Diffusive effects in local instabilities of a baroclinic axisymmetric vortex

Abstract We present a local stability analysis of an idealized model of the stratified vortices that appear in geophysical settings. The base flow comprises an axisymmetric vortex with background rotation and an out-of-plane stable stratification, and a radial stratification in the thermal wind balance with the out-of-plane momentum gradient. Solving the local stability equations along fluid particle trajectories in the base flow, the dependence of short-wavelength instabilities on the Schmidt number $Sc$ (ratio between momentum and mass diffusivities) is studied, in the presence of curvature effects. In the diffusion-free limit, the well-known symmetric instability is recovered. In the viscous, double-diffusive regime, instability characteristics are shown to depend on three non-dimensional parameters (including $Sc$), and two different instabilities are identified: (i) a monotonic instability (same as symmetric instability at $Sc = 1$), and (ii) an oscillatory instability (absent at $Sc = 1$). Separating the base flow and perturbation characteristics, two each of base flow and perturbation parameters (apart from $Sc$) are identified, and the entire parameter space is explored for the aforementioned instabilities. In comparison with $Sc = 1$, monotonic and oscillatory instabilities are shown to significantly expand the instability region in the space of base flow parameters as $Sc$ moves away from unity. Neutral stability boundaries on the plane of $Sc$ and a modified gradient Richardson number are then identified for both these instabilities. In the absence of curvature effects, our results are shown to be consistent with previous studies based on normal mode analysis, thus establishing that the local stability approach is well suited to capturing symmetric and double-diffusive instabilities. The paper concludes with a discussion of curvature effects, and the likelihood of monotonic and oscillatory instabilities in typical oceanic settings.


Introduction
Eddies, along with fronts, i.e. regions of relatively sharp horizontal density gradients, are common occurrences in the atmosphere and the ocean. In the atmosphere, baroclinic and barotropic instabilities result in the formation of cyclones and anticyclones (Emanuel, Fantini & Thorpe 1987), and the resulting advection of temperature leads to the formation of fronts (Hoskins & Bretherton 1972). Similar processes occur in the ocean too. For example, tropical instability near the equator can result in the formation of tropical instability vortices which are associated with strong equatorial sea surface temperature fronts (Holmes et al. 2014). Alternatively, processes such as wind and topographical variations can lead to the development of submesoscale eddies such as the structures which are associated with frontal regions (Mahadevan 2006). In addition, stirring by mesoscale (around 100 km or more, corresponding to a Rossby number much smaller than unity) and submesoscale (1-100 km, corresponding to a Rossby number around unity) eddies can form frontal regions too (Shcherbina et al. 2015;Sarkar et al. 2016). The dynamics of these eddies, apart from significantly influencing the transport of various quantities such as heat, salinity and nutrients (Zhang, Wang & Qiu 2014), can also have significant implications for large-scale phenomena like the El Niño southern oscillation and the equatorial heat budget (Holmes et al. 2014). Furthermore, the dynamics of submesoscale coherent vortices is an important consideration to understand transport and mixing in many parts of the ocean (McWilliams 1985).
Large-scale geophysical eddies, apart from their vortical structure, often have a vertical (out of plane) gradient of momentum which is in thermal wind balance with the horizontal density variation (Pedlosky 1987). Factors such as background rotation and vertical stratification also affect the dynamics of these vortices. In addition, curvature effects have also been shown to have an effect on frontogenesis and the adjustment of fronts near vortices (Shakespeare 2016). Instabilities in these vortices represent an important pathway towards small-scale turbulence and mixing (Thomas, Tandon & Mahadevan 2008), thus playing a key role in parameterization of small-scale processes in large-scale climate models (Fox-Kemper, Ferrari & Hallberg 2008;Bachman et al. 2017). In addition, their instability characteristics can also help in interpreting field observations (Ruddick 1992;D'Asaro et al. 2011;Thompson et al. 2016) and large-scale climate model outputs (Fox-Kemper et al. 2011), which in turn motivate fine-scale process studies (Mahadevan & Tandon 2006).
Instabilities in geophysical vortices could range from purely inertial, such as the centrifugal instability in unstratified planar vortices (Kloosterziel & Van Heijst 1991), to purely convective, resulting from statically unstable vertical stratification (Chandrasekhar 1961). The intermediate regimes, where both inertial and buoyancy effects are present, can be conducive to what is called the symmetric instability (Hoskins 1974;Xui & Clark 1985;Thomas et al. 2013). Purely centrifugal instabilities are generally suppressed by Coriolis forces (Godeferd, Cambon & Leblanc 2001) but could play an important role in regions with anticyclonic vorticity and near the equator, where Rossby numbers are near unity (Haine & Marshall 1998). Symmetric instability can result in slantwise convection along tilted constant angular momentum surfaces when the potential vorticity is negative in an inviscid, adiabatic environment (Hoskins 1974). Recently, curvature effects on the symmetric instability have been studied, and their importance in oceanic eddies has been highlighted (Buckingham, Gula & Carton 2021a,b). In addition, hyperbolic instabilities could also manifest in regions of high strain near the edges of vortices with hyperbolic stagnation points (Leblanc 1997). Apart from the aforementioned local instabilities, global instabilities such as the Kelvin-Helmholtz (Peltier & Caulfield 2003) and baroclinic instabilities (Pierrehumbert & Swanson 1995) are also a consideration in stratified eddies. 928 A14-2 Vortices in thermal wind balance can also become unstable due to unequal mass and momentum diffusivities. McIntyre (1970), using normal mode theory in a locally Cartesian region of an eddy in thermal wind balance, showed that a Prandtl number away from unity modifies the symmetric instability criterion, and also introduces a local oscillatory instability. Laboratory experiments have demonstrated the occurrence of such an oscillatory instability, and resulting density layers (Baker 1971;Meunier et al. 2014). Studies regarding instabilities in long-lived mesoscale oceanic eddies have considered this diffusive instability mechanism to explain intrusions found in density profiles (Ruddick 1992;Kuzmina & Zhurbas 2000). Experimental studies have also observed the formation of density layers at a Prandtl number less than unity, which was further suggested to explain the layers on the scale of 1 m seen in certain parts of the ocean. (Calman 1977;Weber 1980). An energetics-based approach to derive the results of McIntyre (1970) in a parallel shear flow was presented by Kloosterziel & Carnevale (2007). Here, we use the local stability approach (Lifschitz & Hameiri 1991) with small diffusivities in momentum and density to investigate short-wavelength instabilities in stratified eddies in thermal wind balance. Previous studies using the local stability approach have captured the effects of differential diffusion (in mass and momentum) on local instabilities in radially stratified circular Couette flow (Kirillov & Mutabazi 2017) and vertically stratified planar vortices (Singh & Mathur 2019).
In this study, we explore local instabilities in horizontally and vertically stratified vortices in thermal wind balance, including the effects of differential diffusion in mass and momentum. The local stability approach is first demonstrated to be efficient in capturing symmetric and double-diffusive instabilities. Apart from being based on a different approach compared with McIntyre (1970), our study is also wider in scope compared with that of McIntyre (1970) in three significant aspects: (i) exploration in the centrifugally unstable regime, (ii) viscous instability characteristics away from the neutral stability boundaries in both the centrifugally stable and unstable regimes and (iii) curvature effects. The local stability framework and the base flow configuration are described in § 2 followed by our results on the instability characteristics in § 3. The importance of our results, particularly the curvature effects, are discussed in three different contexts in § 4, following which the conclusions are presented in § 5.

Theory
The governing equations of motion for an incompressible flow with background rotation Ωe z (e z is the unit vector along the positive z-axis), within the Boussinesq approximation, are where t is time, ρ, u and p the density, velocity and pressure, respectively, and gravity g = −ge z with g > 0; ρ 0 , ν and κ are the reference density, kinematic viscosity and diffusion coefficient associated with density, respectively. 2.1. Base flow We consider a base flow field that describes an axisymmetric vortex in stratified surroundings. Specifically, the velocity field is given by where (r, ω, z) represent the cylindrical polar coordinates, and the subscript B denotes base flow quantities. The corresponding density field is given by ρ B (r, z), with its vertical and radial gradients characterized by the Brunt Väisälä frequency N z = √ −(∂ρ B /∂z)(g/ρ 0 ) (N 2 z > 0 throughout the current study), and N r = √ −(∂ρ B /∂r)(g/ρ 0 ). Finally, the pressure associated with the base flow is denoted as p B (r, z). The base flow field satisfies the mass conservation (2.1), the azimuthal component of the inviscid momentum equation ((2.2) with ν = 0) and the diffusion-free incompressibility condition ((2.3) with κ = 0). Furthermore, requiring the base flow to satisfy the radial component of (2.2) gives where it has been assumed that the vertical component of (2.2) is described by hydrostatic balance. In other words, (2.5) represents a modified thermal wind relation (Shakespeare 2016), where the centripetal, Coriolis and pressure gradient forces are in balance. In the limit of V/r → 0, (2.5) recovers the well-known geostrophic balance (Vallis 2017). In this study, however, the curvature effects are retained in the relation between the vertical gradient of momentum and the horizontal stratification. A schematic of the base flow in thermal wind balance is shown in figure 1.

Local stability equations
To study the stability properties of the base flow in § 2.1, we superimpose small perturbations to write the net flow field as where the prime denotes perturbation quantities. The linearized, viscous governing equations for the perturbation flow field are where b = gρ /ρ 0 , and the base flow has been assumed to satisfy the inviscid governing equations. In other words, (2.7)-(2.9) represent the governing equations for small, viscous perturbations superimposed on the inviscid base flow described in § 2.1. Here, d/dt = ∂/∂t + u B · ∇ is the material time derivative in the base flow u B .
In accordance with the local stability approach (Lifschitz & Hameiri 1991), we assume short-wavelength perturbations of the form (2.10) where δ is a small 'short-wavelength' parameter, and φ(x, t) is a real scalar field that contains the wave-like behaviour in the perturbations. The perturbation wave vector k is given by k = ∇φ/δ = k/δ, thus rendering the perturbation to be of short wavelength since δ is a small parameter; (a, π, b) are the complex leading-order amplitudes of the velocity, pressure and buoyancy perturbations, respectively. Similarly, (a δ , π δ , b δ ) are the complex perturbation amplitudes at O(δ). Assuming the two diffusivities ν and κ to be of O(δ 2 ), and substituting the perturbation forms in (2.10)-(2.12) in the governing equations (2.7)-(2.9), results at O(δ 0 ) in the local stability equations (2.14) In (2.13)-(2.15), d/dt = ∂/∂t + u B · ∇ is the material time derivative in the base flow u B , k z the z-component of k, and (c ν , c κ ) = (ν, κ)/δ 2 . The assumptions of ν and κ being of O(δ 2 ) are motivated by the second-order spatial gradients in the viscous terms, which then contribute at O(δ 0 ) in (2.8)-(2.9). Previous studies on local instabilities have incorporated viscous effects in this manner. For example, (2.13)-(2.14) without background rotation and buoyancy were considered by Landman & Saffman (1987), who showed that viscous terms suppress the growth rates associated with elliptic instability in an unstratified, planar elliptical vortex. In addition to elucidating viscous damping of inviscid instabilities, the O(δ 2 ) scaling of momentum and mass diffusivities have helped the local approach unearth double-diffusive instabilities in stratified vortices as well (Kirillov & Mutabazi 2017;Singh & Mathur 2019). Finally, the O(δ 2 ) scaling for temperature and salinity diffusivities also leads to the reduction of local stability equations to the classical salt fingering instability equation for a quiescent base flow (Appendix A).
In the absence of diffusive effects (c ν = c κ = 0), (2.13)-(2.15) coincide with the equations considered by Miyazaki (1993) for a stably stratified elliptical vortex with no in-plane stratification; further, if background rotation is also absent, (2.13)-(2.15) reduce to those considered by Miyazaki & Fukumoto (1992). Finally, if background rotation and buoyancy are both absent, (2.13)-(2.14) coincide with those derived by Lifschitz & Hameiri (1991). The equations governing the evolution of a and b are solved on closed fluid particle trajectories in the base flow for periodic wave vectors, to subsequently obtain corresponding growth rates. We proceed to obtain the conditions under which perturbation wave vectors are periodic upon integrating the wave vector evolution equation (2.13) over a closed trajectory in the base flow given by (2.4). For a wave vector k = k r e r + k ω e ω + k z e z , (2.13) can be written in component form as (2.18) Equation (2.17) indicates that k ω is a constant along the trajectory, and a non-zero value for the constant would lead to a monotonically changing k r and k z . Therefore, for each of k r , k ω and k z to be periodic upon integration over one closed trajectory, k ω has to necessarily be zero. With k ω = 0, k r and k z become constant along the trajectory. It is noteworthy that k ω = 0 represents zero azimuthal wavenumber, i.e. axisymmetric perturbations in the normal mode approach, although the perturbation amplitudes are still allowed to evolve along the circular base flow trajectory in the local stability approach. In summary, any wave vector given by k = k r e r + k z e z represents a periodic wave vector; the amplitude evolution equations (2.14)-(2.15) are solved for such periodic wave vectors. The periodicity of the wave vector enables the use of Floquet theory to obtain growth rates, and ensures uniqueness of the perturbation wave vector at a given spatial location. The latter aspect is potentially relevant for establishing a connection between local and global stability approaches.
For the base flow in (2.4), considering periodic wave vectors, (2.14)-(2.15) can be written in cylindrical polar coordinates as where (a|b) = [a r , a ω , a z , b] T and A is a 4 × 4 matrix. Substituting a = a r e r + a ω e ω + a z e z and a periodic wave vector k = k r e r + k z e z in (2.14)-(2.15), we obtain 20) where de r /dt = e ω V/r and de ω /dt = −e r V/r have been used to account for circular fluid particle trajectories with an angular speed V/r. Owing to the constancy of r and V on a streamline, and k r , k z , |k| also being invariant along a streamline for periodic wave vectors, the coefficient matrix A in (2.20) is time independent.

Results
The eigenvalues (λ) of A (2.20) represent the growth rates, and are governed by The growth rate σ is given by the maximum real part of λ, which we analyse in detail in the rest of this paper. Instabilities with zero or non-zero imaginary part in the corresponding eigenvalues are henceforth referred to as monotonic or oscillatory, respectively. In the presence of diffusion terms (c ν > 0, c κ > 0), one of the eigenvalues of A is −c ν |k| 2 , while the other three eigenvalues of A can be given by a cubic equation. Dividing by |Φ/2| 3/2 , (3.1) is non-dimensionalized to give the governing equation for the other three eigenvalues as whereλ = λ/ √ |Φ/2|,Φ = Φ/|Φ| and Sc = ν/κ = c ν /c κ is the Schmidt number. As shown in § 3.2,Φ = −1 corresponds to centrifugal instability in the inviscid limit. With this choice of non-dimensionalization, the important limit of weak (but finite) viscous effects is easily recovered without the divergence of non-dimensionalized growth rate. The non-dimensional parameters that appear in (3.2) are where (Γ, Θ) in (3.4a,b) describe the base flow, and (θ,c) in (3.5a,b) describe the perturbation wave vector. Φ, as defined in (3.3), is the Rayleigh discriminant, i.e. twice the product between the total angular velocity and the absolute vertical vorticity in the base flow. Specifically, Γ is a measure of the vertical velocity gradient (recall that N 2 r = 2(Ω + V/r)∂V/∂z due to thermal wind balance) with respect to the strength of centrifugal instability in the inviscid, unstratified limit (see § 3.2), and Θ is the inclination of the isopycnals with respect to the z-axis in the base flow. In (3.5a,b), θ is the inclination of the perturbation wave vector with respect to the z-axis, andc is the inverse of a perturbation Reynolds number, which quantifies the viscous effects in the perturbation with respect to the inertia in the base flow. It is worth noting that the non-dimensional parameters in (3.4a,b)-(3.5a,b) are defined such that the inviscid limit can be recovered without any singularities. In addition to the four parameters in (3.4a,b)-(3.5a,b), Sc is also a parameter that appears in (3.2), thus influencing the instability characteristics. As shown in § 3.4, for given values of (tan Γ, tan Θ, θ,c, Sc), monotonic and oscillatory instabilities cannot occur simultaneously. McIntyre (1970) McIntyre (1970) considered a base flow similar to the current study, described by a purely azimuthal velocity field V M (r, z)e ω and a potential temperature field T M (r, z), under the influence of background rotation Ωe z , gravity −ge z and in thermal wind balance. Defining C M (r, z) = 2Ωr + V M (r, z), McIntyre (1970) identified the following non-dimensional base flow parameters:

Comparison with
with the Schmidt number being given by Sc = ν/κ. In (3.6a,b), the subscripts z and r denote differentiation with respect to z and r, respectively. Operating in the regime N 2 z = gαT M,z > 0 (statically stable, with α being the thermal expansion coefficient), 2ΩC M,r > 0 (centrifugally stable in locally Cartesian coordinates), McIntyre (1970) considered a locally Cartesian (curvature effects ignored) unbounded normal mode theory (Wentzel-Kramers-Brillouin-Jeffreys, i.e. WKBJ-type approximation where spatial gradients of the base flow are assumed constant). Considering perturbations of the form exp[ik M (r sin θ + z cos θ) + ω M t], with θ being the angle between the wave vector and the z-axis, the author derived the governing equation for the non-dimensional growth rate as where Re(ω M ) is the growth rate, k M is the magnitude of the wave vector, The criteria for monotonic and oscillatory instabilities were then shown to be tan Θ M /tan Γ M < (1 + Sc) 2 /4Sc and tan Θ M /tan Γ M < (3Sc + 1) 2 /8Sc(Sc + 1), respectively. These criteria can be recovered as the zero curvature limit of our results in § 3.3.3. To explore the relation between our local stability framework, and McIntyre's theory, we re-write (3.2) in the limit of zero curvature and non-dimensionalization using the length and time scales of McIntyre (1970). Specifically, defining L = (ν 2 /|N 2 r |) 1/4 and T = (|N 2 r |) −1/2 as the length and time scales, (3.2) can be written as whereλ = λT,k = kL and ν = c ν δ 2 is the kinematic viscosity as defined in § 2.2;Φ = 1 has been assumed. We note thatΦ = 1 is equivalent to 2ΩC M,r > 0, i.e. the study of McIntyre (1970) is restricted to the first and third quadrants of the (tan Γ, tan Θ) plane. Equation (3.8) is the same as (3.7), with k M =k/δ. Thus, we have shown that, in the limit of zero curvature, the local stability equation for the growth rate concurs with the locally Cartesian unbounded normal mode theory. This connection between local stability and normal mode approaches builds on previous such connections demonstrated for other flows: inviscid, unstratified axisymmetric vortices with an axial flow (Le Duc & Leblanc 1999;Mathur et al. 2014), viscous unstratified elliptical vortex (Landman & Saffman 1987) and viscous, in-plane stratified axisymmetric flow with an arbitrary Prandtl number (Kirillov & Mutabazi 2017). Apart from our study being based on a different approach compared with McIntyre (1970), our results are also wider in scope compared with the results of McIntyre (1970) in three significant aspects: (i) exploration in the centrifugally unstable regime (second and fourth quadrants of (tan Γ, tan Θ) plane), (ii) viscous instability characteristics away from the neutral stability boundaries in both the centrifugally stable and unstable regimes and (iii) curvature effects. With respect to point (ii), we note that the length scale L used by McIntyre (1970) for non-dimensionalization makes it difficult to explore the regime of small but finite viscous effects. As discussed in § 3.3, significant growth rates of both monotonic and oscillatory instabilities can occur in the weakly viscous regime, where even the most unstable perturbations can lie. The curvature effects are discussed more in detail in § 4.1.

Inviscid limit
Substituting the inviscid limit of c ν = c κ = 0 in (3.1), the non-trivial roots are obtained as where θ ∈ [0, π] is the angle made by the wave vector k with the z-axis, such that k z /|k| = cos θ and k r /|k| = sin θ. Maximizing λ 2 with respect to θ, and requiring it to be positive results in the following inviscid instability criterion: As a result, Φ < 0 (in other words,Φ = −1) guarantees instability (recall that N 2 z > 0 is assumed). The maximum growth rate occurs at where the range of tan −1 is taken to be [−π/2, π/2]. We recall from (2.5) that thermal wind balance requires N 2 r = 2(V/r + Ω)(∂V/∂z). The ranges of unstable θ are given by where we have again taken the range of tan −1 as [−π/2, π/2]. The results in (3.10) and (3.11), in the limit of no curvature effects, i.e. V/r = 0, are in agreement with the previously known two-dimensional inviscid symmetric instability criteria derived based on the normal mode approach (Ooyama 1966;Hoskins 1974). To the best of our knowledge, recovery of the symmetric instability criteria in the local stability framework has not been pointed out before. Furthermore, (3.10)-(3.14) provide corrections due to finite curvature effects, which are difficult to capture in the normal mode approach (Buckingham et al. 2021a) although they are negligible only in the limit of |V/r| |Ω|. Equation (3.10), which is in agreement with the symmetric instability criterion based on Lagrangian parcel arguments (Solberg 1936;Emanuel 1979) and the recent studies of Buckingham et al. (2021a,b), also establishes the local stability framework as an alternative approach to understand curvature effects. Finally, an insightful interpretation of (3.10) is that the square of the absolute circulation (2π(Ωr 2 + Vr)) decreases with radius when moving along iso-density surfaces (Emanuel 1979); this form of the symmetric instability criterion has been previously used to interpret instabilities in pancake vortices (Negretti & Billant 2013;Yim, Billant & Ménesguen 2016).
In the limit of no radial stratification, i.e. N r = 0, the instability criterion in (3.10) reduces to Φ < 0, with the maximum growth rate being given by λ * = √ −Φ occurring at θ * = 0. This no-radial-stratification inviscid limit was highlighted using the local stability approach by Singh & Mathur (2019), and is consistent with the large axial wavenumber limit of Billant & Gallaire (2005). In this unstable regime of Φ < 0, the range of unstable θ reduces from [0, π/2] for N z = 0 to [0, tan −1 −Φ/N 2 z ] for a finite N z . Finally, in the limit of a homogeneous fluid, i.e. N r = N z = 0, (3.9) gives the classical inviscid centrifugal instability criterion (Kloosterziel & Van Heijst 1991). This limit of centrifugal instability in unstratified vortices with background rotation has been considered in previous local stability studies too (Sipp & Jacquin 2000;Nagarathinam, Sameen & Mathur 2015).
In terms of the non-dimensional base flow parameters in (3.4a,b), the inviscid instability criterion in (3.10) can be written as with the most unstable θ given by It is worth highlighting that represents a modified gradient Richardson number. The inviscid instability regimes on the (tan Γ, tan Θ) plane are shown in figure 2. In the first and third quadrants, Figure 2. Inviscidly stable (white background) and unstable (grey background) regions on the (tan Γ, tan Θ) separates the stable and unstable regions, whereas the entire second and fourth quadrants (Φ < 0 =Φ = −1 in these quadrants) are unstable. It is worth recalling that all inviscid instabilities are monotonic in nature (zero imaginary part for the growth rate).

Viscous regime
In the limit of Sc = 1, the solutions of (3. where λ i are the inviscid eigenvalues given by (3.9). In other words, for Sc = 1, all the eigenvalues from the inviscid limit get reduced by c ν |k| 2 , thus resulting in the inviscid growth rates being reduced by viscous effects, and the occurrence of two stable eigenvalues (= −c ν |k| 2 ). As a consequence, the eigenvalues for Sc = 1 and |k| = 0 coincide with the inviscid eigenvalues, thus establishing an equivalence between inviscid instabilities and instabilities at Sc = 1. For Sc / = 1, three non-trivial eigenvalues governed by (3.2) occur. While two of them could possibly be a continuous extension of the two non-trivial eigenvalues from the inviscid limit, the counterpart of the third eigenvalue was trivial and stable in the inviscid limit. For Sc / = 1, we proceed to plot the non-dimensionalized growth rate (σ = σ/ √ |Φ/2|) as a function of the perturbation parameters (3.5a,b) for given base flow parameters (3.4a,b). As highlighted earlier in this section, our choice of non-dimensionalization allows us to easily explore the important regime of weak but finite viscous effects. Figure 3 shows the growth rate (in log scale) plotted as a function of θ andc for tan Γ = 1, and three different values of tan Θ (1.2, 1 and 0.4), which progressively takes the system from stable to neutrally stable to unstable in the inviscid limit (see first quadrant of figure 2). We recall from (3.15) that tan Θ/ tan Γ < 1 is the inviscid instability criterion, which also holds for Sc = 1. It is also worth noting that for Sc = 1, the instability is always monotonic in nature. In figure 3, panels (a,b,c) and (d,e,f ) correspond to Sc = 0.1 and 5, respectively.
For tan Θ = 1.2 (figure 3a), i.e. the inviscidly stable regime, we observe unstable growth rates at Sc = 0.1 though no instabilities occur for Sc = 1. The monotonic and oscillatory  and (c, f ), respectively. All the plots correspond to tan Γ = 1, thus belonging to the first quadrant of figure 2. The green and brown regions correspond to zero (monotonic instability) and non-zero (oscillatory instability) imaginary part for the growth rate. In each plot, the unfilled circle corresponds to the location of maximum growth rate on the entire (θ,c) plane, with the red colour indicating a location away fromc = 0 axis. No instabilities occur for θ > π/2 in all the plots in this figure.
The values of tan Θ/ tan Γ for (a,b,d,e) correspond to the inviscidly stable regime, and hence the growth rate is zero on thec = 0 axis.
(non-zero imaginary part for the growth rate) instability regions are shown in green and brown, respectively. The monotonic instability dominates the oscillatory instability on the (θ,c) plane, with the overall maximum growth rate occurring at (θ * ,c * ) = (1.05 rad, 0.14) within the monotonic instability region. The monotonic instability is completely suppressed at a threshold value ofc t = 0.54. For the oscillatory instability, the maximum growth rate occurs at (θ * ,c * ) = (0.49 rad, 0.035), and it is completely suppressed beyondc = 0.09. In terms of the range of θ, monotonic and oscillatory instabilities occur within [0.8,1.45] rad and [0.19,0.67] rad, respectively. The width of these unstable θ ranges are used later ( § 3.3.2) to characterize the instability region on the (θ,c) plane. For tan Θ = 1 (figure 3b), i.e. on the inviscid neutral stability boundary, monotonic and oscillatory instabilities are again observed at Sc = 0.1, with an overall increase in the growth rates compared with tan Θ = 1.2. The monotonic and oscillatory instability regions are also slightly larger for tan Θ = 1 than for tan Θ = 1.2. For tan Θ = 0.4 and Sc = 0.1 (figure 3c), i.e. the inviscidly unstable regime, the regions of instability and the associated growth rates are noticeably larger. Furthermore, the maximum growth rate on the entire (θ,c) plane now occurs at (θ * ,c * ) = (0.93 rad, 0), still within the monotonic instability region. For reference, the monotonic instability for (tan Γ, tan Θ) = (1, 0.4) at Sc = 1 is also strongest at the same (θ * ,c * ) location (see (3.16)). Figure 3(d-f ) corresponds to the same parameters as panels (a,b,c), except for Sc, which is now set at 5. In the inviscidly stable regime of tan Θ = 1.2 (figure 3d), monotonic instability is observed while oscillatory instability is absent. The overall growth rates are smaller in magnitude than for Sc = 0.1, and the maximum growth rate occurs at (θ * ,c * ) = (0.5 rad, 0.35). With an increase in tan Θ to unity (figure 3e), the growth rate magnitudes increase, and oscillatory instability appears. In contrast to Sc = 0.1,  −1), and thus belonging to the fourth quadrant in figure 2. The green and brown regions correspond to zero (monotonic instability) and non-zero (oscillatory instability) imaginary part for the growth rate. In each plot, the unfilled circle corresponds to the location of maximum growth rate on the entire (θ,c) plane. In (c), the growth rate corresponding to oscillatory instability vanishes on thec = 0 axis. oscillatory instability occurs at larger θ than that for the monotonic instability at Sc = 5. Finally, in the inviscidly unstable regime of tan Θ = 0.4 (figure 3f ), oscillatory instability again appears alongside the monotonic instability, the region of instability on the (θ,c) plane is substantially larger than for smaller tan Θ, and the maximum growth rate occurs at the same (θ * ,c * ) = (0.93 rad, 0) as that for the monotonic instability at Sc = 1. In summary of figure 3, for Sc / = 1, monotonic instability appears in the inviscidly stable regime too, while a new oscillatory instability appears in inviscidly stable as well as unstable regimes. The maximum growth rate on the (θ,c) plane, however, always lies in the monotonic instability region, irrespective of Sc, tan Γ and tan Θ. We show later in § § 3.3.3 and 3.4 that the monotonic instability observed for Sc / = 1 is a continuous extension of the monotonic symmetric instability that occurs at both Sc = 1 and the inviscid limit. We proceed to investigate (in figure 4) the instabilities for Sc / = 1 in the fourth quadrant of figure 2, the entirety of which is inviscidly unstable due to Φ < 0. Figure 4(a,b) shows that only monotonic instability occurs at Sc = 0.1 and Sc = 1 for (tan Γ, tan Θ) = (1, −1). The range of unstable θ is noticeably larger for Sc = 0.1 compared with Sc = 1. At Sc = 5 (figure 4c), oscillatory instability appears along with the monotonic instability. Finally, we note that the most unstable (θ,c) is (2.75 rad, 0) , which lies within the monotonic instability region, for all three Sc in figure 4. Furthermore, we find that the largest growth rate is always associated with the monotonic instability for every unstable (tan Γ, tan Θ, Sc). Towards obtaining neutral stability boundaries in terms of the base flow parameters and Sc, we proceed to plot the most unstable growth rate in the monotonic and oscillatory instability regions of plots such as in figures 3 and 4, on the (tan Γ, tan Θ) plane.

Dominant instability characteristics
The maximum growth rate on the (θ,c) plane, and the corresponding location at which it occurs, are plotted as a function of tan Γ and tan θ for Sc = 0.1 and 5 in the panels (a,b,c) and (g,h,i) of figure 5, respectively. We recall that the maximum growth rate always corresponds to the monotonic instability. For reference, the equivalent plots for Sc = 1 are shown in panels (d,e,f ), with the black lines in (a,b,d,g,h,i) representing the boundary separating stable and unstable regions for Sc = 1. The panels (a,d,g), (b,e,h) and (c,f,i) show the distributions of maximum growth rateσ max (on a log scale), and the most unstable (θ,c) = (θ * ,c * ), respectively.  For Sc = 0.1, monotonic instability is observed in the inviscidly stable region of the first quadrant of the (tan Γ, tan Θ) plane, with the neutral stability boundary being steeper than that for Sc = 1 (figure 5a). In contrast to Sc = 1, some part of the monotonic instability region for Sc = 0.1 has the maximum growth rate occurring at finite viscous effects, i.e.c * > 0 (figure 5c). Interestingly,c * > 0 occurs for the whole of the unstable region that was inviscidly stable, and some part of the inviscidly unstable region as well. Thẽ c * = 0 boundary is coincident with a distinct θ * contour (figure 5b), on which the value of θ * is equal to the inviscid value. The value of θ * seems to abruptly increase as we enter thec * > 0 region. In the third quadrant of the (tan Γ, tan Θ) plane, we observe similar characteristics as in the first quadrant, but with the θ * variations occurring in the neighbourhood of θ * = π instead of θ * = 0. Finally, the characteristics of dominant instability in the second and fourth quadrants of the (tan Γ, tan Θ) plane for Sc = 0.1 are similar to those for Sc = 1.
For Sc = 5, some part of the inviscidly stable regions in the first and third quadrants of the (tan Γ, tan Θ) plane becomes unstable (figure 5g), as observed for Sc = 0.1. In contrast to Sc = 0.1, however,c * > 0 seems to occur predominantly in the inviscidly stable region for Sc = 5. Also, in the first quadrant of the (tan θ, tan Γ ) plane for Sc = 5, θ * decreases as we move into thec * > 0 region. As observed for Sc = 0.1, the dominant instability characteristics in the second and fourth quadrants seem similar to Sc = 1 for Sc = 5. In summary of figure 5, some parts of inviscidly stable regions become monotonically unstable for Sc / = 1, with the extent of instability depending on the value of Sc. Sc / = 1 also introduces the occurrence of the maximum growth rate at finite viscous effects, i.e. c * > 0, with such regions showing θ * distributions that are different from the inviscid limit, i.e. Sc = 1. Figure 6 shows the dominant instability characteristics from within the oscillatory instability regions (brown regions in figures 3 and 4), plotted on the (tan Γ, tan Θ) plane for Sc = 0.1 (a-c) and 5 (d-f ). We recall that oscillatory instability (non-zero imaginary part for the growth rate) does not occur for Sc = 1, and monotonic instability dominates oscillatory instability for each (tan Γ, tan Θ, Sc). Figure 6(a) shows that the entire inviscidly unstable region in the first quadrant is susceptible to oscillatory instability for Sc = 0.1, with the corresponding θ * o being around π/2 close to the origin, and approaching zero for large (tan Γ, tan Θ) (figure 6b). Figure 6(c) shows that oscillatory instability occurs at finite viscous effects (c * o > 0), with rapid variations observed within the inviscidly unstable region. Some part of the inviscidly stable region is also seen to be susceptible to oscillatory instability, with a growth rate that is much smaller than that for monotonic instability. The extent of oscillatory instability is also smaller than that of monotonic instability, as indicated by the neutral stability boundary (dashed line) in figure 6(a). The oscillatory instability features in the third quadrant are similar to those in the first quadrant, with the θ * 0 variations occurring around π rather than 0. Finally, the inviscidly unstable second and fourth quadrants are not affected by oscillatory instability for Sc = 0.1.
For Sc = 5, the inviscidly unstable region in the first quadrant is again entirely susceptible to the oscillatory instability (figure 6d), withσ max o , θ * o andc * o all being relatively large close to the tan Θ = 0 axis. In addition, there is also a small portion of the inviscidly stable region where oscillatory instability is observed, with the corresponding θ * o andc * o being close to zero. Finally, in contrast to Sc = 0.1, the inviscidly unstable second and fourth quadrants are entirely susceptible to the oscillatory instability for  quadrants of figure 6(e) are attributed to the switch of the location of maximum oscillatory instability growth rate from one unstable region to another on the (θ ,c) plane (see brown regions in figure 4(c) for an example of two disconnected oscillatory instability regions on the (θ ,c) plane). For each (tan Γ, tan Θ), we proceed to identify the range of unstable θ on the (θ,c) plane for each of the monotonic and oscillatory instabilities. The width of such an unstable range, indicative of the range of perturbation wave vectors that are unstable, is then plotted as a function of tan Γ and tan Θ for various Sc, as discussed in § 3.3.2. Figure 7 shows the width of unstable θ range on the (tan Γ, tan Θ) plane for the monotonic (a-c) and oscillatory (d-f ) instabilities. The panels (a,d), (b,e) and (c,f ) correspond to Sc = 0.1, 1 and 5, respectively. For Sc = 1 (figure 7b), monotonic instability occurs in a small range around θ * (previously shown in figure 5e) in the region close to the neutral stability boundary (black line) in the first and third quadrants. The unstable θ width increases as we move away from the neutral stability boundary towards the tan Θ = 0 axis. In the second and fourth quadrants, a significant range of θ is monotonically unstable near the tan Θ = 0 and tan Γ = 0 axes. In regard to oscillatory instability, as expected, the entire plane of (tan Γ, tan Θ) is stable for Sc = 1 (figure 7e). In comparison with Sc = 1, the width of unstable θ range for monotonic instability is noticeably larger throughout the (tan Γ, tan Θ) plane for Sc = 0.1 (figure 7a). A similar conclusion holds for Sc = 5 too (figure 7c), with the extent of increase in the width of the unstable θ range being relatively smaller compared with Sc = 0.1. For oscillatory instability, the width of unstable θ is, in general, smaller than that for monotonic instability for both Sc = 0.1 (figure 7d) and 5 (figure 7f ). For Sc = 0.1, the width of the unstable θ range decreases as we move away from the origin (figure 7d). For Sc = 5, oscillatory instability appears in all the four quadrants of the (tan Γ, tan Θ) plane (figure 7f ), with relatively large width for the unstable θ range occurring in a region slightly shifted away from the tan Θ = 0 axis. The regions close to tan Γ = 0 in the second and fourth quadrants correspond to relatively large width for the unstable θ range of the oscillatory instability, which is similar to what we observed for the monotonic instability in figure 7(c). The neutral stability boundaries in figure 5 (σ max = 0) and theσ max o = 0 boundaries for the oscillatory instability in figure 6 are all observed to be straight lines passing through the origin on the (tan Γ, tan Θ) plane, indicating their dependence only on the ratio tan Θ/ tan Γ . As highlighted in § 3.3, tan Θ/ tan Γ represents a modified gradient Richardson number. We proceed to investigate the variation (with Sc) of the critical value of tan Θ/ tan Γ that separates stable and unstable regions. Figure 8(a) shows the regions of monotonic and oscillatory instabilities on the plane of Sc on the x-axis and tan Θ/ tan Γ on the y-axis, with the corresponding neutral stability boundaries shown in blue and red, respectively. The neutral stability boundary for the monotonic instability (blue dashed line) also represents the overall neutral stability boundary, thus rendering the region above the blue dashed line stable. The threshold tan Θ/ tan Γ above which the flow is stable increases as Sc goes away from unity. At Sc = 0.1 or 10, the threshold tan Θ/ tan Γ is around 3.1 times larger than the value at Sc = 1. The neutral stability boundary for the oscillatory instability (red dashed line) lies below the overall neutral stability boundary at all Sc / = 1. In contrast to Sc < 1. the red dashed line for Sc > 1 always remains close to (but above) tan Θ/ tan Γ = 1, reaching a value of 9/8 (see Appendix D) as Sc → ∞. The red solid line captures the lower threshold of tan Θ/ tan Γ below which oscillatory instability does not occur. For all Sc < 1, the red solid boundary occurs below the red dashed boundary, and there exists no red solid boundary for Sc > 1, indicating that oscillatory instability occurs for all Sc / = 1. For Sc < 1, oscillatory instability occurs between tan Θ/ tan Γ = 0 and the red dashed line, whereas the entire region below the red dashed line is susceptible to oscillatory instability for Sc > 1. In other words, a finite (Sc < 1) or an infinite (Sc > 1) range of tan Θ/ tan Γ becomes susceptible to oscillatory instability as soon as Sc becomes different from unity.

Neutral stability boundaries
In the centrifugally unstable regime in the limit of no radial stratification (Φ < 0, N 2 r = 0), oscillatory instability was previously reported only for Sc > 1 (Singh & Mathur 2019), which is consistent with the tan Θ/ tan Γ → −∞ limit in figure 8(a).
In figure 8(b), the blue line shows the variation of θ * , the location of maximum growth rate, along the overall neutral stability boundary, which is the same as that for the monotonic instability. For Sc 1, it is around 1.1 rad, and it decreases towards the inviscid value (3.11) of π/4 at Sc = 1, before decreasing further towards 0.03 rad for Sc 1. In contrast, along the neutral stability boundary (red dashed line in figure 8a) for the oscillatory instability, θ * o increases from around 0.1 rad for Sc 1 towards 0.9 rad for Sc 1. On the lower neutral stability boundary (red solid line in figure 8a) for the oscillatory instability, θ * o is around 0.68 rad for Sc < 1. The variation of θ * corresponding to monotonic instability (cyan dashed and cyan solid lines in figure 8b) along the neutral stability boundaries for the oscillatory instability (red dashed and red solid lines in figure 8a) indicate that the monotonic and oscillatory instabilities are separated in θ when they occur simultaneously. While not shown in figure 8, the separation in θ between monotonic and oscillatory instabilities has been verified in all the regions where they occur simultaneously. Finally, with respect toc * andc * o , they are found to be zero along the neutral stability boundaries for the monotonic (blue dashed line in figure 8a) and oscillatory (red dashed line in figure 8a) instabilities, respectively. Along the lower neutral stability boundary for the oscillatory instability (red solid line in figure 8a), however,c * o is finite and varies significantly.
As shown in Appendix D, it is possible to derive closed form expressions for the neutral stability boundaries on the (Sc, (tan Θ/ tan Γ )) plane. The resulting unstable regions are for the monotonic instability, and for the oscillatory instability. In the centrifugally stable regime (tan Θ/ tan Γ > 0) with zero curvature effects, (3.18)-(3.19) coincide with the neutral stability boundaries of McIntyre (1970).

Reduction of parameters
We have thus far presented our results in terms of five different non-dimensional parameters: two of them describing the base flow (3.4a,b), two more describing the perturbations (3.5a,b) and Sc. It is, however, possible to choose an alternate non-dimensionalization of (3.1) to further reduce the number of governing nondimensional parameters, albeit at the cost of not separating the base flow and perturbation characteristics. Specifically, (3.2) can be re-written as where λ * = (λ + c ν |k| 2 )/(c ν |k| 2 ), and In terms of λ * , instability occurs if Re(λ * ) > 1. We also define a non-dimensional growth rateσ = σ/(c ν |k| 2 ) = max(Re(λ * ) − 1), where σ is the maximum real part of the eigenvalues λ. Unlike the non-dimensionalization used in (3.2), the inviscid limit of c ν = 0 represents a singularity in (3.20), and hence the weakly viscous limit of ν → 0 is not easily recovered. Additionally, the thermal wind relation in (2.5) requires β 1 = β 2 = β. Equation (3.20) shows that instability characteristics are dependent only on three different parameters, namely α 1 − β, α 2 − β and Sc. As shown in Appendix B, the neutral stability boundaries for (3.20) are where s = sgn(1 − Sc). In the limit of Sc = 1, the neutral stability boundaries are governed by (3.22) only.
In summary of this section, we identified new parameters (α 1 − β, α 2 − β, Sc) based on an alternate non-dimensionalization, which allowed us to derive analytical expressions for various instability characteristics. Specifically, expressions for the neutral stability boundaries and the interface between monotonic and oscillatory instabilities on the ((α 1 − β), (α 2 − β)) plane were derived; in addition, it was also shown that monotonic and oscillatory instabilities cannot simultaneously occur for the same values of the parameters. It is, however, noteworthy that the parameters α 1 , α 2 and β are a combination of base flow and perturbation characteristics. The instability characteristics in terms of physically more relevant parameters, which also separate the effects of base flow and perturbations, were earlier presented in § § 3.2-3.3.

Discussion
In this section, we address two different goals, namely (i) to highlight the effects of curvature, an aspect that is relatively less understood, and (ii) to explore typical oceanic regimes and comment on the possibility of the instabilities discussed in § 3.

Effects of curvature
As shown in § 3.3.3, the neutral stability boundaries for the monotonic and oscillatory instabilities are given by (3.18) and (3.19), respectively. In the absence of curvature effects, the neutral stability boundaries are obtained by replacing Γ and Θ by Γ M and Θ M , where Γ M and Θ M are as defined in (3.6a,b). We recall that the subscript M refers to the variables defined in the study of McIntyre (1970), which did not account for curvature effects (see § 3.1); (Γ M , Θ M ) are related to (Γ, Θ) by (4.1a,b) where R c = (V/r)/(∂V/∂r + 2Ω) is a non-dimensional parameter that quantifies the curvature effects. The unstable region (on the (Sc, (tan Θ M / tan Γ M )) plane) corresponding to monotonic instability (3.18) can now be written in terms of tan Γ M , tan Θ M and R c as Correspondingly, the unstable region for oscillatory instability (3.19) can be written as Setting R c = 0 in (4.2)-(4.3) recovers the limit of zero curvature exactly. For R c → ∞, the unstable regions asymptotically approach tan Θ M / tan Γ M < 0 for monotonic instability at all Sc and oscillatory instability for Sc > 1; oscillatory instability does not occur for Sc < 1 at R c = ∞. For R c → −∞, the unstable regions asymptotically approach tan Θ M / tan Γ M > 0 for monotonic instability at all Sc and oscillatory instability for Sc > 1; oscillatory instability again does not occur for Sc < 1 at R c = −∞. In other words, for strongly negative R c , ignoring the curvature effects can result in qualitatively and quantitatively misleading conclusions in terms of which regions on the (Sc, (tan Γ M / tan Θ M )) plane are unstable. Such misleading conclusions are a result of a change in the sign of (1 + R c ) at R c = −1. To quantitatively visualize the effects of curvature, we proceed to plot the neutral stability boundaries on the (Sc, (tan Θ M / tan Γ M )) plane for various values of R c . Figure 10 shows the neutral stability boundaries on the plane of Sc and tan Θ M / tan Γ M for different values of R c . While the region below the boundaries is unstable for R c > −1, the region above the corresponding neutral stability boundary is unstable for R c < −1.
In addition, for all R c , there is a neutral stability boundary for oscillatory instability at tan Θ M / tan Γ M = 0 for Sc < 1 in figure 10(b). In the absence of curvature effects, i.e. R c = 0, the black neutral stability boundaries in figure 10(a,b) are exact. For R c / = 0, the neutral stability boundaries move away from the black boundaries; however, a theory that ignores curvature effects (McIntyre (1970), for example) always predicts the black boundaries as the neutral stability boundaries. For R c > 0 (red boundaries), the regions of both monotonic and oscillatory instabilities are smaller than what a theory with no curvature effects would predict. On the other hand, for −1 < R c < 0 (blue boundaries), the actual regions of instability are larger than at R c = 0. For a given R c > −1, the distance between the exact and the curvature-effect-free neutral stability boundaries increases as Sc moves away from unity. For R c < −1, the regions of instability are above the corresponding neutral stability boundaries (shown in green for R c = −2), which now lie in the negative half of the plane. Therefore, as mentioned earlier, a curvature-free theory would be completely misleading if R c < −1.

Relevant ocean regimes
In this subsection, we discuss representative ocean regimes to explore the likelihood of occurrence of the instabilities described in this study. As shown in figure 8(a), the values of Sc and tan Θ/ tan Γ determine if an eddy is susceptible to any short-wavelength instability, be it inviscid or due to differential diffusion between momentum and mass. With respect to Sc, molecular diffusion gives Sc ≈ 7 for temperature in water, and Sc ≈ 700 for salinity in water. In highly turbulent flows, the effective diffusion rates for momentum and scalar fields are often assumed to be nearly equal, resulting in a turbulent Schmidt number value near unity (Kays & Crawford 1993;Kays 1994). The turbulent Schmidt number being close to unity, however, is not necessarily valid in stably stratified turbulent flows, as highlighted by numerical simulations (Venayagamoorthy & Stretch 2010) and field data (Salehipour et al. 2016). Specifically, Sc can vary from around 0.7 at small Richardson numbers, to around 20 at large Richardson numbers (Elliott & Venayagamoorthy 2011). In addition, the buoyancy Reynolds number also plays a role in determining the value of turbulent Sc (Salehipour & Peltier 2015). Based on the definition in (3.3), Θ can be physically interpreted as the orientation of isopycnals with respect to the vertical direction. Therefore, its value can range from being very small at front locations (steep isopycnals) to being very large far from fronts (horizontal isopycnals). As a consequence, the magnitude of tan Θ/ tan Γ is close to zero at sharp fronts, and is infinitely large when horizontal stratification is not present, i.e. far from the fronts. Further, in a stable stratification (N 2 z > 0), the sign of tan Θ/ tan Γ would be the same as the sign of Φ. Given the possibility of tan Θ/ tan Γ taking any value in (−∞, ∞), it is important to accurately estimate the effective Sc in various settings. As noted in figure 8(a), the departure of Sc from unity can both increase the range of unstable tan Θ/ tan Γ and introduce the possibility of oscillatory instability.
It is also worthwhile to discuss the importance of curvature effects in various oceanic settings. In mesoscale eddies, for example, the current speed and radius are, respectively, of the order of 1 m s −1 and 100 km. These values give estimates for V/r and ∂V/∂r as 10 −5 s −1 . For cyclonic eddies, as the latitude varies from 0 (equator) to 90 • (poles), the curvature parameter in (4.1a,b) varies from 1 to 0.064. Correspondingly, for anticyclonic eddies, it varies from 1 at the equator to ∞ at a latitude of around 4 • N, and then becomes strongly negative slightly northward; R c then reaches a value of −1 at around 8 • N, before asymptotically increasing towards −0.074 at 90 • N. The latitude at which R c reverses sign will be larger for stronger current speeds or smaller eddies. As shown in figure 10, R c can significantly affect the stability criterion, and a curvature-effect-free theory would therefore be error prone.
Another feature of importance in sub-mesoscale oceanic eddies is their finite extent in both the horizontal and vertical directions. Specifically, intra-thermocline eddies tend to be around 10-20 km and 200-600 m in horizontal and vertical extents, respectively (Nguyen et al. 2012), and are often modelled as pancake vortices. Depending on the vorticity distribution, Reynolds number, Froude number, Burger number and Schmidt number, these pancake vortices can be in different instability regimes, including barotropic and baroclinic instabilities Storer, Poulin & Ménesguen 2018), short-wavelength instabilities such as symmetric and double-diffusive instabilities (Negretti & Billant 2013;. Some of these instabilities are recognized as driving mechanisms for density layering observed in oceanic eddies (Hua et al. 2013). Of specific relevance to our study are the results of , who performed global stability analysis to investigate short-wavelength and other instabilities in Gaussian pancake vortices.  also presented results for Sc / = 1, to show that oscillatory instability (McIntyre 1970) occurs at Sc = 700 but not at Sc = 7. To recall from our results (figure 8), for Sc > 1, the entire centrifugally unstable regime is conducive to the oscillatory instability as well; the Gaussian pancake vortex, however, contains centrifugally stable and unstable regions. It would therefore be insightful to evaluate the local stability criteria (and identify the most unstable perturbations corresponding to monotonic and oscillatory instabilities) on all the streamlines in the Gaussian pancake vortex considered by , to subsequently establish a relation between the local and global stability results.

Conclusions
In this study, we performed a local stability analysis of a stratified, axisymmetric vortex in thermal wind balance, which represents a model for large-scale vortices in the ocean and atmosphere. The results are also relevant for fronts that appear in the vicinity of eddies. Using the local stability approach, which is alternate to the conventional normal mode approach of McIntyre (1970), our results extend those of McIntyre (1970) to include both curvature effects and centrifugally unstable regimes. In addition, the limit of small but finite viscous effects are easily recovered with the non-dimensionalization used in our study; this allowed us to explore the entire plane of perturbation characteristics at base flow conditions that were far from the neutral stability boundaries. The local stability framework was first shown to recover the well-known symmetric instability in the inviscid limit ( § 3.2). The study then focused on the effects of Schmidt number, which represents the ratio between momentum and mass diffusivities.
In the viscous, double-diffusive regime, the instability characteristics were shown to depend on five non-dimensional parameters: two base flow parameters, two perturbation parameters and Sc ( § 3.3). Two different instabilities, monotonic and oscillatory, were shown to occur for Sc / = 1. Monotonic instability, which is the same as symmetric instability at Sc = 1, can occur for inviscidly stable (absence of symmetric instability) parameter values if Sc / = 1; correspondingly, inviscidly unstable parameter values can become stable for Sc / = 1. Oscillatory instability, characterized by a non-zero imaginary part in the growth rate, occurs only for Sc / = 1. The modification of monotonic and oscillatory instability regimes due to Sc / = 1 were then discussed in detail in the entire parameter space, including the centrifugally unstable regime ( § § 3.3.1-3.3.2). For a given base flow and Sc, the monotonic instability dominates the oscillatory instability in terms of the growth rate, although both instabilities cannot occur simultaneously for the same perturbations. Neutral stability boundaries on the plane of Sc and a modified gradient Richardson number (tan Θ/ tan Γ ) were then identified for both monotonic and oscillatory instabilities ( § 3.3.3). The monotonic instability was shown to significantly extend into the tan Θ/ tan Γ > 1 region when Sc moves away from unity (for both Sc < 1 and Sc > 1). The oscillatory instability, which does not occur at Sc = 1, was shown to occupy a significant portion of the monotonically unstable region in tan Θ/ tan Γ > 0 for Sc < 1. For Sc > 1, oscillatory instability extends into the entirety of inviscidly unstable (−∞ < tan Θ/ tan Γ < 1) region, with a small excursion to the tan Θ/ tan Γ > 1 region.
In § 3.4, it was shown that it is possible to further reduce the number of governing non-dimensional parameters to three by choosing an alternate non-dimensionalization of (3.1), albeit at the cost of not separating the base flow and perturbation characteristics ( § 3.4). Each of the two newly identified parameters other than Sc represent a combination of base flow and perturbation characteristics. Neutral stability boundaries for both monotonic and oscillatory instabilities were then analytically derived in terms of the aforementioned three parameters. Additionally, it was also shown that monotonic and oscillatory instabilities cannot simultaneously occur for the same values of the parameters. Finally, in § § 4.1-4.2, the implications of our overall results were discussed from two different view points. Specifically, the curvature effects were quantified in terms of a non-dimensional parameter, and it was shown that ignoring curvature effects can be misleading in typical oceanic settings. In addition to curvature effects, non-traditional effects (inclusion of the complete Coriolis force, Gerkema et al. 2008) could also be important, especially near the equator. Indeed, recent studies have shown that the horizontal component of background rotation can significantly affect the symmetric instability (Itano & Maruyama 2009;Kloosterziel, Carnevale & Orlandi 2017;Zeitlin 2018).
In the future, it would be worthwhile investigating the manifestation of the instabilities discussed in this paper in direct numerical simulations, including the nonlinear flow states that would result from these instabilities. To explore short-wavelength instability regimes in realistic oceanic settings, the instability criteria derived in this study could be evaluated in field data (in situ and satellite measurements). The results in this study are also potentially useful in interpreting outputs from large-scale climate models, which often use some constant Sc value, unity or otherwise (Danabasoglu et al. 2012). An interesting follow-up to this study would be to investigate the effects of non-isotropic diffusivity, which is often the case in stratified oceanic settings, and triple-diffusive effects resulting from the different diffusivities of momentum, temperature and salinity. Finally, while the current study focused on short-wavelength instabilities, other instabilities such as Kelvin-Helmholtz and baroclinic instabilities have to be considered too to construct an overall instability regimes diagram.
In the neighbourhood of the oscillatory neutral stability boundary on the (α 1 − β), (α 2 − β) plane, the growth rate Δ is governed by (B10). For given base flow parameters, we first maximize Δ with respect to the perturbation parameters, and then identify the Δ = 0 boundary on the plane of base flow parameters. To maximize Δ with respect to θ, we differentiate (B10) with respect to θ to get and substitute ∂Δ/∂θ = 0. Furthermore, Δ = 0 on the neutral stability boundary we are seeking, thus reducing (D6) to Substituting the expressions in (D1) in (D7) gives the expression for the most unstable θ for oscillatory instability as Recalling from § 3.3.1 thatc = 0 on the neutral stability boundaries in the plane of (Sc, (tan Θ/ tan Γ )) and substituting (D8) in (B11), we obtain the oscillatory neutral stability boundary as tan Θ tan Γ = (3Sc + 1) 2 8Sc(Sc + 1) .