land on the line-by-line limit). Horizontal lines: sunlight absorbed by Venus today and by a young Venus with an albedo of 0.193, the albedo of a hot cloud-free steam atmosphere, and by the Earth today with its albedo of 0.3. Where the absorbed flux lies above the plateau, no surface temperature balances it: the greenhouse runs away.*

With the albedo of a cloud-free steam atmosphere, 0.193, an Earth-like planet around the Sun runs away when it receives 1.06 times the Earth’s sunlight, at $0.97\,\mathrm{au}$. Before that, at 1.015 times the Earth’s sunlight and a surface temperature of $340\,\mathrm{K}$, its stratosphere turns moist: on the Earth today water is cold-trapped at the tropopause, near $0.1\,\mathrm{bar}$, but on a warmer planet the cold trap rises and lets vapour through. When the mixing ratio of water in the stratosphere reaches about $3 \times 10^{-3}$, [diffusion-limited escape](#def-b3-planetary-atmospheres-hydrodynamic) removes an ocean of hydrogen in about the age of the Earth.

The deuterium of Venus measures what was lost. Each atom that escapes removes hydrogen and a little deuterium from the remaining reservoir, as each drop that rains out removes a little of the heavy isotopes from a cloud.

**Proposition 27.11 (Isotopic enrichment by escape).**

Let a reservoir of water lose hydrogen to space, each atom of deuterium escaping with the efficiency $\alpha$ relative to an atom of hydrogen ($\alpha < 1$). When the reservoir has shrunk from $M_0$ to $M$, its ratio $R = \mathrm{D}/\mathrm{H}$ has grown from $R_0$ to

$$
\frac R{R_0} = \left(\frac{M_0}M\right)^{1-\alpha}.
$$

**Proof.** Losing $\mathrm dN_\mathrm H$ hydrogen atoms costs the reservoir $\mathrm dN_\mathrm D = \alpha R\,\mathrm dN_\mathrm H$ deuterium atoms: $\mathrm dN_\mathrm D/N_\mathrm D = \alpha\,\mathrm dN_\mathrm H/
N_\mathrm H$, so $N_\mathrm D \propto N_\mathrm H^\alpha$ and $R \propto
N_\mathrm H^{\alpha - 1}$. The mass of water is proportional to $N_\mathrm H$. This is [Rayleigh distillation](https://one-course.com/books/earth/5/en/chapter/14-stable-isotope-geochemistry#prop-b3-stable-isotopes-rayleigh-distillation), with escape in the place of rain. ∎

If no deuterium escaped at all ($\alpha = 0$), a hundredfold enrichment would mean that Venus once held at least a hundred times its present water. Escape that fractionates less needs far more: in [diffusion-limited escape](#def-b3-planetary-atmospheres-hydrodynamic) $\alpha \approx 0.8$, and a hundredfold enrichment would require the reservoir to shrink by a factor of $100^5$. The ratio is read as a lower bound: at least a few tenths of a percent of a terrestrial ocean, and estimates of an early Venus ocean range from 4 to $525\,\mathrm{m}$ spread over its surface. Two cautions remain. Most of the fractionation may have happened only in the loss of the last few bars of water, and a steady supply of water from comets or volcanoes, lost as fast as it came, could build the same ratio. Venus is still losing water: its escaping ions are hydrogen and oxygen in the ratio of two to one, pulled out by an electric field five times stronger than the one in the Earth’s ionosphere, around a planet with no magnetic field.

## 27.4 Mars: a thin atmosphere and a wet past

Mars keeps a mean surface pressure of $6.36\,\mathrm{mbar}$, between 4.0 and $8.7\,\mathrm{mbar}$ with the seasons, 95 % carbon dioxide, at about $214\,\mathrm{K}$. The pressure barely exceeds the triple-point pressure of water, $6.1\,\mathrm{mbar}$: liquid water cannot last at its surface, where ice sublimes. Yet ancient terrains are cut by branching valleys, and carry minerals that form only in liquid water.

![A network of dried-up valleys on Mars, seen by the camera of Mars Express at about 14\, m per pixel, near 17 S, 66 E; north is to the right, and the scale bar is 20\, km. Tributaries join downstream into larger valleys, the pattern of a drainage network. Image ESA/DLR/FU Berlin, CC BY-SA 3.0 IGO.](https://one-course.com/images/onecourse/chapters/earth-5/b3-planetary-atmospheres/img-ece6c11f272b.jpg)

*A network of dried-up valleys on Mars, seen by the camera of Mars Express at about $14\,\mathrm{m}$ per pixel, near $17{}^{\circ}$ S, $66{}^{\circ}$ E; north is to the right, and the scale bar is $20\,\mathrm{km}$. Tributaries join downstream into larger valleys, the pattern of a drainage network. Image ESA/DLR/FU Berlin, CC BY-SA 3.0 IGO.*

The valleys and the flow channels of Mars need, by geological estimates, a global layer of water 100 to $1500\,\mathrm{m}$ deep, against 3 to $25\,\mathrm{m}$ in its ice and air today. Much of the rest went to space. The MAVEN orbiter measured the solar wind stripping gas from Mars at about $100\,\mathrm{g}$ per second, three quarters of it down the tail behind the planet, where the solar wind flows, and a quarter in a plume over the poles; during the solar storms of March 2015 the loss sped up, and it was probably much faster when the young Sun was more active. Mars also loses hydrogen, about $3 \times 10^{26}$ atoms per second on average today: kept up for four billion years, a loss worth a global layer of water only about $4\,\mathrm{m}$ deep.

The rate has not always been today’s. The obliquity of Mars, $25.2{}^{\circ}$ now, has wandered between 0 and $66{}^{\circ}$ over the last 250 million years, around a mean near $35{}^{\circ}$, while the Earth’s varies by little more than a degree. The motion is chaotic and cannot be traced back over billions of years; elliptical craters made by grazing impacts, whose orientations record the obliquity, suggest a mean between about 10 and $30{}^{\circ}$ over the last 3.5 billion years or so. At high obliquity the summer pole warms, more water vapour rises, and climate models make the loss of hydrogen twenty times faster: over Mars’s history, a layer of the order of $80\,\mathrm{m}$.

## 27.5 Titan: a methane cycle

Titan, a moon smaller than Mars, has a thicker atmosphere than the Earth: a surface pressure about 60 % higher, at $-179{}^{\circ}\mathrm{C}$. The atmosphere is about 95 % nitrogen and 5 % methane, and because the moon’s gravity is weak it extends ten times higher than the Earth’s, to nearly $600\,\mathrm{km}$. Ultraviolet light splits the methane and nitrogen high up; the fragments recombine into an orange haze of heavier hydrocarbons that hides the surface from visible light. Below the haze, methane plays the part of water: it condenses into clouds, rains, cuts river channels and fills lakes and seas of methane and ethane.

![Ligeia Mare, a sea near Titan’s north pole, in a false-colour mosaic of Cassini radar images: features thought to be liquid in blue and black, solid ground tinted brown, with bays, islands and presumed tributary networks. Of about 400 lakes and seas in the mapped north, those larger than 26\,000\, km2 hold 70 % of the area. NASA/JPL/USGS, public domain.](https://one-course.com/images/onecourse/chapters/earth-5/b3-planetary-atmospheres/img-98bcf15ba655.jpg)

*Ligeia Mare, a sea near Titan’s north pole, in a false-colour mosaic of Cassini radar images: features thought to be liquid in blue and black, solid ground tinted brown, with bays, islands and presumed tributary networks. Of about 400 lakes and seas in the mapped north, those larger than $26\,000\,\mathrm{km}^{2}$ hold 70 % of the area. NASA/JPL/USGS, public domain.*

Whether a liquid can lie on a surface depends on its phase diagram and on the pressure and temperature there. Titan’s surface lies just above the triple point of methane, $90.67\,\mathrm{K}$ and $0.117\,\mathrm{bar}$, and below its critical point: liquid methane is possible, and methane at 5 % of $1.6\,\mathrm{bar}$ is not far from saturation. The surface of Mars sits near the triple point of water, the Earth’s well inside its liquid field, and Venus’s above water’s critical temperature, $647\,\mathrm{K}$, where no liquid can exist at all.

![The boundaries between vapour and condensed water (blue: liquid–vapour, from the triple point to the critical point; dashed: ice–vapour) and between liquid methane and its vapour (orange), with the mean surface states of Venus, the Earth, Mars and Titan (squares). A liquid can lie on a surface whose pressure is above the curve of that liquid, between its triple and critical temperatures.](https://one-course.com/images/onecourse/chapters/earth-5/b3-planetary-atmospheres/fig-e6a205bcde26.svg)

*The boundaries between vapour and condensed water (blue: liquid–vapour, from the triple point to the critical point; dashed: ice–vapour) and between liquid methane and its vapour (orange), with the mean surface states of Venus, the Earth, Mars and Titan (squares). A liquid can lie on a surface whose pressure is above the curve of that liquid, between its triple and critical temperatures.*

Titan keeps its nitrogen easily: at its [exobase](#def-b3-planetary-atmospheres-exobase) $\lambda = 41$ for nitrogen. Its hydrogen, at $\lambda$ near 1.5, leaves almost freely, and the escape of molecular hydrogen is set lower down by the limiting flux through the [homopause](#def-b3-planetary-atmospheres-hydrodynamic), as on the Earth. The heavy compounds made from the broken methane settle to the surface, where they make the sand of vast fields of dunes.

## 27.6 Planetary habitability

The habitable zone of the school books is the range of distances from a star at which a planet like the Earth can keep liquid water at its surface. Its edges are the limits met in this chapter.

**Definition 27.12 (Planetary habitability).**

The *planetary habitability* of a planet is its capacity to keep liquid water at its surface over geological times: it receives a stellar flux within the limits of the habitable zone, it holds on to its atmosphere and its water against escape, and a long-term carbon cycle regulates its climate.

The inner edge of the habitable zone is the moist or the [runaway greenhouse](#def-b3-planetary-atmospheres-runaway): an Earth-like planet around the Sun turns moist at $0.99\,\mathrm{au}$ and runs away at $0.97\,\mathrm{au}$. The outer edge is the *maximum greenhouse*: adding carbon dioxide warms a planet only until the extra gas scatters back more sunlight than its greenhouse effect gains; around the Sun this happens at $1.70\,\mathrm{au}$, under some $8\,\mathrm{bar}$ of carbon dioxide. Those are conservative edges, computed without clouds. Two empirical ones are wider: Venus seems to have had no surface water for at least a billion years, when it received 1.76 times the Earth’s present sunlight ($0.75\,\mathrm{au}$); Mars had flowing water when it received 0.32 times that sunlight, if its valleys are 3.8 billion years old ($1.77\,\mathrm{au}$). Around cooler stars the same limits come at lower fluxes, because their redder light is scattered less and absorbed more by water and carbon dioxide.

![The habitable zone of an Earth-like planet, as the stellar flux it receives against the temperature of its star (shaded: between the moist greenhouse and the maximum greenhouse). Dotted: the empirical limits drawn from recent Venus and early Mars. The fits are those of a cloud-free climate model, valid from 2600 to 7200\, K.](https://one-course.com/images/onecourse/chapters/earth-5/b3-planetary-atmospheres/fig-eced055cf41b.svg)

*The habitable zone of an Earth-like planet, as the stellar flux it receives against the temperature of its star (shaded: between the [moist greenhouse](#def-b3-planetary-atmospheres-runaway) and the maximum greenhouse). Dotted: the empirical limits drawn from recent Venus and early Mars. The fits are those of a cloud-free climate model, valid from 2600 to $7200\,\mathrm{K}$.*

Distance is not enough. A planet must hold on to its atmosphere: a small or hot one, whose [escape parameter](#def-b3-planetary-atmospheres-jeans-escape) is low, loses its hydrogen and with it its water, and a planet in a [moist greenhouse](#def-b3-planetary-atmospheres-runaway) dries out from the top. It must also keep its climate stable over billions of years while its star brightens: on the Earth, the silicate-weathering thermostat of the long-term carbon cycle draws carbon dioxide down when the climate warms and lets it build up when it cools. On Venus, without plate tectonics, outgassed carbon dioxide has had no way back into the rocks and has accumulated in the air; it now holds about as much carbon dioxide as the Earth has locked in carbonate rocks. Whether a magnetic field protects an atmosphere is debated: it shields the upper atmosphere from the solar wind, but it also opens other paths of escape, such as the outflow of ions near the poles, and the habitability of a planet cannot be read from its place in the habitable zone alone.

## 27.7 Exercises

**Exercise 27.1 ★.**

Compute the scale height $H = RT/Mg$ near the surface of Venus ($737\,\mathrm{K}$, carbon dioxide of molar mass $44.01\,\mathrm{g}\,\mathrm{mol}^{-1}$, $g = 8.87\,\mathrm{m}\,\mathrm{s}^{-2}$), the Earth ($288\,\mathrm{K}$, $28.97\,\mathrm{g}\,\mathrm{mol}^{-1}$, $9.80\,\mathrm{m}\,\mathrm{s}^{-2}$), Mars ($214\,\mathrm{K}$, $43.34\,\mathrm{g}\,\mathrm{mol}^{-1}$, $3.71\,\mathrm{m}\,\mathrm{s}^{-2}$) and Titan ($94\,\mathrm{K}$, $28.0\,\mathrm{g}\,\mathrm{mol}^{-1}$, $1.35\,\mathrm{m}\,\mathrm{s}^{-2}$). Which atmosphere is the most extended, and why?

**Solution of Exercise 27.1.**

$H = RT/Mg$: Venus $8.314\times737/(0.04401\times8.87) = 15.7\,\mathrm{km}$; the Earth $8.314\times288/(0.02897\times9.80) = 8.4\,\mathrm{km}$; Mars $8.314\times214/(0.04334\times3.71) = 11.1\,\mathrm{km}$; Titan $8.314\times94/(0.0280\times1.35) = 20.7\,\mathrm{km}$. Titan’s atmosphere, cold as it is, is the most extended: its gravity is seven times weaker than the Earth’s.

**Exercise 27.2 ★.**

The Earth’s [exobase](#def-b3-planetary-atmospheres-exobase) lies at $500\,\mathrm{km}$ (radius $6878\,\mathrm{km}$); its temperature varies from 800 to $1600\,\mathrm{K}$ over the solar cycle. Take the mass of the Earth as $5.97 \times 10^{24}\,\mathrm{kg}$. Compute the [escape parameter](#def-b3-planetary-atmospheres-jeans-escape) of hydrogen atoms at both temperatures, and the escaping fraction $(1 + \lambda)e^{-\lambda}$. By what factor does the solar cycle change it?

**Solution of Exercise 27.2.**

$\lambda = GMm/kTr = 6.674 \times 10^{-11}\times5.97 \times 10^{24}\times1.674 \times 10^{-27}
/(1.381 \times 10^{-23}\,T\times6.878 \times 10^{6})$: 8.78 at $800\,\mathrm{K}$, 4.39 at $1600\,\mathrm{K}$. The escaping fractions are $9.78\,e^{-8.78} =
1.5 \times 10^{-3}$ and $5.39\,e^{-4.39} = 6.7 \times 10^{-2}$: the solar cycle changes the escaping fraction of hydrogen by a factor of about 44.

**Exercise 27.3 ★.**

Around the Sun, an Earth-like planet turns moist at the flux $S_\mathrm{eff}
= 1.014$, runs away at 1.0512 and reaches the maximum greenhouse at 0.3438 (fluxes relative to the Earth’s). (a) Compute the three distances, in astronomical units. (b) Venus and Mars receive 1.91 and 0.43 times the Earth’s sunlight. Place them.

**Solution of Exercise 27.3.**

(a) $d = S_\mathrm{eff}^{-1/2}$: [moist greenhouse](#def-b3-planetary-atmospheres-runaway) $0.993\,\mathrm{au}$, runaway $0.975\,\mathrm{au}$, maximum greenhouse $1.705\,\mathrm{au}$. (b) Venus, at 1.91, receives more than the runaway flux and even more than the empirical recent-Venus limit (1.78): it lies inside the inner edge. Mars, at 0.43, lies between 1.014 and 0.3438, inside the conservative habitable zone: its dryness comes from its small size and the loss of its atmosphere, not from its distance.

**Exercise 27.4 ★.**

The vapour pressure of liquid methane is $\log_{10}(p/\mathrm{bar}) = 3.9895 -
443.028/(T/\mathrm{K} - 0.49)$. (a) Compute it at the surface of Titan, $94.15\,\mathrm{K}$. (b) Methane makes 5 % of Titan’s air at $1.6\,\mathrm{bar}$. Compute its partial pressure and its relative humidity. (c) What does the result suggest about evaporation from Titan’s seas?

**Solution of Exercise 27.4.**

(a) $\log_{10}p = 3.9895 - 443.028/93.66 = -0.741$, $p =
0.18\,\mathrm{bar}$. (b) $0.05\times1.6 = 0.080\,\mathrm{bar}$, a relative humidity of $0.080/0.18 = 44\,\%$. (c) The air above the seas is far from saturated: methane evaporates from them, as water does from the Earth’s oceans, and the humid air must rise and cool before it rains.

**Exercise 27.5 ★★.**

At the Earth’s [exobase](#def-b3-planetary-atmospheres-exobase) ($1000\,\mathrm{K}$, $\lambda = 7.02$ for hydrogen), compute the [escape parameter](#def-b3-planetary-atmospheres-jeans-escape) of deuterium, its thermal speed relative to hydrogen’s and the ratio of the Jeans fluxes per atom, D to H. Is [Jeans escape](#def-b3-planetary-atmospheres-jeans-escape) a strong isotopic filter?

**Solution of Exercise 27.5.**

$\lambda_\mathrm D = 7.02\times2.014/1.008 = 14.0$. $u_\mathrm D/u_\mathrm H
= \sqrt{1.008/2.014} = 0.71$. Ratio per atom $= 0.71\times(15.0\,
e^{-14.0})/(8.02\,e^{-7.02}) = 0.71\times1.69 \times 10^{-3} = 1.2 \times 10^{-3}$. [Jeans escape](#def-b3-planetary-atmospheres-jeans-escape) lets almost no deuterium out: it is a strong filter, with $\alpha \approx 0.001$.

**Exercise 27.6 ★★.**

The ratio D/H of the water of Venus is $0.016$; that of ocean water on the Earth is $1.5575 \times 10^{-4}$. (a) Compute the enrichment. (b) With no escape of deuterium at all, what is the smallest past inventory of water of Venus, given $6 \times 10^{15}\,\mathrm{kg}$ today? What depth would it make spread over the planet’s $4.60 \times 10^{14}\,\mathrm{m}^{2}$? (c) What shrinking of the reservoir would [diffusion-limited escape](#def-b3-planetary-atmospheres-hydrodynamic), with $\alpha = 0.8$, require? Conclude.

**Solution of Exercise 27.6.**

(a) $0.016/1.5575 \times 10^{-4} = 103$. (b) With $\alpha = 0$ the enrichment is $M_0/M$: $M_0 = 103\times6 \times 10^{15} = 6.2 \times 10^{17}\,\mathrm{kg}$, or $6.2 \times 10^{17}/(1000\times4.60 \times 10^{14}) = 1.3\,\mathrm{m}$ of water over Venus. (c) $M_0/M = 103^{1/0.2} = 1.2 \times 10^{10}$, a past inventory of $7 \times 10^{25}\,\mathrm{kg}$, twelve times the mass of the Earth: impossible. The enrichment needs a strongly fractionating escape (Jeans or non-thermal), active at least during the loss of the last of the water, or a steady state with a supply of water.

**Exercise 27.7 ★★.**

Mars, of radius $3389.5\,\mathrm{km}$, loses about $3 \times 10^{26}$ hydrogen atoms per second. (a) If each pair of atoms came from a molecule of water, what global layer of water does the loss remove in four billion years? (b) Same question at $6 \times 10^{27}$ atoms per second, the rate of a high obliquity. (c) Compare with the 100 to $1500\,\mathrm{m}$ the valleys and channels need.

**Solution of Exercise 27.7.**

(a) In four billion years ($1.26 \times 10^{17}$ s) Mars loses $3.8 \times 10^{43}$ atoms, $1.9 \times 10^{43}$ molecules of water, $5.7 \times 10^{17}\,\mathrm{kg}$; over $4\pi(3.3895 \times 10^{6})^2 = 1.44 \times 10^{14}\,\mathrm{m}^{2}$ that is a layer $3.9\,\mathrm{m}$ deep. (b) Twenty times more, $78\,\mathrm{m}$. (c) Even the high-obliquity rate reaches only the lower end of the 100 to $1500\,\mathrm{m}$; the rest went into the crust and the ice, or was lost faster when the Sun was young.

**Exercise 27.8 ★★.**

(a) Compute the mass of the atmosphere of Mars from its mean surface pressure, $636\,\mathrm{Pa}$, its gravity, $3.71\,\mathrm{m}\,\mathrm{s}^{-2}$, and its radius. (b) The solar wind strips about $100\,\mathrm{g}$ of gas per second. What mass does that remove in four billion years, and in how long would it remove the present atmosphere? (c) Why is that an underestimate of the past loss?

**Solution of Exercise 27.8.**

(a) $m = pA/g = 636\times1.44 \times 10^{14}/3.71 = 2.5 \times 10^{16}\,\mathrm{kg}$. (b) $0.1\times1.26 \times 10^{17} = 1.3 \times 10^{16}\,\mathrm{kg}$, half the present atmosphere; the whole of it in $2.5 \times 10^{16}/0.1 = 2.5 \times 10^{17}\,\mathrm{s}$, $7.8$ billion years. (c) The young Sun was more active and its storms more frequent, and the loss grows during storms; other channels (hydrogen, sputtering, photochemical escape) are not counted.

**Exercise 27.9 ★★.**

An Earth-like planet with a cloud-free steam atmosphere reflects 19.3 % of the sunlight it receives; its infrared output cannot exceed $291\,\mathrm{W}\,\mathrm{m}^{-2}$. (a) Above what flux of sunlight, in watts per square metre and relative to the Earth’s $1361\,\mathrm{W}\,\mathrm{m}^{-2}$, does it run away? (b) Compare with Venus today, $2601\,\mathrm{W}\,\mathrm{m}^{-2}$, and with a young Venus under a Sun at 70 % of its present luminosity. (c) Why is the conclusion for the young Venus not final?

**Solution of Exercise 27.9.**

(a) $S(1 - 0.193)/4 = 291$ gives $S = 1442\,\mathrm{W}\,\mathrm{m}^{-2}$, 1.06 times the Earth’s. (b) Venus today would absorb $0.807\times2601/4 =
525\,\mathrm{W}\,\mathrm{m}^{-2}$; a young Venus, $0.7\times2601 = 1821\,\mathrm{W}\,\mathrm{m}^{-2}$ received, $367\,\mathrm{W}\,\mathrm{m}^{-2}$ absorbed: both above the limit, so a cloud-free young Venus would have run away from the start. (c) Clouds raise the albedo; three-dimensional models with clouds have found a path to a habitable young Venus.

**Exercise 27.10 ★★★.**

A model thermosphere of atomic oxygen is isothermal at $1000\,\mathrm{K}$, with $n = 1 \times 10^{16}\,\mathrm{m}^{-3}$ at $200\,\mathrm{km}$; take $g =
9.21\,\mathrm{m}\,\mathrm{s}^{-2}$ at that height and a collision cross-section $\sigma_c = 3 \times 10^{-19}\,\mathrm{m}^{2}$. (a) Compute the scale height of the oxygen. (b) Compute the density at the [exobase](#def-b3-planetary-atmospheres-exobase) and the height of the [exobase](#def-b3-planetary-atmospheres-exobase). (c) Gravity decreases with height. Does that move the [exobase](#def-b3-planetary-atmospheres-exobase) up or down?

**Solution of Exercise 27.10.**

(a) $H = kT/mg = 1.381 \times 10^{-23}\times1000/(16\times1.661 \times 10^{-27}\times9.21)
= 56\,\mathrm{km}$. (b) $n_\mathrm{exo} = 1/(\sigma_c H) = 1/(3 \times 10^{-19}\times
5.64 \times 10^{4}) = 5.9 \times 10^{13}\,\mathrm{m}^{-3}$; $z = 200 + 56.4\ln(1 \times 10^{16}/
5.9 \times 10^{13}) = 200 + 56.4\times5.13 = 490\,\mathrm{km}$. (c) Gravity weaker higher up makes the scale height grow with height, so the density falls more slowly than assumed: the [exobase](#def-b3-planetary-atmospheres-exobase) moves up.

**Exercise 27.11 ★★★.**

(a) Suppose the Earth’s stratosphere turned moist, with a mixing ratio of water vapour of $3 \times 10^{-3}$ (counted as $\ce{H2}$). With the diffusion limit $3.0 \times 10^{13}\,f$ molecules of $\ce{H2}$ per square centimetre and per second, at $200\,\mathrm{K}$, compute the loss of hydrogen of the whole Earth (radius $6371\,\mathrm{km}$). (b) How long would an ocean, $1.4 \times 10^{24}\,\mathrm{g}$ of water, last? Compare with the age of the Earth.

**Solution of Exercise 27.11.**

(a) $\Phi = 3.0 \times 10^{13}\times3 \times 10^{-3} = 9 \times 10^{10}\,\mathrm{cm}^{-2}\,\mathrm{s}^{-1} =
9 \times 10^{14}\,\mathrm{m}^{-2}\,\mathrm{s}^{-1}$; over $4\pi(6.371 \times 10^{6})^2 =
5.10 \times 10^{14}\,\mathrm{m}^{2}$, $4.6 \times 10^{29}$ molecules of $\ce{H2}$ per second. (b) An ocean holds $1.4 \times 10^{24}/18.015\times6.022 \times 10^{23} =
4.7 \times 10^{46}$ molecules of water, one $\ce{H2}$ each: it lasts $1.0 \times 10^{17}\,\mathrm{s} = 3.2\text{ billion years}$, comparable with the age of the Earth, which is why a mixing ratio of $3 \times 10^{-3}$ marks the [moist greenhouse](#def-b3-planetary-atmospheres-runaway) limit.

**Exercise 27.12 ★★★.**

In a pure-steam upper atmosphere absorbing as a grey gas with $\kappa =
0.005\,\mathrm{m}^{2}\,\mathrm{kg}^{-1}$, on a planet with $g = 9.81\,\mathrm{m}\,\mathrm{s}^{-2}$ and $D = 1.66$: (a) compute the pressure $p_1$ of the radiating level; (b) with $p_\mathrm{sat}(T) = 611.657\,\mathrm{Pa}\,\exp[(L/R_v)(1/T_t -
1/T)]$, $L = 2.5 \times 10^{6}\,\mathrm{J}\,\mathrm{kg}^{-1}$, $R_v = 461.5\,\mathrm{J}\,\mathrm{kg}^{-1}\,\mathrm{K}^{-1}$, $T_t = 273.16\,\mathrm{K}$, compute its temperature and the radiation limit. (c) The line-by-line limit is $291\,\mathrm{W}\,\mathrm{m}^{-2}$. Should the effective $\kappa$ of real water vapour be larger or smaller?

**Solution of Exercise 27.12.**

(a) $p_1 = g/D\kappa = 9.81/(1.66\times0.005) = 1180\,\mathrm{Pa}$. (b) $1/T = 1/273.16 - \ln(1182/611.657)\times461.5/2.5 \times 10^{6}$, $T =
282.5\,\mathrm{K}$, and $\sigma T^4 = 361\,\mathrm{W}\,\mathrm{m}^{-2}$. (c) The real limit is lower, so the radiating level is colder and at lower pressure: real water vapour is more opaque than this grey gas, and its effective $\kappa$ larger.

## 27.8 Problem: Will Kepos Keep Its Water?

**Problem 27.1.**

Weekend problem — escape and habitability of an invented ocean planet

Kepos is an invented planet of mass $5.2 \times 10^{24}\,\mathrm{kg}$ and radius $6200\,\mathrm{km}$, with oceans and an atmosphere of nitrogen and carbon dioxide. It orbits at $0.60\,\mathrm{au}$ a star of luminosity 0.30 times the Sun’s and effective temperature $4800\,\mathrm{K}$. Its [exobase](#def-b3-planetary-atmospheres-exobase) lies $500\,\mathrm{km}$ above the surface, at $1400\,\mathrm{K}$, with $2 \times 10^{11}\,\mathrm{m}^{-3}$ hydrogen atoms; its [homopause](#def-b3-planetary-atmospheres-hydrodynamic) is at $200\,\mathrm{K}$, where carbon dioxide dominates and where hydrogen in all its forms makes a mixing ratio $f = 1 \times 10^{-3}$, counted as $\ce{H2}$. An Earth ocean is $1.4 \times 10^{24}\,\mathrm{g}$ of water.

**Part I — The exobase.**

1. Compute the surface gravity and the mean density of Kepos.
2. Compute the escape velocity at the [exobase](#def-b3-planetary-atmospheres-exobase) .
3. Compute the thermal speed $u = \sqrt{2kT/m}$ of hydrogen, helium and oxygen atoms at the [exobase](#def-b3-planetary-atmospheres-exobase) .
4. Compute their [escape parameters](#def-b3-planetary-atmospheres-jeans-escape) .
5. Which of them can escape by [Jeans escape](#def-b3-planetary-atmospheres-jeans-escape) at a significant rate? Is any close to the hydrodynamic regime?
6. During an active youth of its star the [exobase](#def-b3-planetary-atmospheres-exobase) of Kepos may have reached $3000\,\mathrm{K}$ . What was then the [escape parameter](#def-b3-planetary-atmospheres-jeans-escape) of hydrogen, and what does it suggest?

**Part II — Jeans escape of hydrogen.**

7. Compute the escaping fraction $(1 + \lambda)e^{-\lambda}$ for hydrogen.
8. Compute the Jeans flux of hydrogen, per square metre and per second.
9. Compute the number of hydrogen atoms that leave the whole [exobase](#def-b3-planetary-atmospheres-exobase) per second.
10. How many hydrogen atoms does an Earth ocean hold?
11. At this rate, how long would Kepos take to lose them?
12. Compute the [escape parameter](#def-b3-planetary-atmospheres-jeans-escape) of deuterium and its escape efficiency relative to hydrogen, per atom.

**Part III — The diffusion limit.**

13. Compute the scale height of carbon dioxide at the [homopause](#def-b3-planetary-atmospheres-hydrodynamic) .
14. The binary diffusion parameter of hydrogen in carbon dioxide is $b = 1.2 \times 10^{19}\,\mathrm{cm}^{-1}\,\mathrm{s}^{-1}$ at $200\,\mathrm{K}$ . Compute the diffusion-limited flux of $\ce{H2}$ , per square metre and per second.
15. Check it against the Earth’s limit, $3.0 \times 10^{13}\,f$ molecules per square centimetre and per second, scaled by gravity.
16. Compute the number of hydrogen atoms that the diffusion limit can supply to the upper atmosphere of the whole planet per second (take the area of the surface).
17. Compare with question 9. Which process limits the escape, and what happens to the hydrogen of the thermosphere?
18. What density of hydrogen at the [exobase](#def-b3-planetary-atmospheres-exobase) would let [Jeans escape](#def-b3-planetary-atmospheres-jeans-escape) carry the whole supply?
19. How long would Kepos take to lose an Earth ocean of hydrogen at the diffusion limit?

**Part IV — Is Kepos in the habitable zone?**

20. Compute the stellar flux Kepos receives, relative to the Earth’s.
21. For a star of $4800\,\mathrm{K}$ the [moist greenhouse](#def-b3-planetary-atmospheres-runaway) limit is at $S_\mathrm{eff} = 0.939$ and the maximum greenhouse at 0.290. Compute the edges of the habitable zone, in astronomical units, and place Kepos.
22. By what factor must the star brighten before Kepos reaches the inner edge?
23. With an albedo of 0.3, compute the sunlight Kepos absorbs per square metre, and its equilibrium temperature. Compare with the [runaway greenhouse limit](#def-b3-planetary-atmospheres-runaway) .
24. If a warmer climate made the stratosphere of Kepos moist, with $f = 3 \times 10^{-3}$ , how long would an Earth ocean last?
25. Give the time for Kepos to lose an Earth ocean of hydrogen by [diffusion-limited escape](#def-b3-planetary-atmospheres-hydrodynamic) with $f = 1 \times 10^{-3}$ , in billions of years, to two significant figures.

**Solution of Problem 27.1.**

**1.** $g = GM/R^2 = 6.674 \times 10^{-11}\times5.2 \times 10^{24}/(6.2 \times 10^{6})^2 =
9.03\,\mathrm{m}\,\mathrm{s}^{-2}$; $\bar\rho = M/\tfrac43\pi R^3 = 5210\,\mathrm{kg}\,\mathrm{m}^{-3}$.

**2.** $v_\mathrm{esc} = \sqrt{2GM/r} = \sqrt{2\times3.47 \times 10^{14}/6.7 \times 10^{6}}
= 10.18\,\mathrm{km}\,\mathrm{s}^{-1}$.

**3.** $u = \sqrt{2kT/m}$: hydrogen $4.81\,\mathrm{km}\,\mathrm{s}^{-1}$, helium $2.41\,\mathrm{km}\,\mathrm{s}^{-1}$, oxygen $1.21\,\mathrm{km}\,\mathrm{s}^{-1}$.

**4.** $\lambda = (v_\mathrm{esc}/u)^2$: 4.49, 17.8, 71.2.

**5.** Only hydrogen: its escaping fraction is 0.06, helium’s $3.5 \times 10^{-7}$, oxygen’s $9 \times 10^{-30}$. None is near the hydrodynamic regime, $\lambda \approx 1.5$ to 3.

**6.** $\lambda = 4.49\times1400/3000 = 2.09$: within the transition; hydrogen would have streamed away hydrodynamically, perhaps dragging heavier gases.

**7.** $(1 + 4.49)\,e^{-4.49} = 0.0618$.

**8.** $n u/2\sqrt\pi = 2 \times 10^{11}\times4806/3.545 = 2.71 \times 10^{14}\,\mathrm{m}^{-2}\,\mathrm{s}^{-1}$; $\Phi_\mathrm J = 2.71 \times 10^{14}\times0.0618 = 1.68 \times 10^{13}\,\mathrm{m}^{-2}\,\mathrm{s}^{-1}$.

**9.** $4\pi(6.7 \times 10^{6})^2 = 5.64 \times 10^{14}\,\mathrm{m}^{2}$; $9.5 \times 10^{27}$ atoms per second.

**10.** $1.4 \times 10^{24}/18.015 = 7.8 \times 10^{22}\,\mathrm{mol}$, $4.68 \times 10^{46}$ molecules, $9.36 \times 10^{46}$ hydrogen atoms.

**11.** $9.36 \times 10^{46}/9.5 \times 10^{27} = 9.9 \times 10^{18}\,\mathrm{s}$, about 310 billion years.

**12.** $\lambda_\mathrm D = 4.49\times2.014/1.008 = 8.96$; escaping fraction $9.96\,e^{-8.96} = 1.28 \times 10^{-3}$; relative efficiency $0.707\times
1.28 \times 10^{-3}/0.0618 = 0.015$.

**13.** $H_a = kT/m_a g = 1.381 \times 10^{-23}\times200/(44.01\times1.661 \times 10^{-27}
\times9.03) = 4.18\,\mathrm{km}$.

**14.** $b = 1.2 \times 10^{21}\,\mathrm{m}^{-1}\,\mathrm{s}^{-1}$, so

$$
\Phi_\mathrm{DL} = \frac{b f(m_a - m_i)}{m_a H_a}
= \frac{1.2 \times 10^{21}\times1 \times 10^{-3}\times(42.0/44.0)}{4185}
= 2.74 \times 10^{14}\,\mathrm{m}^{-2}\,\mathrm{s}^{-1}.
$$

**15.** $3.0 \times 10^{13}\times1 \times 10^{-3}\times9.03/9.81 =
2.76 \times 10^{10}\,\mathrm{cm}^{-2}\,\mathrm{s}^{-1} = 2.76 \times 10^{14}\,\mathrm{m}^{-2}\,\mathrm{s}^{-1}$: the same within 1 %.

**16.** $4\pi(6.2 \times 10^{6})^2 = 4.83 \times 10^{14}\,\mathrm{m}^{2}$; $1.32 \times 10^{29}$ molecules of $\ce{H2}$, $2.64 \times 10^{29}$ atoms per second.

**17.** The diffusion limit supplies 28 times what the [exobase](#def-b3-planetary-atmospheres-exobase) lets out at its present density. Hydrogen piles up in the thermosphere until the Jeans flux matches the supply: in the long run the escape is diffusion-limited, as on the Earth.

**18.** $2 \times 10^{11}\times28 = 5.6 \times 10^{12}\,\mathrm{m}^{-3}$.

**19.** $4.68 \times 10^{46}/1.32 \times 10^{29} = 3.54 \times 10^{17}\,\mathrm{s}$, 11.2 billion years.

**20.** $S = 0.30/0.60^2 = 0.833$.

**21.** $d = \sqrt{L/S_\mathrm{eff}}$: inner edge $\sqrt{0.30/0.939} =
0.565\,\mathrm{au}$, outer edge $\sqrt{0.30/0.290} = 1.02\,\mathrm{au}$. Kepos, at $0.60\,\mathrm{au}$, is inside, close to the inner edge.

**22.** $0.939/0.833 = 1.13$: a brightening of 13 %.

**23.** $0.833\times1361\times0.7/4 = 198\,\mathrm{W}\,\mathrm{m}^{-2}$, $T_\mathrm{eq} =
(198/\sigma)^{1/4} = 243\,\mathrm{K}$; well below the $291\,\mathrm{W}\,\mathrm{m}^{-2}$ limit (computed for a Sun-like star, but the margin is wide).

**24.** Three times faster: 3.7 billion years.

**25.** **11 billion years**.