Mars has a carbon dioxide atmosphere with a surface pressure of only a few hectopascals, a surface of low thermal inertia and almost no ocean-like reservoir of heat. The ground and the air above it therefore warm and cool through a large range every sol, and the atmosphere answers with global oscillations locked to the Sun: the thermal tides. On Earth the tides are a small ripple on the surface pressure record. On Mars they are a leading feature of it, and they were among the first dynamical signals identified in the meteorological record returned from the surface (Leovy and Zurek, 1979).

Dust is the other defining element of Martian weather. Fine mineral particles are present in the air at all seasons, they absorb sunlight efficiently, and their heating shapes the temperature structure of the whole lower atmosphere (Gierasch and Goody, 1972). Storms that raise dust range from local events lasting a sol or two to planet-encircling storms that veil the surface for months, and the largest do not occur every year (Zurek and Martin, 1993). A comprehensive account of the dust cycle is given by Kahre et al. (2017).

The two subjects meet in a simple way. Tides are driven by heating, dust controls the heating, and tidal winds near the ground contribute to the stress that lifts dust. A loop of this kind invites the suggestion that tides help to start storms and not only respond to them. This review considers how well that suggestion is supported. It asks what theory predicts, what the observations show at the time of onset, and what numerical models add, and it separates the points on which the literature agrees from those still in dispute.

This is a narrative review of the published literature. It draws on the theoretical papers that adapted tidal theory to Mars, on analyses of lander and orbiter data, and on modelling studies that include dust lifting and transport. It is selective and does not attempt a complete catalogue of the field. The emphasis is on the lower atmosphere, taken here as the layer from the surface to a few scale heights, where lifting occurs and where the surface pressure signal of the tides is set. Tides in the upper atmosphere, which matter for aerobraking and for escape, are mentioned only where they bear on the lower levels. No new data or simulations are reported.

Classical tidal theory treats the tides as small oscillations of a stratified atmosphere on a rotating sphere, forced by periodic heating. The horizontal structure of each oscillation is described by Hough functions, the solutions of Laplace's tidal equation, and each has an equivalent depth that fixes whether it propagates vertically or stays confined near the level at which it is forced (Chapman and Lindzen, 1970). The theory carries over to Mars with little change because the planet's rotation period is close to that of Earth.

Lifting on Mars is hard. Because the air is so thin, the friction velocity needed to set sand grains moving is roughly an order of magnitude greater than on Earth, and such winds are uncommon (Greeley and Iversen, 1985). Particles of dust size are harder still to move directly, since cohesive forces between small grains rise as their weight falls. The usual view is that dust is raised mainly when saltating sand grains strike the surface, and that convective vortices supply a steady background of dust at times when the mean wind is too weak (Kok et al., 2012).

Two properties of this process matter for the present question. Lifting is a threshold phenomenon, so that a modest increase in wind stress can turn a quiet surface into a source. And the stress depends on the total wind, which is the vector sum of every circulation present: the seasonal mean flow, slope winds, travelling weather systems and the tides. Circulation models with a dust cycle represent lifting by wind stress and by dust devils with separate parameterisations, and the simulated storms are sensitive to the threshold chosen (Newman et al., 2002). A tidal wind that is too weak to raise dust alone may still decide whether the sum crosses the threshold.

Three kinds of observation bear on the link: pressure records at the surface, images and soundings from orbit, and the temperature and opacity climatologies that place individual storms in their seasonal setting.

General circulation models allow the pieces to be separated. The simulation of Wilson and Hamilton (1996) reproduced the Viking tidal record only when dust loading was raised to storm values and distributed deeply, which supports the reading of the semidiurnal tide as a measure of global dust. Models with interactive dust lifting go further. With a wind stress scheme and a suitable threshold, they generate storms spontaneously, including occasional global events, and some produce year-to-year variability without any change in external forcing (Basu et al., 2004). In such experiments the positive feedback on wind stress lifting is essential to storm growth, whereas dust devil lifting is self-limiting (Newman et al., 2002).

Models have limits that bear directly on the tidal question. Lifting occurs at gusts and on scales far below the grid, so the threshold in a model is a tuned quantity and not a measured one. Simulated tidal winds depend on the vertical distribution of dust, which most models prescribe or represent crudely, and on water ice clouds. A model can therefore show that tides are able to tip the balance toward onset without showing that they did so in any particular storm.

Three questions remain open. The first is causal order at onset. Pressure records show tides growing as dust arrives over a lander, but a lander samples one point, and the storm has usually started elsewhere. A network of surface stations with pressure and wind sensors, even a sparse one, would allow tidal wind to be compared with lifting at the source. The second concerns the near-surface wind itself. Almost all evidence about tidal winds is inferred from pressure, temperature or models, and direct wind measurements through a storm onset are rare.

The third question is interannual variability. Proposals include the slow redistribution of surface dust between source regions, intrinsic variability of the circulation, and a coupling between the planet's orbital motion and its rotation (Shirley, 2015). The last of these is debated. None of the proposals removes the need for a trigger in the right season, and for that the superposition of tides with fronts and slope winds remains the best documented mechanism. Continuous global sounding at several local times, which sun-synchronous orbiters cannot provide, would let the tides be separated cleanly from other variations and is perhaps the single most useful observational advance in prospect.

The literature gives a consistent account on two points. Thermal tides in the lower Martian atmosphere strengthen promptly when dust loading rises, the semidiurnal tide most reliably, and this response has been seen by every long-lived lander. Tidal winds also contribute to onset by adding to frontal, slope and seasonal winds at particular places and local times, as the cross-equatorial storms show most clearly. The stronger claim, that tides start large storms unaided, is not supported. They are better regarded as one necessary contributor to a threshold process, and as the fastest link in the feedback that lets a regional storm grow. Deciding how much of the year-to-year difference in storm activity they explain will need wind measurements at the surface and soundings that cover the full daily cycle.

To be declared by the author(s) before publication.

To be declared by the author(s) before publication.