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5Original Russian Text © A. A. Slepyshev, 2021, published in MORSKOY GIDROFIZICHESKIY ZHURNAL, Vol. 37, Iss. 4 (2021)
Vertical Transfer of Momentum by Inertia-Gravity Internal Waves on a Two-Dimensional Shear Flow
A. A. Slepyshev
Marine Hydrophysical Institute of RAS, Sevastopol, Russian Federation H [email protected]
Purpose. The paper is aimed at investigating the momentum vertical transfer by inertia-gravity internal waves on a two-dimensional flow with a vertical shear of velocity, and also at studying the Stokes drift of liquid particles and the mean current effect on it.
Methods and Results. Free internal waves in an infinite basin of constant depth are considered in the Boussinesq approximation with the regard for the Earth rotation. Two components of the mean current velocity depend on the vertical coordinate. The equation for the vertical velocity amplitude has complex coefficients; therefore the eigenfunction and the wave frequency are complex. The corresponding boundary value problem is solved numerically by the implicit Adams scheme of the third order of accuracy. The wave frequency at a fixed wavenumber was found by the shooting method. It was determined that the frequency imaginary part was small and could be either negative or positive depending on a wave number and a mode number. Thus, both weak attenuation and weak amplification of an internal wave are possible. The vertical wave momentum fluxes are nonzero and can exceed the corresponding turbulent fluxes. The Stokes drift velocity, transverse to the wave direction, is nonzero and less than the longitudinal velocity. The vertical component of the Stokes drift velocity is also nonzero and four orders of magnitude less than the longitudinal component. The signs of the vertical component of the Stokes drift velocity for the waves with the frequencies 10 and 16 cph are opposite, since the signs of their frequency imaginary parts are different; and the vertical component of the Stokes drift velocity is proportional to the wave frequency imaginary part.
Conclusions. The vertical momentum wave flux of inertia-gravity internal waves differs from zero in the presence of the current whose velocity component, transverse to the wave propagation direction, depends on the vertical coordinate. The component of the Stokes drift velocity, transverse to the wave propagation direction, is nonzero and less than the longitudinal one. The vertical component of the Stokes drift velocity is also nonzero and can contribute to formation of the vertical fine structure.
Keywords: internal waves, imaginary correction to frequency, wave momentum flux, Stokes drift
Acknowledgements: the author is grateful to N.O. Ankudinov for numerical calculations in solving the boundary problem. The study was carried out within the framework of the state task on theme No. 0827-2019-0003 "Fundamental investigations of oceanological processes conditioning state and evolution of marine environment being affected by natural and anthropogenic factors, based on the observation and modeling methods".
For citation: Slepyshev, A.A., 2021. Vertical Transfer of Momentum by Inertia-Gravity Internal Waves on a Two-Dimensional Shear Flow. Physical Oceanography, [e-journal] 28(4), pp. 363-375. doi: 10.22449/1573-160X-2021-4-363-375
DOI: 10.22449/1573-160X-2021-4-363-375
© A. A. Slepyshev, 2021
© Physical Oceanography, 2021
The problem of vertical exchange remains relevant at the present time, since it is the vertical exchange that ensures the oxygen supply to the deep layers of the sea and the removal of organic material from the deep layers. This is extremely important for the functioning of the ecosystem. According to existing concepts, vertical exchange is provided by small-scale turbulence [1-4]. However, in the pycnocline region turbulence is strongly suppressed by buoyancy forces.
On the other hand, the pycnocline is a waveguide for internal waves, and it seems relevant to study the contribution of internal waves to vertical exchange. Internal waves propagate mainly by wave trains localized in space [5]. Nonlinear effects during the propagation of trains of internal waves are manifested in the generation of currents averaged on the wave scale [6, 7]. The vertical velocity component of this current has different signs at the leading and trailing edges of the train, and there is no integral vertical transfer. After the wave train passage, the unperturbed stratification profile is reconstructed. A number of works [8, 9] are devoted to the study of the vertical transfer of momentum by internal waves. Vertical wave momentum fluxes are nonzero with allowance for turbulent viscosity and diffusion [8]. In this case, the wave attenuates [10, 11] and the phase shift between the oscillations of vertical and horizontal velocity differs from n/2. For inertia-gravity internal waves in the presence of a current velocity component transverse to the direction of wave propagation, which depends on the vertical coordinate, the vertical wave momentum flux is nonzero even if turbulent viscosity and diffusion are not taken into account. The point is that the boundary value problem for the amplitude of the vertical velocity of internal waves fixed mode has complex coefficients. This problem was solved analytically in [9] at a constant Brunt - Vaisala frequency and a linear current velocity profile. In this case, the wave propagated perpendicular to the flow. It was obtained that the solution of the boundary value problem (eigenfunction of internal waves) is complex, and the wave frequency is real. When internal waves propagate at an angle to a planeparallel flow with no regard to the Earth's rotation, the wave frequency is real and the eigenfunction is real, since the equation for the vertical velocity amplitude has real coefficients [12, 13]. It will be obtained below that in a two-dimensional stratified current, taking into account the Earth's rotation, the wave frequency is complex, and the imaginary part of the frequency can be both negative and positive, i.e. both weak attenuation and weak amplification of the wave are possible. In this case, the vertical wave momentum flux and the vertical component of the Stokes drift velocity are nonzero. In [9], the vertical wave momentum flux is not zero, but the vertical component of the Stokes drift velocity is zero, since the wave frequency is real.
Statement of the problem. In the Boussinesq approximation, free internal waves are considered taking into account the Earth's rotation in an infinite basin of constant depth on a two-dimensional current, two horizontal velocity components U0 (z), V0 (z) of which depend on the vertical coordinate. In the linear approximation, the boundary value problem for the amplitude of internal waves vertical velocity is numerically solved, and the complex frequency of internal waves fixed mode at a constant wavenumber is found. In the second order in wave amplitude, the Stokes drift velocity of liquid particles and vertical wave momentum fluxes are found.
Hydrodynamics equations for wave disturbances have the form
Du dUn 1 dP
_ v+=__1_dP, (1)
Dt dz p0 (0) dx
Dv ~Dt Dw Dt
fu
dV0 w-— =
dz
1 dP
DP
P0(0) dy gP
P0(0) dz P0(0)
DP _ w dPc , Dt dz '
d u dx
dv
dy
dw "dz
= 0,
(2)
(3)
(4)
(5)
where u, v, w are two horizontal and vertical components of current wave velocity, respectively; p, P are wave disturbances of density and pressure; p0 (z) is an average density profile; x, y, z are two horizontal and one vertical coordinates, z axis is directed upwards; f is the Coriolis parameter; U0 (z), V0 (z) are two velocity
components of mean current; Action of D operator is expanded by the formula
Dt
D d d d d
— _ — + (u + U0) — + (v + V0) — + w —. Using geostrophic relations from [14],
Dt dt dx dy dz
we are to estimate the horizontal scales of mean density variation:
Lx _ P0 / dp0 _ g / f max dx
dVn
dz
, Ly _ P0 / dp0 _ g / f max
dy
dUn
dz
F i g. 1. Vertical profiles of the current velocity components U0, V0
The vertical profiles of the current velocity components are demonstrated in Fig. 1. The maximum values of the modulus of vertical gradients of current velocity components U0, V0 are 0.067 and 0.011 l/s, respectively. The horizontal
scales of density variation are equal to Lx = 8.283 -106m, Ly = 1.398-106 m,
respectively, and they are much larger than the wavelength, therefore, the horizontal density variation is neglected.
The boundary condition on the sea surface z = 0 is the "rigid lid" condition that filters internal waves from the surface waves [15]:
w(0) = 0. (6)
The boundary condition at the bottom is impermeability condition:
w(-H) = 0, (7)
where H is a sea depth.
Linear approximation. We seek solutions of linear approximation in the following form:
u1 = u10(z)Ae'e + c.c., v1 = v10(z)Ae'e + c.c., w1 = w10(z)Ae'e + c.c.,
(8)
P = p0(z)Ae'e + c.c., p1 = p10(z)Ae'e + c.c.,
where c.c. are complex conjugate terms; A is an amplitude factor; e is a wave phase (de/dx = k, de / dt = -ro, k is a horizontal wavenumber, © is a wave frequency). It is assumed that the wave propagates along x axis.
After substituting (8) into system (1) - (5), the amplitude functions
U10, V10, P10, P0 are linked with ww :
i dw
U10 =
10
Po(0) k
k dz
Q dw,n dU,
Q = ®-k-Un
k dz dz
10 , dU 0 w + f dVo w J dWlO)
Wio (l~TWio ^^--~>
Q dz
f dwio
k dz
Pio =-Q W10-
1 ( f dw
Q\ k
dVn
- iwu
(9) (10) (11)
Function w10 satisfies the equation
d 2 wu dz2
+kw,,
f
dUr,
Q2 - f2 Q(Q2 - f2)
dw
k(N2 -Q2) + Q
d U
-if
d 2V
Q2 - f2
dz dz
Q( Q2 - f2)
= 0,
(12)
where n2 ___g dp° is a square of Brunt - Vaisala frequency.
P0(0) dz
Boundary conditions for w10 :
at z _ 0 w10 _ 0, (13)
at z _-H w10 _ 0. (14)
Boundary value problem (12) - (14) was solved analytically in [9] at a constant Brunt - Vaisala frequency and a linear velocity profile of a planeparallel mean current. The wave propagated perpendicular to the flow. It was found that the eigenfunction - the solution to this boundary value problem - is complex, and the wave frequency is real. Below, while carrying out numerical calculations, it will be shown that the wave frequency is complex in a two-dimensional current.
In [16], equation (12) was solved by the perturbation method by expanding
the solution in a series in a small parameter 8 _ V0* /(Hro*), where V0*is characteristic value of current velocity and ro* is the characteristic wave frequency. However, this parameter is not always small and is the applicability of the method is limited. Therefore, in the present work, the implicit Adams scheme of the third order of accuracy is used for the numerical solution of equation (12) for real profiles of Brunt - Vaisala frequency and current velocity.
Boundary value problem (12) - (14) was solved analytically in [12, 13, 17] for a plane-parallel flux with a linear current velocity profile at f = 0, N = const in case when the wave propagates at an arbitrary angle to the flow. A dispersion equation containing modified Bessel functions is obtained. In [17], only the first three terms were left in the expansion of the Bessel functions in a series; therefore, the imaginary part of the phase velocity is greater than zero even at the Richarson
N2 1
number Ri _-- > , which contradicts the Miles criterion [18, 19] of a plane-
'dU Y 4
dz
parallel flow hydrodynamic stability. However, in [12, 13], the same dispersion equation was solved numerically and asymptotically, and no contradiction to Miles criterion of hydrodynamic stability was found. In [20], for an arbitrary planeparallel flow with a continuous velocity profile at N _ const, no contradiction to the Miles criterion was also revealed.
It is of interest to compare the numerical solution of boundary value problem (12) - (14) according to the implicit Adams scheme of the third order of accuracy with the analytical solution [9] for a plane-parallel flow with a linear flow velocity profile at N _ const when the wave propagates perpendicular to the flow. For the first mode 15-minute internal waves with ro _ 0.00698132 rad/s frequency, a numerical calculation provides the wavenumber value k _ 0.0418831513 rad/m. If this value is substituted into the formula for the frequency of the analytical solution (20) from [9], then the frequency value is ro _ 0.00698133 rad/s. The frequency difference from numerical solution is 10-4%. A similar calculation
for the second mode gives a discrepancy between the numerical and analytical solutions for the frequency in 3 • 10-4 %.
Now we are to compare the numerical solution of the boundary value problem (12) - (14) according to the implicit Adams scheme of the third order of accuracy with the analytical solution from [12] for a plane-parallel flow with a linear velocity profile at f= 0, N = const, when the wave propagates at an arbitrary angle to the flow. For this purpose, we use the second model of the flow velocity from [12], when the specified velocity is zero at the bottom. Wave frequency ro in [12] (normalized to the Brunt - Vaisala frequency) was taken equal to 0.54 in dimensionless variables. Let p, v be the projections of the dimensionless wave
vector (normalized to n/H) onto the directions along and across the flow. Then, for v = 0.5 the numerical solution of the boundary value problem (4) in [12] according to the implicit Adams scheme of the third order of accuracy provides the value p = 0.1742 for the first mode, which corresponds to both the numerical and asymptotic solutions of the dispersion equation (5) in [12].
Nonlinear effects. The Stokes drift velocity of liquid particles is determined by the formula from [21]:
: j (UJXV)U ,
(15)
where u is a field of Euler wave velocities, the bar above means averaging over the wave period. The horizontal velocity component of the Stokes drift, directed along the wave vector, up to terms quadratic in the wave amplitude, has the form
u =
A A
1 d
a dz
w,
dwio dz
-c.c.
(16)
where A1 = A exp(5a • t ), Sra = Im(a) is an imaginary part of wave frequency.
The horizontal component of the Stokes drift velocity transverse to the wave propagation direction is determined by the formula
v, = Ai A
-A A*
1 dw,.
bQ k dz
dw
dVn
if- k^
dz
dz
+ c.c.
bQ2
Q
dw10 dV0 if d2w10
dz dz k dz2
■ + w,
d V
dz2
+ k
dU 0 dz
dV0 if dw 1(
dz k dz
+ c.c. !
(17)
In the presence of an average current, for which the velocity component V0 transverse to the wave propagation direction depends on the vertical coordinate, the value vs is nonzero. The vertical component of the Stokes drift velocity is proportional to the imaginary part of the frequency and is determined by the formula
1 1 I d(
ro ro J dz
w.
= iA1 A1 I---* l-H w10 w10
f,~\ fi\ /7-7 V
).
(18)
We find vertical wave momentum fluxes uw, vw taking into account (8),
The vertical wave flux of momentum vw in formula (20) is nonzero and in the absence of flow, the flux of momentum uw in formula (19) is nonzero only in the presence of an average current, for which the velocity component V0
transverse to the direction of wave propagation depends on the vertical coordinate. In the absence of the Earth's rotation at f = 0, the wave momentum fluxes are equal to zero.
Calculation results. We will analyze the vertical momentum fluxes for internal waves and the Stokes drift velocity using the results of the third stage of the 44th cruise of R/V Mikhail Lomonosov in the area of the Black Sea northwestern shelf 1. The profiles of two components of the mean current velocity are given in Fig. 1, the Brunt - Vaisala frequencies are depicted in Fig. 2.
(9), (11):
(19)
z, m
-60
-20
-40
0.01 0.02 0.03 N, rad/s
F i g. 2. Vertical profile of the Brunt - Vaisala frequency
1 MHI AS USSR, 1985. Report on the Work in the 44th Cruise (3rd Stage) of R/VMikhail Lomonosov, August, 7 - September, 15. Sevastopol: MHI AS USSR. Vol. 1, 135 p. (in Russian). PHYSICAL OCEANOGRAPHY VOL. 28 ISS. 4 (2021) 369
Boundary value problem (12) - (14) of determining the mode vertical structure is solved numerically according to the implicit Adams scheme of the third order of accuracy. The wave frequency at a fixed wavenumber is found by the shooting method from the need to fulfill the boundary conditions (13), (14). The eigenfunction (the solution to the boundary value problem (12) - (14)) is complex, therefore the vertical wave flux of momentum uw (18) is nonzero. The dependences of real and imaginary wave frequency parts on the wave number for the first two modes are shown in Fig. 3, 4. In Fig. 3 the dispersion curves of the first two modes are given, ®0 = Re(®) is the real part of the frequency.
■lir 1 o -i
-3
-5
"""
r
\ Kj 1 1 1
0.05 0.1 0.15 k, rad/m
F i g. 3. Dependence of the wave frequency real F i g. 4. Dependence of the wave frequency part on the wave number for the first 1 and imaginary part on the wave number for the first 1 second 2 modes and second 2 modes
In Fig. 4, the imaginary part of frequency for the first mode is negative at k < 0.055 rad/m and positive at k > 0.055 rad/m are demonstrated. In absolute value, the imaginary part of the frequency is three to four orders of magnitude less than the real part of the frequency. Thus, the first mode has a weak attenuation in the low-frequency region at k < 0.055 rad/m, and weak wave amplification in the high-frequency region at k > 0.055 rad/m. In the second mode, the imaginary part of the frequency is always negative, i.e. the wave attenuates weakly. In the first mode attenuation region, the attenuation decrement for the second mode is greater in absolute value.
It is of interest to study the vertical momentum fluxes and the Stokes drift velocity for the first mode waves with different signs of the imaginary part of the frequency, for example, for internal waves with frequencies of 10 and 16 cph (meaning the real part of the frequency). For a wave of the first mode with a 10 cph frequency, the imaginary part of 5®=- 8.378-10-7 rad/s is negative. For a wave of
the same mode with 16 cph frequency, the imaginary part of 5® =1.379 -10-6 rad/s is positive. Therefore, further we will compare the vertical wave momentum fluxes and the Stokes drift velocity for these waves. In Fig. 5 the profiles of vertical momentum fluxes uw for internal waves of the first mode with 0.5 m amplitude and frequencies of 10 cph (red line) and 16 cph (blue line), as well as turbulent flux
u w
(green line) are given.
UJ - V dU0
The turbulent momentum flux is determined by the formula u w =- Kz ,
zdz
the coefficient of vertical turbulent exchange - by the formula Kz = 0.93 • 10-4 N— m2/s ( Nc corresponds to the Brunt - Vâisâlâ frequency in cph) [22, 23]. In general,
with the exception of 15-25 m depth interval, the turbulent flux prevails over the wave flux. The wave momentum flux for waves with 10 cph frequency prevails over the flux for waves with a frequency of 16 cph in the depth interval of 15-40 m. In the upper 15-meter layer, there is a slight predominance of the flux for waves with a frequency of 16 cph. Deeper than 40 m, wave fluxes are comparable in magnitude.
F i g. 5. Profiles of the wave uw and turbulent F i g. 6. Profiles of the wave vw and turbulent u'w' vertical momentum fluxes v'w' vertical momentum fluxes
In Fig. 6 the profiles of vertical fluxes of momentum vw for internal waves of the first mode with 10 cph (red line) and 16 cph (blue line) frequencies, as well as
turbulent flux v1 w' (green line) are demonstrated.
The turbulent momentum flux is determined by the formula v1 w! =- KzdV°.
z dz
The dominance of turbulent flux over the wave flux is already absent here. In 2.540 m depth interval of the waves with 10 cph frequency vertical momentum flux
vw exceeds the turbulent one in absolute value. For the waves with 16 cph
frequency, the vertical momentum flux vw is less than for the waves with 10 cph frequency.
It is of interest to compare uw and vw fluxes with each other. In Fig. 7 the profiles of these fluxes for the first mode waves with 10 cph frequency are
represented. In general, uw flux (red line) is noticeably inferior to vw flux (blue line).
Now we are to compare the Stokes drift velocity for internal waves of the first mode with 10 and 16 cph frequencies. The vertical profiles of the Stokes drift velocity component along the wave propagation direction (formula (16)) are demonstrated in Fig. 8 for the waves with 10 cph (red line) and 16 cph frequency (blue line). The structure of the profiles of the Stokes drift velocity longitudinal component is very similar, only in the upper 10-m layer and deeper than 30 m the Stokes drift velocity is higher for the waves with 10 cph frequency.
F i g. 7. Profiles of the wave uw vw vertical F i g. 8. Vertical profiles of the longitudinal momentum fluxes component of the Stokes drift velocity
o
: m -20
-40
4 -2 0 2 4 10"4
us, m/s
Fig. 9. Profiles of the Stokes drift velocity F i g. 10. Vertical profiles of two components component transverse to the wave propagation of the Stokes drift horizontal velocity direction
-1? .5 0 5 JO"
i.. i.i s
The vertical profiles of the Stokes drift velocity component transverse to the direction of wave propagation (formula (17)) for waves with 10 cph (red line) and 16 cph (blue line) frequencies are demonstrated in Fig. 9. Here, in the upper 25-m layer, the moduli of the maximum and minimum values of this velocity component for the waves with 16 cph frequency is higher, while deeper than 25 m
and up to 48 m depth, the Stokes drift velocity prevails for the waves with 10 cph frequency.
It is of interest to compare the Stokes drift velocities along and across the direction of wave propagation. In Fig. 10 the vertical profiles of these velocity components for the waves with 10 cph period are presented. The Stokes drift velocity us along the direction of wave propagation (red line) noticeably exceeds
the transverse velocity vs (blue line).
F i g. 11. Profiles of the vertical component of the Stokes drift velocity
Now we are to compare the vertical component of the Stokes drift velocity (formula (18)) for waves with of 10 and 16 cph frequencies. In Fig. 11 the maximum (in modulus) velocity prevails for the waves with frequency 16 cph (blue line). The directions of vertical component of Stokes drift velocity for the waves with 10 and 16 cph frequencies are opposite, since it is proportional to the imaginary part of frequency and differs in sign. The magnitude of the vertical component of this velocity is very small, four orders of magnitude less than the velocity along the direction of wave propagation. However, it can make a significant contribution to the vertical heat and salt transfer, as well as to the vertical fine structure generation [24].
Conclusions
1. Vertical momentum fluxes of wave uw, vw of internal waves at two-dimensional shear flow with regard to the Earth rotation differ from zero and can be comparable or exceed corresponding turbulent fluxes.
2. The imaginary part of wave frequency differs from zero and is negative for the second mode - weak wave attenuation takes place. In the first mode
the attenuation occurs in the low frequency area at k < 0.055 rad/m, at k > 0.055 rad/m a weak wave amplification takes place.
3. The Stokes drift velocity along the direction of wave propagation noticeably exceeds transverse velocity.
4. The vertical components of the Stokes drift velocity of the first mode waves with 10 and 16 cph frequencies has different signs due to the fact that it is proportional to the imaginary part of frequency.
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About the author:
Aleksandr A. Slepyshev, Leading Research Associate, Marine Hydrophysical Institute of RAS
(2 Kapitanskaya St., Sevastopol, 299011, Russian Federation), Dr. Sci. (Phys.-Math.), ResearcherID:
V-6948-2017,' ORCID ID: 0000-0002-9259-7558, IstinaResearcherID (IRID): 3614585,
The author has read and approved the final manuscript.
The author declares that he has no conflict of interest.
