the Creative Commons Attribution 4.0 License.
the Creative Commons Attribution 4.0 License.
How many modes are needed to predict climate bifurcations? Lessons from an experiment
Bérengère Dubrulle
François Daviaud
Davide Faranda
Louis Marié
Brice SaintMichel
According to everyone's experience, predicting the weather reliably over more than 8 d seems an impossible task for our best weather agencies. At the same time, politicians and citizens are asking scientists for climate projections several decades into the future to guide economic and environmental policies, especially regarding the maximum admissible emissions of CO_{2}. To what extent is this request scientifically admissible?
In this review we will investigate this question, focusing on the topic of predictions of transitions between metastable states of the atmospheric or oceanic circulations. Two relevant examples are the switching between zonal and blocked atmospheric circulation at midlatitudes and the alternation of El Niño and La Niña phases in the Pacific Ocean. The main issue is whether present climate models, which necessarily have a finite resolution and a smaller number of degrees of freedom than the actual terrestrial system, are able to reproduce such spontaneous or forced transitions. To do so, we will draw an analogy between climate observations and results obtained in our group on a laboratoryscale, turbulent, von Kármán flow in which spontaneous transitions between different states of the circulation take place. We will detail the analogy, investigate the nature of the transitions and the number of degrees of freedom that characterize the latter, and discuss the effect of reducing the number of degrees of freedom in such systems. We will also discuss the role of fluctuations and their origin and stress the importance of describing very small scales to capture fluctuations of correct intensity and scale.
The present review paper is based on the lecture delivered by Bérengère Dubrulle on the occasion of her reception of the Lewis Fry Richardson Medal 2021. The story around this lecture started back in the year 2000, when Bérengère became interested in climate change and started discussions with colleagues at the Laboratoire des Sciences du Climat et de l'Environnement (LSCE). She was intrigued by a strange behaviour of the temperature curves discussed in the IPCC reports: they all exhibited a constant, quasilinear increase with time, linearly following the rise of CO_{2} concentration. Given that the perturbation of the CO_{2} concentration was far from being negligible (we were talking about doubling it) and that climate is a highly nonlinear system, she was wondering why the output of climate models did not show at the time any sign of a nonlinear response. It was surprising as her research group routinely observed nonlinear behaviour such as bifurcations or saturations in experimental setups or in numerical simulations of turbulent flows.
She became all the more puzzled as the climate community was starting to acknowledge the possibility of occurrence of tipping points (Russill and Nyssa, 2009; Russill, 2015). In particular, some of her frequent interlocutors like Didier Paillard, Pascal Yiou, or Gilles Ramstein showed her interesting occurrences of bifurcations in lowdimensional models of the atmosphere (e.g. the Stommel model, Stommel, 1961) or spontaneous abrupt transitions in (proxies of) temperature records during the last hundreds of millennia (see Fig. 1). More recently, multistability and bifurcations were also observed in a simplified climate model (Margazoglou et al., 2021).
On the other hand, the climate science community has achieved considerable success in predicting the increase in Earth average temperatures in the last few decades. This success shows that present climate models, though still incomplete and perfectible, capture the correct evolution of atmospheric or oceanic circulation, at least in terms of largescale features and most probable events. Recent versions of climate models also include nonlinear effects on oceanic circulation (Boucher et al., 2020), vegetation (Guimberteau et al., 2018), and icesheet dynamics (Le Clec'h et al., 2019). They also better represent the energy and water cycles, including more physical constraints on conservation laws (Irving et al., 2021). They are therefore able to capture nowadays some nonlinear interactions between the different components of the climate system, i.e. the El Niño–Southern Oscillation (ENSO) feedback to atmospheric motions (Bayr et al., 2020), monsoons (Yang et al., 2019), or stratospherictotropospheric interactions (Olsen et al., 2007). Geophysicists are therefore studying extensively the nonlinear properties of the different components of the climate system (atmosphere, hydrosphere, lithosphere, biosphere, and cryosphere) that appear ubiquitously.
In the atmosphere, characterizing the geometry and the dynamics of the polar jet is still an open problem, as it can be in an almost zonally symmetric state with strong zonal currents associated with trains of extratropical cyclones or in broken, flowerlike, socalled “blocked” states which induce hot or cold waves depending on the season and the geography (Serra et al., 2017). Despite the great increase in computational power of climate models, the switching between the two main phases of the jet is still difficult to characterize statistically and dynamically (Faranda et al., 2019b). It is therefore complicated to determine its evolution under climate change.
In fact, nonlinear phenomena arise in all the “spheres”. In the ocean, while ENSO is reproduced by most models, correctly reproducing the magnitude and frequency of its occurrence is still challenging, and the fate of the thermohaline circulation remains to be determined, whereas the biosphere is a mine of nonlinear interactions between living species directly breathing the nonlinear atmospheric chemistry and reacting nonlinearly (losing leaves, migrating, hibernating, etc.) to changes in their physical environment.
Considering all that, it appeared clear to Bérengère that the richness of nonlinear interactions in climate needed to be further understood, and she had a feeling that laboratory experiments of turbulence could help guide intuition regarding the role of such nonlinearities in climate bifurcations, as already demonstrated earlier by Weeks et al. (1997) and the work of Hide (Ghil et al., 2010).
This review is the story of the long journey she undertook with four main collaborators into theoretical, laboratory, and numerical explorations to try and understand these mysterious apparent contradictions and examine how many modes it takes to capture transitions in climate models.
Simulating climate is an arduous task, for we need to describe the interaction of fluid envelopes (atmosphere, ocean) with the lithosphere, cryosphere, and biosphere under solar forcing. This makes the climate a nonequilibrium nonlinear and complex system. “Complex” here means that there are several interacting scales at which the energy is accumulated and distributed in space, time, and towards other scales through energetic processes that are visible to humans as meteorological and oceanic phenomena, e.g. cyclones, thunderstorms, marine currents, or iceberg breakoff. How many degrees of freedom are needed to take into account this complexity is still an open question. The number we choose is therefore fixed by necessity (i.e. by computing capabilities) rather than by reason. Let us take for example the case of the fluid envelopes.
Their basic physics obey the nonlinear, partial differential equations proposed by Navier and Stokes 200 years ago. They describe the dynamics of a velocity field u(x,t) under the action of a pressure field, viscous dissipation, and stirring by volume forces. From the work of Kolmogorov on turbulence (Kolmogorov, 1991), hereafter referred to as the K41 theory of turbulence, we know that the balance between forcing and dissipation results in a selfsimilar organization of the fluid. Kinetic energy is injected at scale L_{f} and is transferred at a constant rate ϵ by the energy flux down to the scale η where the energy flux becomes compensated by the viscous flux, with $\mathit{\eta}=({\mathit{\nu}}^{\mathrm{3}}/\mathit{\u03f5}{)}^{\mathrm{1}/\mathrm{4}}$ and ν the viscosity. At smaller scales, the energy flux is transported by the viscous processes to the smallest hydrodynamic scale, where it is dissipated into heat. A turbulent flow then displays vortices of all sizes in between L_{f} and η, and its energy spectrum scales like $E\left(k\right)\sim {\mathit{\u03f5}}^{\mathrm{2}/\mathrm{3}}{k}^{\mathrm{5}/\mathrm{3}}$. This means that if we want to capture the flow physics (e.g. location of vortices and their dynamics in the flow, energy dissipation, interplay between vortices at different scales), we need to discretize the Navier–Stokes equations on a grid that is $({L}_{\mathrm{f}}/\mathit{\eta})\times ({L}_{\mathrm{f}}/\mathit{\eta})\times ({L}_{\mathrm{f}}/\mathit{\eta})$, containing a priori $N\sim ({L}_{\mathrm{f}}/\mathit{\eta}{)}^{\mathrm{3}}$ degrees of freedom (as we shall discuss later, the actual number may even be larger). If we put numbers corresponding to the atmosphere (L=10^{3} km, η=10 mm) and take into account the anisotropy (Schertzer and Lovejoy, 1991), we get an astronomical number, N∼10^{27}, larger than the Avogadro number. Reading in or writing out this volume of data at each time step to advance the flow would take 73 billion years of CPU time at the pace of the fastest massively parallel computers.
In recent years there have been developments in understanding that this computational nightmare can be partially solved by applying neural networks or, more generally, machine learning approaches (see e.g. Pathak et al. (2017, 2018) for artificial intelligence methods applied to the behaviour of chaotic systems). We would like to stress that these approaches are never holistic and often target a specific subset of spatial and temporal scales of the climate systems, e.g. the prediction of geophysical data (Wu et al., 2018), the parameterizations of subgrid processes in climate models (Krasnopolsky et al., 2005; Krasnopolsky and FoxRabinovitz, 2006; Rasp et al., 2018; Gentine et al., 2018; Brenowitz and Bretherton, 2018, 2019; Yuval and O’Gorman, 2020; Gettelman et al., 2020; Krasnopolsky et al., 2013), the forecasting (Liu et al., 2015; Grover et al., 2015; Haupt et al., 2018; Weyn et al., 2019; Faranda et al., 2021) and nowcasting (i.e. extremely shortterm forecasting) of weather variables (Shi et al., 2015, 2017; Sprenger et al., 2017), and the quantification of the uncertainty of deterministic weather prediction (Scher and Messori, 2018). The greatest challenge of entirely replacing the equations of climate models with neural networks capable of producing reliable long and shortterm forecasts of meteorological variables has, to the best of our knowledge, not yet been achieved with these methods.
We are then led by necessity to simulate far fewer degrees of freedom, typically a few thousands in the atmosphere or ocean for recent climate models. How reasonable is this drastic reduction of the number of degrees of freedom? It now depends on the flow physics: the selfsimilar energy spectrum is an indication that some scales or modes may play a more prominent role than others. So, maybe, the theoretical $N\sim ({L}_{\mathrm{f}}/\mathit{\eta}{)}^{\mathrm{3}}$ figure overestimates the actual number of modes that are needed to represent the flow dynamics, and we could circumvent the computational obstacle by a clever selection of grid points or modes. In 1963, a pioneer study by Lorenz (1963) showed that only three modes were necessary to obtain chaotic behaviour on an attractor and reproduce some key dynamical effects observed in Rayleigh–Bénard convection, an essential ingredient of atmospheric dynamics. More generally, it is thought that if we were able to understand what the “attractor” of the climate dynamics is, then the number of modes we would need is simply the dimension of such an attractor. However, both the computation of the attractor for climate and the identification of the independent variable sufficient to describe it are still highly debated issues that remain far from being solved theoretically (Faranda et al., 2019a; Falasca et al., 2019; Brunetti et al., 2019).
Climate models therefore use a simpler idea and currently select modes based on length scales: the idea is that the largest scales are very energetic and do not directly feel the viscosity, which becomes active only at scales of the order of η. The large scales are however indirectly influenced by the viscosity through their interaction with the small scales, which play the role of a “turbulent viscosity” with respect to the large scales. The concept of turbulent viscosity is therefore akin to a clever renormalization procedure that takes care of the energy accumulation taking place at the cutoff scale (Forster et al., 1977; Frisch et al., 1980; Herring et al., 1982). Hence, current climate models only keep the largest modes and add a “turbulent viscosity” to take into account the influence of the small scales. The magnitude of the turbulent viscosity is known to depend on the cutoff scale since Richardson (Richardson and Walker, 1926) and is usually significantly higher than the classical Newtonian viscosity of the fluids under study: for a cutoff scale of the order of a few hundred kilometres – the smallest scale that climate models can currently solve without saturating memories of modern supercomputers – turbulent viscosities are equivalent to the Newtonian viscosity of tar in the atmosphere, while in the ocean, they are equal to that of honey.
Replacing air and water with tar and honey does not look too appealing. Moreover, there are a lot of more complex processes like beating/backscatter/intermittency (Forster et al., 1977; Frisch et al., 1980; Herring et al., 1982) that cannot be taken into account by a simple “turbulent viscosity”, yet numerical simulations based on these assumptions provide a fairly realistic picture of the past and present states of circulation in the ocean and in the atmosphere (Flato et al., 2013). There is therefore a rationale in this procedure that we should try to understand and improve. To do so, we considered a laboratory model experiment that retains some essential properties of natural flows (forcing, dissipation, symmetries, wide range of spatial and temporal scales) but with simple boundary conditions and few interacting components in order to limit the number of relevant observables to be analysed. To some extent, this is similar to the simplification obtained by considering a perfect monoatomic gas to describe a real gas.
Our experimental setup is summarized in Fig. 2: we consider a transparent cylindrical tank of aspect ratio 1.8 filled with water. The tank is closed at each end by two coaxial and counterrotating impellers with curved blades. Such a device provides a very efficient, inertial stirring of the liquid inside the tank, which easily reaches speeds of the order of 1m s^{−1} for an impeller rotation frequency of 10 Hz in a 10 cm radius tank. The flow produced in the device (called von Kármán flow) is highly turbulent, characterized by a Reynolds number in water around 10^{6} – about 1000 times lower than in the atmosphere. We characterize the flow using two complementary types of measurements.

The torque or velocity applied by each of the impellers to the turbulent flow. These are global measurements of the state of the system.

Local velocity maps obtained using stereoscopic particle image velocimetry (sPIV). These measurements give us access to the three instantaneous components of the velocity field in a vertical plane crossing the centre of the experiment with an acquisition rate of about 15 Hz. This rate is insufficient to resolve in time all turbulent scales but offers reliable statistics on the velocity field, obtained by averaging several thousands of instantaneous maps.
Averaging a large number of instantaneous velocity fields during statistically steady regimes allows us to observe the mean flow established in the geometry. It takes the form of a largescale circulation carrying the vertical angular momentum from one impeller to the other. This circulation is analogous to the atmospheric or thermohaline circulation, transporting heat from the Equator to the pole, under the action of either solar radiative forcing and/or surface forcing by winds. The analogy is summarized in Table 1.
We have used our von Kármán setup in two complementary forcing modes. In the first mode, the rotation rates of the impellers are kept fixed. In this case one can set the mean rotation rate of the impellers, $({f}_{\mathrm{1}}+{f}_{\mathrm{2}})/\mathrm{2}$, but also the normalized rotation rate difference of the impellers, $\mathit{\theta}=({f}_{\mathrm{1}}{f}_{\mathrm{2}})/({f}_{\mathrm{1}}+{f}_{\mathrm{2}})$. The former quantity governs the total angular momentum – along the vertical axis – present in the fluid. The latter parameter offers a fine control of the degree of ℛ_{π} symmetry of the flow forcing. Such a forcing mechanism is analogous to convective Rayleigh–Bénard systems with fixed temperature gradients. However, in natural systems, the forcing is rather done by imposing the heat flux that traverses the system (due to solar radiation). We have thus also performed experiments in a second forcing mode in which we controlled the torque applied to the von Kármán flow by the impellers. In this mode, the mean torque $({c}_{\mathrm{1}}+{c}_{\mathrm{2}})/\mathrm{2}$ is a measure of the vertical angular momentum flux from top to bottom, while the reduced difference $\mathit{\gamma}=({c}_{\mathrm{1}}{c}_{\mathrm{2}})/({c}_{\mathrm{1}}+{c}_{\mathrm{2}})$, which prescribes the dissipation of angular momentum at the cylinder wall, also controls the level of ℛ_{π} symmetry of the forcing mechanism. In principle, a mixed forcing type in which the rotation rate of one impeller and the torque of the other one are fixed is also possible, but we have not yet explored the behaviour of the system in this case.
One can control the degree of perturbation in the von Kármán flow by controlling the level of velocity fluctuations for a given set of forcing conditions and viscosity. This may be achieved by changing the curvature of the impeller blades, which will be used as an analogue of changes in CO_{2} concentration in natural flows.
We can also change the number of degrees of freedom in the von Kármán flow by considering more or less viscous fluids, going from N∼10^{13} for a waterfilled experiment at Re∼10^{6} down to N∼10^{4} for a glycerolfilled experiment at Re∼10^{2}. This is an experimental equivalent of the reduction of the number of degrees of freedom that is explicitly done when using turbulent viscosities in present numerical simulations of atmospheric or oceanic circulation. Eventually, the only major difference between natural flows and the von Kármán flow is the symmetry of the geometry, which is spherical rather than cylindrical. From the point of view of a theoretical physicist, though, this difference only affects the detailed shape of the circulation.
4.1 Flow symmetries and circulation topology
In the von Kármán system, vertical angular momentum of opposite signs is injected by the top and bottom impellers. The resulting imbalance produces a largescale meridional circulation analogous to the largescale oceanic and atmospheric circulations between the Equator and the poles. The topology of the largescale circulation is strongly influenced by the symmetries of the experimental setup. Arbitrary rotations around the cylinder axis obviously leave the experimental setup invariant. Its symmetry group thus contains the symmetry group of the oriented circle, the special orthogonal group SO(2). This symmetry usually carries over, in the timeaveraged sense, to the large scales of the flow. Another basic symmetry of the system is the ℛ_{π} symmetry, which exchanges the two impellers by rotation of 180^{∘} around any axis of the middle plane which intersects the cylinder axis (the “hourglass reversal” symmetry; see Fig. 2). When the two impellers rotate at exactly the same frequency f_{1}=f_{2}, corresponding to a relative speed difference $\mathit{\theta}=({f}_{\mathrm{1}}{f}_{\mathrm{2}})/({f}_{\mathrm{1}}+{f}_{\mathrm{2}})=\mathrm{0}$, the system is strictly symmetric with respect to ℛ_{π} and its symmetry group is the (general) orthogonal group O(2). When θ≠0, ℛ_{π} is broken and the experiment symmetry group reduces to the special orthogonal group SO(2). The latter is the (connected) component of O(2) whose elements have +1 determinants, the other component having determinants −1. This explains how O(2) reduces to SO(2) with the breakdown of rotational symmetry. Except on “Aquaplanets” (Ferreira et al., 2011), the symmetry group of the continents is trivial. If one neglects the continental influences, the symmetry group of the atmosphere is SO(2)×ℤ_{2} (rotations around the polar axis and mirror symmetry with respect to the Equator), while the symmetry group of each hemisphere taken separately is SO(2). These symmetry considerations guide us in our search for analogies between the von Kármán system and the Earth system: in some respects, the symmetry group of the ℛ_{π}asymmetric von Kármán flow is the same as the symmetry group of the atmosphere in a single hemisphere, and insight gained in the study of vertical angular momentum transport in the von Kármán flow may be expected to carry over to the transport of heat from the Equator to one pole in the natural atmosphere.
However, it is well known that the distinct distribution of continental masses between the two hemispheres or the insulation distribution on seasonal timescales breaks the mirror symmetry of the Earth with respect to the Equator. The SO(2)×ℤ_{2} symmetry of the Earth system is thus in fact quite imperfect and in some respects closer to the SO(2) symmetry of the von Kármán flow in ℛ_{π}asymmetric conditions. It can thus be hoped that some aspects of the von Kármán flow could also bear resemblance to phenomena involving the Earth system as a whole, such as the seasonal motion of the Intertropical Convergence Zone at the boreal summer–austral summer transitions, the oceanic thermohaline circulation, or the glacial–interglacial climate transitions.
The different largescale flow configurations observed in the von Kármán flow in the rotationratecontrolled mode when θ is varied are represented in Fig. 3. For large negative (Fig. 3b) or positive (Fig. 3c) values of θ, ℛ_{π} is unambiguously broken, and the flow is in a SO(2) configuration consisting of a single cell rotating in the direction of the fastest impeller (the analogue of a direct Equator–pole atmospheric meridional circulation in a single hemisphere, of an austral or boreal summer with grossly exaggerated interhemisphere asymmetry, or of a glacial episode). In this case the total mean vertical angular momentum $\langle I\rangle =\langle \int r{u}_{\mathit{\theta}}\phantom{\rule{0.125em}{0ex}}\mathrm{d}V\rangle $ follows the sign of θ. Negative 〈I〉 corresponds to b_{−} states (“austral summer”, henceforth “A” states), whereas positive 〈I〉 corresponds to b_{+} states (“boreal summer”, henceforth “B” states). The B state obtained for a value of θ is transformed by ℛ_{π} into the A state obtained for −θ.
When θ becomes close to 0, the configuration obtained is closer to ℛ_{π} symmetry: it consists of two toroidal recirculation cells arranged on either side of the median plane, rotating in opposite azimuthal directions (Fig. 3a). The two halves of the von Kármán flow are almost ℛ_{π}symmetric images of one another, and the total mean vertical angular momentum is close to zero: 〈I〉≃0. In a way, the situation can also be said to resemble the global Earth system in which the two hemispheres are approximately images of one another by reflection across the equatorial plane separated by an interface that shifts gradually as the symmetry of the forcing is varied (in analogy to the seasonal cycle of insulation, which brings the latitude of maximal solar energy input into the Earth system alternatively in the two hemispheres). This situation is thus reminiscent of a “spring” or “autumn” transition situation (henceforth “T” state) or of an interglacial situation.
However, the situation in that case can also be considered to be analogue to the atmospheric situation in a single hemisphere: it consists of two toroidal recirculation cells arranged on either side of a transition plane, separated by a highly turbulent shear layer – a configuration somewhat equivalent to the Hadley circulation of the atmosphere: positive vertical angular momentum fluid is confined to the lower half of the cylinder, negative vertical angular momentum fluid is confined to the upper half, and vertical angular momentum transport between the two is only mediated by the turbulent fluctuations, which have a visual appearance strikingly similar to that of synopticscale atmospheric disturbances. This situation prevails for small values of the impeller rotation rate imbalance θ, for which the midplane shear layer (analogue of the midlatitude “storm track”) shifts continuously in “latitude” as θ varies, moving gradually away from the fastestrotating impeller.
4.2 Seasonal cycle in the water experiment
Given the properties of the largescale circulation, we are therefore able to produce the equivalent of a “seasonal cycle” in our experiment by modulating the forcing asymmetry as a function of time θ(t). This modulation reflects the yearly modulation of the heat flux imbalance between the poles and the Equator as the Earth revolves around the Sun. An example of the reaction of the mean vertical angular momentum 〈I〉 to such a seasonal cycle in the von Kármán water experiment is shown in Fig. 4a. On average, the flow responds continuously – yet in a nonlinear fashion – to the forcing imbalance θ: the shift between the A and B states is progressive, as observed on Earth. Indeed, boreal summer and austral summer circulations have different characteristics on our planet, and they are often studied separately (Vrac et al., 2014). For a given value of θ, the instantaneous value of I is however fluctuating, as illustrated in Fig. 4b, and similarly to the fluctuations of the daily temperatures on Earth.
4.3 Transitions induced by changes in the velocity fluctuation intensity
We can now apply a perturbation to our system by imposing highervelocity fluctuations (“increasing CO_{2}”) using blades that are more curved. In that case, we observe an interesting bifurcation: when the level of fluctuations is sufficiently high, the seasonal cycle becomes discontinuous and the transition between the A and B states becomes brutal, with a jump in the global mean vertical angular momentum 〈I〉, as seen in Fig. 5. In addition, this discontinuous seasonal cycle shows hysteresis: once we have switched to one of the summer branches, if we decrease again θ, the flow jumps directly to the other summer branch without going through the T state (Ravelet et al., 2004; Ravelet, 2005). Once the flow is in one of the two summer states, its configuration remains the same permanently unless the parameters of the forcing are changed. The transition from one of the summer states to the T state seems forbidden, and we have never been able to observe it.
The symmetric T state is then particulary difficult to reach, as it becomes marginally stable: starting from a symmetric state at θ∼0, the flow switches to either of the summer states after a time that diverges as θ^{−6} (Ravelet, 2005). Thus, the lifetime of the twocell symmetric state is then drastically shortened even for small values of θ. This observation is reminiscent of what happens on Earth. For the atmospheric circulation, recent studies suggest that increasing fluctuations and concentrations of CO_{2} disrupt the shoulder season dynamics. In Cassou and Cattiaux (2016), a clear example of this disruption of seasons is provided, whereas an analysis of the way in which altering greenhouse gas concentration disrupts the proportion of zonal vs. blocked states of the atmospheric dynamics is provided in Faranda et al. (2019a).
4.4 Spontaneous jumps between circulation states under a fixed torque difference
Up to now, we focused on circulation changes induced by externally imposed changes in impeller rotation rate imbalance θ: these are forced transitions, similar to the ones caused by changes in solar radiation on Earth, resulting in seasonal cycles or glacial–interglacial transitions. However, the von Kármán flow is actually even more interesting. Using another type of forcing, which is actually closer to the forcing conditions of the natural flows on Earth, we also observed interesting spontaneous transitions of the circulation (Marié, 2003; Ravelet, 2005; SaintMichel et al., 2013). In this situation we set the torque imbalance applied by the impellers to the fluid $\mathit{\gamma}=({c}_{\mathrm{1}}{c}_{\mathrm{2}})/({c}_{\mathrm{1}}+{c}_{\mathrm{2}})$, imposing a constant flux of vertical angular momentum in the experiment. The new type of dynamics only happens when the level of fluctuations is sufficiently high. It is illustrated in Fig. 6, where we observe spontaneous transitions between a summer state and the T state. The transitions can be quasiperiodic (case a) or very rare (case b), depending on the value of γ. They can be viewed as a laboratory equivalent of “weather regimes” (Vautard, 1990), of El Niño events, or of the Heinrich events of Fig. 1.
These observations show that fast spontaneous transitions between longlived states may arise in a complex system with many degrees of freedom and large fluctuations even when the external forcing does not vary as a function of time. Similar transitions could then occur in the atmospheric and oceanic circulation on Earth should the level of perturbations – our greenhouse gas emissions – become sufficiently high. Current models employ forcing functions for solar dynamics and CO_{2} concentration that possess a smooth structure, and bifurcations and sharp transitions in climate models are avoided. The von Kármán analysis shows however that smallscale fluctuations are important for the largescale dynamics, because they can trigger sudden transitions in macroscopic states.
4.5 The lowdimensional attractor
Despite their apparent complexity, the spontaneous transitions can actually be characterized by lowdimensional objects called attractors. This is illustrated in Fig. 7, where we show the joint probability density function (PDF) with simultaneously a rotation frequency f_{1} at the top and f_{2} at the bottom impeller. Each subplot of Fig. 7 corresponds to a different value of the torque imbalance γ. We see that in each case the joint PDF concentrates on a welldefined set, which we call the attractor. It can be a round blob, reflecting the existence of a fixed point in the dynamics (cases a and f) where the circulation remains either in the spring or summer state, or a more extended object, corresponding to transitions between the states. We have checked (SaintMichel, 2013; SaintMichel et al., 2013) that the transitions between states follow on average the same paths (delineated by the coloured arrows in subpanels c and d). Using tools from the dynamical system community, we have been able to prove that all these observations were consistent with the existence of an attractor resulting from the coupling of the periodic forcing of the classical deterministic Duffing attractor (2D) with a Langevin equation (1D). Moreover, the attractor has a fractal dimension between 3 and 10 (Faranda et al., 2017). This fractal dimension is very small compared to the number of degrees of freedom of the system N∼10^{13}. This study has motivated the development of a minimal model of the effective dynamics of the midlatitude jet stream (Faranda et al., 2019b). This model has been used to explore a range of possible behaviours beyond those displayed in the available data that could have appeared in past climates and could appear again in future climates. Similarly to the model derived by Faranda et al. (2017) for the von Kármán turbulent flow, the jet model is based on a coupled map lattice. Each element of the lattice reflects the dynamics of the jet at a given longitude. Stochastic forcing is used to simulate the alternation of cyclones and anticyclones, the geography, and the smallscale dynamics.
The existence of a lowdimensional stochastic attractor in the experiment illustrates the fact that some degrees of freedom are probably not necessary to capture the bifurcations. It leaves the hope that maybe the essential features of the bifurcation will remain even if we decrease the number of degrees of freedom. So, let us see what happens when we reduce the number of degrees of freedom by increasing the viscosity, which is what is done in climate models when turbulent viscosity is introduced.
4.6 Circulation properties in glycerol
We have therefore conducted additional studies in the von Kármán cell filled with glycerol. This amounts to reducing the degrees of freedom to ∼10^{4}, a number 2 orders of magnitude larger than the dimension of the stochastic attractor. In this reduced system, we observe again three different states, one symmetric with respect to the ℛ_{π} symmetry and two states that are exchanged by applying the ℛ_{π} symmetry. They are shown in Fig. 8. They have the same global topology as the equivalent states in the full system even though they differ in details: for instance, the global rotation of the fluid is significantly more localized in the summer states and only extends to the vicinity of the rotating impeller.
One can also produce a forced seasonal cycle in this configuration by varying θ and examining the associated variations of the vertical angular momentum 〈I〉, as shown in Fig. 9a. One sees that the seasonal cycle 〈I〉(θ) is continuous from winter to summer, similarly to the case of the full system with low fluctuations. The seasonal cycle also looks almost linear in θ, and smaller differences in the vertical angular momentum 〈I〉 are seen between summer and winter.
The instantaneous global vertical angular momentum I(t) (displayed in Fig. 9b) shows very small fluctuations as a function of time regardless of the impeller frequency imbalance θ: the fluctuations corresponding to the varying daily temperatures are suppressed. In this reduced system, we are thus able to capture forced circulation transitions but not the shortterm fluctuations of the observable: in other words, we are able to conduct “climate” experiments (testing the switching between glacial and interglacial state) but not weather experiments (reproducing the daily temperature records) or amplitude of transition between summer and winter.
In a sense, this is quite an achievement: with a much smaller number of modes than the real system, we are able to forecast the dynamics of natural systems at a climatic level. Is this really so? Given that the number of degrees of freedom is still larger than the dimensions of the stochastic attractor, we may think that we should also be able to capture the bifurcations and the dynamics when switching to more curved blades and imposing a torque imbalance.
This hope however was shattered by our experiments: at high viscosity, the multiplebranch region of Fig. 5 disappears (Ravelet, 2005; SaintMichel, 2013; SaintMichel et al., 2013) along with the bifurcations and their associated dynamics, as shown in Fig. 10. The contrast with the flow in water – the full system – is striking: not only does the stochasticity disappear (a reasonable observation if we believe that stochasticity is induced by the small scales), but so does the attractor itself. This means that our way of separating the large and small scales is not suitable for our system, as it has suppressed some of the degrees of freedom that are essential for the largescale dynamics. Instead, one has to pick up carefully chosen large, intermediate, and small scales to represent both the attractor and the transitions between its branches. The question of how to do it is however still open and left for future work.
We have seen in the previous section that the smallscale velocity fluctuations are essential to get the rich transition dynamics between metastable states. The usual mental image invoked in such cases is that of an “energy” landscape (Fig. 11) in which the summer and spring states are represented by potential wells of different depths. Once the system is e.g. in the spring state (at position x_{−}), it can only jump towards the other potential well (at location x_{+}) following fluctuations exceeding the energy barrier ΔU_{0}. This classical problem of stochastic processes results in an exponential distribution of escape times from the potential well that we have observed experimentally (Ravelet, 2005). This kind of scenario has also recently been observed in the stochastically forced PLASIM model of climate (Margazoglou et al., 2021).
How does one get fluctuations of sufficient amplitude to trigger these transitions? Let us take a closer look at fluctuations in our von Kármán flow. They are shown in Fig. 11a, from data issued from a direct numerical simulation of our experiment by Hugues Faller and collaborators, using the SFEMANS code (Cappanera et al., 2020). Large velocity fluctuations are primarily observed at two locations: one close to the “corner” of the experiment (i.e. close to the impellers and the outer wall) and the second at midheight. The first location obviously corresponds to the fluctuations induced by the moving boundary conditions which are then advected by the mean velocity of the spring state of Fig. 3a. The second location is associated with a strong shear layer resulting from the counterrotation of the two main toroidal cells of the spring state. We then observe, in agreement with our physical intuition, that larger velocity gradients produce stronger velocity fluctuations.
What is the physical process that generates strong velocity gradients in a turbulent flow? Obviously not the viscous dissipation, which has the opposite effect of smearing out such gradients. In fact, only the nonlinear term of the Navier–Stokes equations (u⋅∇)u can produce finer length scales through triadicmode interactions. At a given scale, the intensity of the effect of the nonlinear term can be estimated through the “local energy transfer” term defined as ${\mathrm{\Pi}}_{\mathrm{\ell}}={\mathrm{\nabla}}_{\mathrm{\ell}}{\stackrel{\mathrm{\u203e}}{({\mathit{\delta}}_{r}u{)}^{\mathrm{3}}}}^{\mathrm{\ell}}$, where ${\mathit{\delta}}_{r}u=u(x+r)u\left(x\right)$ is the velocity increment over a distance r and ${\stackrel{\mathrm{\u203e}}{x}}^{\mathrm{\ell}}$ indicates that we average the distance r over a ball of size ℓ centred on x. Indeed, this term provides the contribution of nonlinear interactions to the energy budget and provides the quantity of energy that is transferred through scales (Dubrulle, 2019). In other words, the larger Π_{ℓ}, the higher the energy cascade towards smaller scales and the stronger the final gradient (and velocity fluctuations) at this location. The quantity Π_{ℓ} is shown in Fig. 12b): as expected, areas of large velocity fluctuations correspond to areas of large local energy transfers Π_{ℓ}.
5.1 Scaling exponents and intermittency
Can we quantify the connection between strong velocity fluctuations and large energy transfer events in a more rigorous way? To do so, we can introduce a local diagnostic quantity that will prove useful in the understanding of the local dynamics of the energy transfer. It is the “local scaling exponent”, defined as $h=\mathrm{ln}\left(\right{\mathit{\delta}}_{r}u\left\right)/\mathrm{ln}\left(r\right)$, or equivalently, $\left{\mathit{\delta}}_{r}u\right\sim {r}^{h}$. This quantity is connected to the mathematical notion of Hölder continuity, which provides a weaker regularity condition than differentiability. A given velocity field is Hölder continuous with some exponent h<1 (i.e. not necessarily differentiable) at small scales if the following holds:
We see that Hölder continuity uses the velocity increment δ_{r}u as a building block. This is interesting, as a classical result by Kolmogorov states that under stationarity and homogeneity conditions, the mean energy flux of a solution of Navier–Stokes equations is constant in the inertial range
where ϵ is the global energy dissipation. Integrating this over scale, one gets $\langle {\left(\mathit{\delta}\mathit{u}(\mathit{x},\mathrm{\ell})\right)}^{\mathrm{3}}\rangle =(\mathrm{4}/\mathrm{3})\mathit{\u03f5}\mathrm{\ell}$ for ℓ in the inertial range. This is called the Kolmogorov $\mathrm{4}/\mathrm{3}$ law. If signed and unsigned (with absolute values) values of velocity increments were equivalent and the turbulence were fully homogeneous, this would suggest that $h\sim \mathrm{1}/\mathrm{3}$ for scales in the inertial range: turbulence would be a monofractal, with exponent $h=\mathrm{1}/\mathrm{3}$.
However, these two hypotheses are violated. First, it is clear that unsigned moments converge much more rapidly and easily than signed moments, as the latter are prone to cancellation effects and sensitive to large fluctuations of positive or negative values. Due to these phenomena, signed moments are sensitive to possible subleading correction to scaling and are avoided by taking the absolute value. In that sense, the local scaling exponent we define is more robust but maybe less sensitive to subtle scaling effects like oscillatory scaling behaviour. In the von Kármán flow, we have checked that indeed $\langle {\left(\mathit{\delta}\mathit{u}(\mathit{x},\mathrm{\ell})\right)}^{\mathrm{3}}\rangle \sim \mathrm{\ell}$ while $\langle \left\mathit{\delta}\mathit{u}\right(\mathit{x},\mathrm{\ell}){}^{\mathrm{3}}\rangle \sim {\mathrm{\ell}}^{\mathrm{0.8}}$ (Faller et al., 2021). Second, we have observed that at small scale, the turbulence is strongly inhomogeneous (Faller et al., 2021), so that it is not clear that a single exponent can be sufficient to describe the flow.
While we cannot consider the $\mathrm{4}/\mathrm{3}$ law to be an exact constraint pointing to $h=\mathrm{1}/\mathrm{3}$, we can still find a relic of such a value using the scale dynamics of turbulence. Indeed, from dimensional analysis, it is possible to show that the local energy transfer scales like ${\mathrm{\Pi}}_{\mathrm{\ell}}\sim {\mathrm{\ell}}^{\mathrm{3}h\mathrm{1}}$ (Dubrulle, 2019) (see however Schertzer and Lovejoy (2011) for multifractal transitions allowing deviations from such dimensional scaling). So, when $h>\mathrm{1}/\mathrm{3}$, Π_{ℓ} decreases with scale and tends to zero, while for $h<\mathrm{1}/\mathrm{3}$, Π_{ℓ} increases with decreasing scales and is able to provide larger and larger fluctuations. The case $h=\mathrm{1}/\mathrm{3}$ is special and corresponds to a case where the local energy flux is scale invariant. This is the situation that was assumed in the original selfsimilar theory of turbulence proposed by Kolmogorov. This theory leads to an energy spectrum scaling as ${k}^{\mathrm{5}/\mathrm{3}}$, yet we see from Fig. 12b that the local energy transfer term is highly variable in space, contrasting with the assumptions of homogeneity and isotropy made by Kolmogorov. This means that we have to forget about global homogeneity or scale invariance for turbulent flows, which would provide us with a single value for the scaling exponent, and rather consider the possibility that there may be a whole bunch of interesting local scaling exponents. To capture them, we must find a way to describe them using local scaling laws.
5.2 The multifractal spectrum
The corresponding mathematical description can be built using the large deviation theory (Eyink, 2007–2008) that allows us to describe the probability of finding an exponent h at a given place or time in the flow as
where C(h) is the rate function of h, also called the multifractal spectrum. Originally, C(h) was interpreted as the statistical codimension of the set where the velocity increment at a distance ℓ scales like ℓ^{h} (see Frisch and Parisi, 1985, and Schertzer and Lovejoy, 2011, and references therein). In that interpretation, it is natural that C(h) be less than the space dimension (C(h)≤3). In the largedeviation interpretation, however, one can get arbitrarily large C(h) corresponding to arbitrarily rare events. The codimension interpretation nevertheless allows us to single out the exponents where C(h)>3 (possibly C(h)→∞), meaning that the corresponding events are rarer than pointdistributed events, which indeed corresponds to exponents with a very low probability of occurrence. More generally, the largedeviation property enables us to make a direct connection between the multifractal spectrum and the scaling exponents of the nth moment of $\left{\mathit{\delta}}_{\mathrm{\ell}}u\right$ as
This is a Legendre transform. In that description, the value of h at which C(h) is minimum corresponds to the exponent with the highest probability, h_{mp}. This exponent is usually very easy to measure, as it corresponds to an exponent that is frequently hit.
We have computed the multifractal spectrum in the von Kármán flow using both experimental measurements and numerical simulations. The result is shown in Fig. 11b. We see that the minimum of C(h) is attained for h_{mp}=0.35, very close to but slightly larger than the $\mathrm{1}/\mathrm{3}$ Kolmogorov exponent. The fact that it is not exactly equal to $\mathrm{1}/\mathrm{3}$ is a hallmark of intermittency, as can be understood by coming back to the $\mathrm{4}/\mathrm{3}$ law. This law is strictly valid only for the signed exponent, but let us assume for the moment that it gives a good approximation for our absolute value moment, meaning ζ(3)=1. Given the Legendre property (4), this imposes that we must have $C\left(h\right)\le \mathrm{1}\mathrm{3}h$, which means that at $h=\mathrm{1}/\mathrm{3}$, C(h) is positive. In the codimension interpretation, this means that $h=\mathrm{1}/\mathrm{3}$ is true everywhere but for an ensemble of dimension 3−C(h). The only way it can be true everywhere is if $C(\mathrm{1}/\mathrm{3})=\mathrm{0}$, which means that C(h) is a delta function centred on $\mathrm{1}/\mathrm{3}$ (a pure fractal). Indeed, consider a simple model in which the multifractal spectrum is parabolic around its minimum $C\left(h\right)=(h{h}_{\mathrm{mp}}{)}^{\mathrm{2}}/\mathrm{2}b$. This is usually true near a minimum, and assuming that it extends further away was first done by Kolmogorov (1962), resulting in the lognormal model of turbulence. If we now impose that ζ(3)=1 in this model, we get ${h}_{\mathrm{mp}}=\mathrm{1}/\mathrm{3}+\mathrm{3}b/\mathrm{2}$, so that the only free parameter is b, the scale parameter. Therefore, in this model, the only value for which ${h}_{\mathrm{mp}}=\mathrm{1}/\mathrm{3}$ is b=0, corresponding to a delta function for C(h) and then to a pure fractal.
If this simple model were valid in the von Kármán flow, our measured value of h_{mp} would correspond to b=0.011, meaning a rather mild intermittency. Given that the condition ζ(3)=1 does not apply exactly for the absolute moment in our case, a more precise measure of intermittency can be made by performing a parabolic fit to our data, resulting in a larger value $b\sim \mathrm{0.035}\pm \mathrm{0.01}$. We stress here that the intermittency property is not in contradiction with the flux conservation of Eq. (2): we have indeed checked that 〈Π_{ℓ}〉 is scale independent in the inertial range and equal to the global energy dissipation. Locally, there is however no reason for the local flux to be scale independent, as it can hit regions with $h\ne \mathrm{1}/\mathrm{3}$, with nonzero probability (intermittency).
At all the places where $h<\mathrm{1}/\mathrm{3}$ (and we see that there are quite a few), the local energy transfer increases with decreasing scales. This means that there are many places in a turbulent flow where large fluctuations can build up. The smallest exponent we were able to measure is h≈0.17. We may also compute the multifractal spectrum using the scaling laws of the local energy transfers:
Using the local energy transfers, we are actually able to observe a smaller local scaling exponent very close to 0. These values can be compared to values obtained by computing the multifractal spectrum via application of the Legendre transform to scaling exponents computed in recent high Reynolds number numerical simulations of Iyer et al. (2020) for both longitudinal $\mathit{\delta}{u}^{\mathrm{L}}=\mathit{\delta}u\cdot \mathrm{\ell}/{\mathrm{\ell}}^{\mathrm{2}}$ and transverse $\mathit{\delta}{u}^{\mathrm{T}}=\mathit{\delta}u\times \mathrm{\ell}/{\mathrm{\ell}}^{\mathrm{2}}$ velocity increments. One sees that the longitudinal velocity increments also provide a minimal value around h≈0.16, while the minimal value for transverse velocity increments is h≈0. The smallest exponents, if they exist, will become increasingly rare, and we probably need to wait an order of magnitude longer time to be able to have a chance to observe them. To get an idea of what could be the smallest exponent we may observe, we can extrapolate our measurements with the lognormal model. The parabolic extrapolation to the value where C(h)=3 shows that the smallest exponent we may be able to find in the flow with a nonzero probability is ${h}_{\mathrm{min}}\simeq \mathrm{0.2}$. For such a negative value of h, the local energy transfer increases sharply towards the smaller scales like ${\mathrm{\Pi}}_{\mathrm{\ell}}\sim {\mathrm{\ell}}^{\mathrm{1.6}}$. Does it increase without limit? Is there any process to stop it?
5.3 The regularizing scale
Indeed, at the smallest scales of the flow, viscous effects curb the growth of the local energy transfer. The typical scale below which viscous effects become effective can be estimated from the dimensional analysis arguments of Paladin and Vulpiani (1987). Their argument is that the local energy budget of a turbulent flow at a given scale ℓ includes a sink term due to viscous dissipation besides the local energy transfer we mentioned in the previous sections (for a complete expression of the energy budget, see Dubrulle, 2019).
The sink term reads ${\mathrm{\Pi}}_{\mathit{\nu}}=\mathit{\nu}{\stackrel{\mathrm{\u203e}}{({\mathit{\delta}}_{r}u{)}^{\mathrm{2}}}}^{\mathrm{\ell}}$ and scales like ${\mathrm{\Pi}}_{\mathit{\nu}}^{\mathrm{\ell}}\sim \mathit{\nu}{\mathrm{\ell}}^{\mathrm{2}h\mathrm{2}}$ at locations where δ_{r}u∼r^{h}. The viscous term therefore balances the local energy transfer term at a scale ${\mathit{\eta}}_{h}\sim {\mathit{\nu}}^{\mathrm{1}/(\mathrm{1}+h)}$. This scale thus appears as a fluctuating cutoff scale which depends on the scaling exponent and therefore on x. This is a generalization of the Kolmogorov scale ${\mathit{\eta}}_{\mathrm{K}}\sim {\mathit{\nu}}^{\mathrm{3}/\mathrm{4}}$. Below η_{h}, the sink term due to dissipation becomes dominant in the energy budget, the local energy transfer vanishes, and the flow becomes regular, whereas this regularization occurs everywhere at η_{K} in the K41 model.
On Earth, strong velocity gradients develop in regions associated with the planetary boundary layer and may result in largescale extreme weather events: tornadoes, hurricanes, or supercells. Besides viscosity, there are other types of regularizing mechanisms for such phenomena. The energy can indeed be dissipated directly on solid surfaces with sometimes dramatic consequences for human beings, animals, and vegetation. Such a process is however akin to a “largescale friction” that is not present in our experiment. Extreme weather phenomena are still difficult to forecast. To capture them, is it enough to refine our everyday weather forecasts at a resolution of ∼1 km (the scale of convective flows) (Hohenegger et al., 2015)? This is the topic of the next section.
5.4 The computational nightmare continues
We have seen in Sect. 4 that we need to include the velocity fluctuations of the von Kármán turbulent flow down to their smallest scales to accurately reflect the largescale properties and dynamics of its seasonal cycle. For any given local exponent $h<\mathrm{1}/\mathrm{3}$, the local energy transfer increases with decreasing scales down to ℓ=η_{h}. Therefore, we have to make sure that our modelling resolution δ (the size of our grid) is below η_{h} for any h present in the flow. Otherwise, we may underestimate the magnitude of the fluctuations by a factor (δη_{h})^{h}. A stringent criterion to make sure all small scales are properly taken into account would be to choose δ equal to ${\mathit{\eta}}_{h={h}_{\mathrm{min}}}$, where h_{min} is either the smallest measured exponent observed in our simulation (optimistic view) or the smallest estimated exponent, computed using e.g. parabolic extrapolation (pessimistic view). In the first case, this gives h_{min}∼0, resulting in ${\mathit{\eta}}_{h={h}_{\mathrm{min}}}\sim \mathrm{1}/Re$, smaller than the Kolmogorov scale by a factor $R{e}^{\mathrm{1}/\mathrm{4}}$. In the pessimistic view, ${h}_{\mathrm{min}}\sim \mathrm{0.2}$, resulting in ${\mathit{\eta}}_{h={h}_{\mathrm{min}}}\sim R{e}^{\mathrm{5}/\mathrm{4}}\sim {\mathit{\eta}}_{\mathrm{K}}R{e}^{\mathrm{1}/\mathrm{2}}$. This pessimistic choice actually increases the number of degrees of freedom required to accurately model turbulent flows by a factor $R{e}^{\mathrm{3}/\mathrm{2}}$ compared to our initial estimate based on the Newtonian viscosity of the fluid and the K41 turbulent model. We then reach N∼10^{23} degrees of freedom (the Avogadro number) in our water von Kármán experiment or N∼10^{40} for the atmosphere.
We seem to have understood why climate models work in the first place: the largescale topology and externally forced transitions do not depend very much on the value of the viscosity and may in fact be described with tools from statistical mechanics (Thalabard et al., 2015) involving only a few hundred to thousand modes that can easily be captured by present climate models. However, when it comes to understanding whether present climate models have enough degrees of freedom to capture global bifurcations, we have reached contrasting conclusions using our laboratory experiment.
A key result from this experiment is that the large scales of even highly turbulent flows are not restricted to having purely relaxational dynamics, decaying monotonically to an “energy landscape pit” from which escape is impossible, the turbulent fluctuations “randomizing away” any escape attempt. The forced rotation rate experiments (Sect. 4.3) show that this is definitely not the case: when brought to the symmetric forcing θ=0 situation, the flow remembers with seemingly infinite memory how it has been prepared and remains in its “A” or “B” state indefinitely (the “T” state is peculiar in that its decay time diverges when θ→0, but the transition seems a priori possible). In this respect, though the level of turbulent fluctuations is very high, the large scales of the flow are as deterministic as a light switch. This behaviour is in fact well known in aerodynamics, where it is encountered in the “stalling” transition of airfoils (Sarraf et al., 2005). The fixed flux experiments (Sect. 4.4) are even more spectacular in that they show that the large scales of the flow can have nontrivial temporal dynamics, with an elaborate scenery of fast transitions between longlived states and with residence times in the states either sharply distributed around a finite value or exponentially distributed with a long characteristic time of decay.
The fact that this time evolution of the largescale topology of the flow can be described by a lowdimensional attractor, corresponding to a few degrees of freedom, is very encouraging and justifies the search for procedures for cutting down the number of degrees of freedom. However, the destruction of the coherent largescale dynamics by the large increase in the viscosity in the glycerol experiments shows that a too trivial procedure might preclude a sufficient representation of potentially vitally important largescale Earth system processes. Indeed, our study suggests that a good practice to approach complexity is to use both simple conceptual models such as the one presented in Faranda et al. (2017, 2019b) as well as complex models (e.g. direct numerical simulations, DNS, or large eddy simulations, LES, for the von Kármán flow and full numerical integration of primitive equations for the climate). While simple models can quickly provide an overview of the bifurcation landscape of a system, fine models can be used to explore targeted regions of the phase space where interesting phenomena produce e.g. extreme dissipation events in the von Kármán flow or convective events in climate simulations.
We have seen that these fluctuations are generated at very small scales by a concentration of local energy transfer ending up in pointlike quasi singularities, with large fluctuations over small scales. These small scales are really small, even smaller than the Kolmogorov scale η_{K}. Resolving these small scales using direct numerical simulations comes at a colossal computational cost, out of reach of current (and future) computing facilities. So, the problem of smallscale parametrization is in fact even more acute than we thought. From what we have learned, one thing we must take care of is to devise a model that is able to reproduce and include the large velocity fluctuations observed at very small scales in experimental turbulent flows without explicitly resolving them. This is clearly the next challenge in climate modelling.
Code is available upon request to berengere.dubrulle@cea.fr.
Data are available upon request to berengere.dubrulle@cea.fr.
BD, FD, DF, BSM and LM conceived and designed the analysis. LM and BSM collected the data. DF contributed analysis tools. BD, BSM and DF performed the analysis. BD (main text) and BSM (figure editing) wrote the paper. BD, FD, DF, LM and BSM reviewed the paper.
The contact author has declared that neither they nor their coauthors have any competing interests.
Publisher’s note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
This article is part of the special issue “Centennial issue on nonlinear geophysics: accomplishments of the past, challenges of the future”. It is not associated with a conference.
Even though Bérengère Dubrulle received the medal as an individual, most of this work has been done through and thanks to collaboration with students, postdocs, and colleagues, some of them coauthors of this paper. Didier Paillard cosupervised with Bérengère on topics related to the subjects and fuelled our thinking with many interesting references and ideas. She learned a lot about climate and dynamical systems from discussion with Pascal Yiou, Robert Vautard, Didier Roche, and other members of their team.
Thanks to JeanPhilippe Laval, Vishwanath Shukla, Florian Nguyen, Hugues Falller, Caroline Nore, JeanLuc Guermond and Loïc Cappanera for providing the numerical data and analysis. François Daviaud, Arnaud Chiffaudel, Adam Cheminet, JeanMarc Foucaut, Christophe Cuvier, Yashar Ostovan, Vincent Padilla, Cécile Wiertel, Pantxo Diribarne, PierrePhilippe Cortet, Éric Herbert, Davide Faranda, EweWei Saw, Valentina Valori, Romain Monchaux, Brice SaintMichel, Simon Thalabard, Denis Kuzzay, Paul Debue, and Damien Geneste performed the particle velocimetry measurements and analysis. The bifurcation measurements in water and glycerol owe much to the PhD work of Louis Marié, Florent Ravelet, and Brice SaintMichel. This work has been supported by Agence Nationale de la Recherche (ANR) EXPLOIT, grant agreement no. ANR16CE06000601.
This research has been supported by the Agence Nationale de la Recherche (grant no. ANR16CE060006).
This paper was edited by Daniel Schertzer and reviewed by two anonymous referees.
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 Abstract
 Context
 How many degrees of freedom are theoretically and practically involved in climate simulations?
 The von Kármán flow, an analogue for oceanic or atmospheric largescale circulation
 Largescale circulation properties
 Fluctuations and smallscale properties
 Conclusions
 Code availability
 Data availability
 Author contributions
 Competing interests
 Disclaimer
 Special issue statement
 Acknowledgements
 Financial support
 Review statement
 References
 Abstract
 Context
 How many degrees of freedom are theoretically and practically involved in climate simulations?
 The von Kármán flow, an analogue for oceanic or atmospheric largescale circulation
 Largescale circulation properties
 Fluctuations and smallscale properties
 Conclusions
 Code availability
 Data availability
 Author contributions
 Competing interests
 Disclaimer
 Special issue statement
 Acknowledgements
 Financial support
 Review statement
 References