Around latitudes ∣ϕ∣ ≈ 30° where diurnal D1 equals the local inertial frequency f = 2Ωsinϕ, Ω denoting the Earth's rotational vector, several mechanisms can enhance shear at f due to a reduction in vertical scales. This would imply locally enhanced deep-ocean mixing. Here, recent 1.5 years of acoustic Doppler current profiler (ADCP) observations from the Canary Basin demonstrate largest kinetic energy at semidiurnal tides (D2), but a complete absence of D2-shear. Instead, shear is peaking at subinertial 0.97 ± 0.01f and terdiurnal 3f(≈D2 + f ≈ D3 here), and vertical scales Δz(f) < 0.1Δz(D2). However, the f-band is broader than deterministic tidal frequencies and the smallest vertical scales, organizing shear in thin layers, are found at the lower inertio-gravity wave limit, which equals 0.97f for the weakest stratification observed (N = 6f, using Δz = 10 m). Hence, besides possibly subharmonic resonance, other mechanisms must be involved in enhancing f-shear, including non-linear harmonic interactions and wave trapping at the critical latitude's poleward shift.
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 The importance of internal waves for mixing in the deep-ocean, with likely implications for the meridional overturning circulation and distribution of suspended material, has led to renewed investigations in ocean shear. As linear waves do not mix, somehow a transition is required to non-linearity, so that large-scale internal waves' induced vertical (z) current shear S = (∂u/∂z, ∂v/∂z), for horizontal current components (u, v), may cause small-scale waves to break resulting in irreversible mixing. In this paper, the primary question is the transfer of energy from large to small scales and the possible associated change in dominant frequency σ. The question is addressed analyzing open ocean moored current and shear observations at latitude ϕ = 30.0012 ± 0.0009°N, at which f = K1, a diurnal tidal harmonic constituent, ≈S2/2, half the semidiurnal tidal solar constituent.
 One of the reasons for choosing this site is that one of the main candidates for an energy transfer from large to small scales, at σ/2, is parametric sub-harmonic instability or, in other words, sub-harmonic resonance (SR), besides direct K1-forcing and a more general mechanism of non-linear interaction [Xing and Davies, 2002]. A similar mooring at f = M2/2, half the semidiurnal lunar constituent, was lost. Although suggestions have been made for SR's possible relevance in the ocean, time scales seemed far too long O(100 days) [Olbers, 1976; McComas and Bretherton, 1977], until renewed modeling demonstrated much smaller scales O(5 days) [Hibiya et al., 2002; MacKinnon and Winters, 2005; Gerkema et al., 2006]. Observations using microstructure profiler suggested enhanced mixing around the critical diurnal latitude [Hibiya and Nagasawa, 2004]. Historic half-year long moored current meter data demonstrated greatly enhanced (factor of 10) kinetic energy at f in a relatively broad band ϕ ≈ 28 − 30°, although without diurnal harmonic peaks at M1, N1 or S1 and extending poleward of the critical latitudes, besides 50%-decreased levels at M2 [van Haren, 2005]. The spatial extent seems small when SR is associated with internal wave beams near their topographic source. After the first bottom reflection of the M2-beam into the interior, the M1− and M3-signals are lost in the model by Gerkema et al. .
 In the present paper, long open-ocean acoustic Doppler current profiler (ADCP-) data are analyzed focusing on 30-m shear and spectral variations with a view to examining the role of SR and other non-linear effects in determining the energy distribution in the internal wave spectrum.
2. Data and Background Conditions
 An upward looking 75 kHz RDI-Longranger ADCP was mounted at 1450 m in the large elliptically shaped top-buoy of a 3700 m long mooring in the Canary Basin, North-Atlantic Ocean (Table 1). Nearest topography was 450 km away. The mooring showed <1.5° tilt angle implying very small mooring motions across <100 m in horizontal and <1.2 m in vertical directions. Currents are estimated as averages over the beam spread, which varies between 30–440 m depending on the range from the ADCP. The fairly large triangularly weighted transmission length of nearly 40 m ensures relatively accurate ensemble averaged u, v (±5·10−3 m s−1) at the expense of loss of vertical resolution. However, this length corresponds well with the vertical scale Δz ∼ 25 m, which represents dominant ocean shear scales [Orlanski and Bryan, 1969; Gregg, 1989; Hibiya et al., 2002] to within ∼30%.
Table 1. Upward Looking ADCP Mooring Details
Water depth, m
Beam slant angle, deg
Transmission length, m
Instrument depth, m
First bin, m
# bins x bin size, m
60 × 10
Ensemble period, s
 The present data quality is generally high, especially further from the ADCP, due to the larger amounts of scattering material associated with layers of larger density stratification. From SeaBird-911 CTD-data around times of mooring deployment and recovery it is observed that the ADCP ranges through the lower parts of Mediterranean outflow water, as evidenced from occasional passages of a Mediterranean eddy (‘meddy’). The buoyancy frequency is not small, N > 20 ± 10f using Δz = 25 m, f = 0.7292·10−4 s−1 (1.0027 cpd, cycles per day).
 The 1.5 years mean kinetic energy (Ek) spectra show the familiar harmonically sharp M2, N2 and S2, with the first containing the largest energy in the spectrum. The second largest value, nearly at σ = K1 = f for this ϕ, is in a moderately broad f-band that, naturally, coincides with the diurnal band D1 without sharp peaks at harmonics (Figure 1). Henceforth, an (over-)harmonic diurnal band will be indicated as ‘Dx’, x = 1,2,3,4 etcetera, when no specific tidal constituent is indicated. Two minor energetic bands are observed in the spectrum, D4, a familiar first harmonic of D2 and attributed to non-linear advection, and D3, an unfamiliar harmonic frequency but including a familiar inertial-tidal interaction frequency [Xing and Davies, 2002]. D3's direct (tidal potential) forcing is commonly quite weak [Cartwright and Taylor, 1971] and only rare occasions have been reported of resonance-enhanced amplitudes [Huthnance, 1980]. However, it may represent here a non-linear inertial-tidal coupling as D3 = f + D2 ≈ D1 + D2.
 In contrast, the 30-m shear spectrum consists of only two peaks: at f/D1 and D3 (Figure 1). Possible peaks at D2 and D4 do not significantly extend above the background, non-white ‘noise’, which is a most dramatic comparison with Ek of up to 2 decades in variance for the tidal D2-constituents. As a result, the vertical scales Δz(D2) > 10Δz(f). This is observed throughout the ADCP's range, although details of peak heights vary slightly. Over time, never a significant D2-peak is observed in the 30-m shear, in any of the monthly sub-spectra (not shown).
 The shear spectrum does not show peaks as narrow as Ek(M2, N2, S2), although weak sub-peaks are discernable within the relatively flat f-band (Figure 1b). Whilst the Ek(f)-“peak” frequency σp(f) is slightly blue-shifted with respect to f, σp(f) = 1.02 ± 0.01f, the shear spectrum for the f-band S(f) shows a tendency for red-shift, with a mean σp(f) = 0.97 ± 0.01f. Recall that M1 = 0.9638f, here, whilst no peak is observed at K1. The standard deviation is for 1.5 years' mean shear at many different depth levels. For individual z-levels in Figure 1bσp = 0.966 ± 0.003f. In time, S(f) over the first 200 days (<day 570, before the obvious passage of a meddy, Figure 2), demonstrates a slightly further red-shift as σp(f) = 0.96 ± 0.015f (not shown), whilst in the period >day 600 mean S and Ek have σp(f) = 0.99 ± 0.015f. In the former period, shear spectra are slightly more peaked at f and have larger variance by ∼1/3 decade at D3 than in the latter period, whilst no noticeable change in D2-constituents is found between the periods. Only at σ < f and some σ = D3 the vertical current difference variance equals twice the Ek − variance, implying maximum shear (currents showing permanently 180° phase difference).
 The association of D3 with f is also observed in the time domain (Figure 2). The f-shear shows a flat pancake pattern reflecting the regularly maximum shear is confined to relatively thin layers. Shear magnitude remains large (>2π/f) for 3–6 days in such layers. D3-current component amplitudes are, like f-current components, more homogeneous in the vertical, except for the odd sudden transition. There, large D3-shear is found, which shows larger vertical coherence than S(f) over roughly 2Δz(f), still smaller than Δz(D2). The S(D3) polarization coefficient CR(D3) = 0.63 ± 0.15, much less than CR(f) = 0.96 ± 0.04 (CR = 1 denotes purely circular motions, CR = 0 rectilinear). These values correspond well with a linear internal wave model: CR = 1,0.62 for f,D3, respectively [Gonella, 1972]. Furthermore, large S(D3) do not coincide (in z,t) with those of large S(f), especially when the vertical f-phase difference is not equal to 180°. As a result, the relatively smooth S(f) detailed pictures become more frayed at the edges, which implies that total shear magnitude varies over shorter time scales than sub-inertial scales for near-circular S(f).
 Thin, O(10–100 m) layering of “large-scale” shear is commonly observed in the upper ocean [e.g., Alford and Pinkel, 2000]. However, depending on the observational tools, much thinner layering O(1 m) in near-surface stratification and shear is observed as well [Marmorino et al., 1987; van Haren, 2000]. In all these observations, ∣S∣ seems relatively larger at f than at M2, despite the usually larger Ek at the latter, and the shear is largest at the depth of largest stratification. This can be due to proximity of the atmosphere as its passing disturbances are considered a major source for inertial motions.
 For the deep ocean interior not many prolonged detailed observations exist on such layering, following classic vertical profiler observations [Leaman and Sanford, 1975]. The present long record of, somewhat limited in vertical resolution, moored ADCP-data shows a similar trend as in the near-surface observations: in the ocean interior S(f) ≫ S(D2). This confirms the general notion that, outside source regions, internal tides predominantly have large vertical scales [e.g., St. Laurent and Garrett, 2002], but these scales are exceptionally large at the present site. However, this does not rule out the role of internal tides on ocean mixing, because they may generate near-inertial motions and shear in the interior. Two possible mechanisms to explain the fairly large Ek(f, D3) near the critical diurnal latitude are distinguished: a non-linear transfer of energy from D2 → D1, D3, and SR.
 The observational latitude is “exactly” critical for SR-generated S1, and just 1.2° north of the f = M1-latitude. Despite this latitudinal discrepancy, the result of SR(M1) is still expected to be somewhat noticeable due to finite horizontal scales [MacKinnon and Winters, 2005]. Indeed, relatively large Ek(f) and S(f) are observed, but much less peaking at M1, S1 [and not at all at N1] than is expected from a direct transfer from sharp harmonic Ek(M2, N2, S2). Consequently, a spring-neap cycle is not observed in shear. Either, Ek contains relatively large barotropic D2-energy and very little barotropic D1-energy, or the SR-generated D1 rapidly transfer energy to neighbouring ‘noise’ internal wave bands, or SR is not the only mechanism transferring energy to small inertial scales. Small-scale motions are more subject to non-linear interactions, which may broaden spectral peaks and thus blur SR-evidence away from a local source, e.g. near a continental slope [Gerkema et al., 2006]. As with previous data [van Haren, 2005], bicoherence analysis of the present data yields virtually no significant results supporting SR (not shown), which is not surprising as sharp harmonic M1,S1 are not observed. Two more problems occur in explaining the observed f-band directly using SR. Firstly, the shear spectrum ‘peaks’ at M1, but Ek(f) not. The latter's σp(f) = 1.02 cpd is not half a known [tidal] constituent. Secondly, if the shear's σp(f) = 0.97 cpd represents SR[M1], the associated free waves must have propagated poleward, which is impossible in traditional internal gravity wave theory (using large N).
 Alternatively, the relatively broadband, and slightly blue-shifted, Ek(f) point at “locally”, to within 100 km in latitudinal direction, generated inertial motions following a geostrophic adjustment process. This may be through an atmospheric storm, but also through thin strongly stratified layers tilted by horizontally short-scale internal [tidal] waves, although the precise mechanism for enhancement at this locality is not obvious despite strong insolation. The observed red-shift in S(f) may then reflect trapping of poleward propagated waves at the extension of the lowest inertio-gravity wave (IGW)-limit σl to sub-inertial frequencies σl < f accounting for local weak stratification (weakest observed N = 6f using Δz = 10 m, yielding σl ≈ 0.97f). At σ = σl (and σ = σh > N) the shortest IGW-scales are found. Except for spatially and temporally localized low-frequency vorticity areas, this is the only means for internal inertial waves to propagate poleward from their f-latitude. The fact that here σl ≈ M1 seems merely a coincidence and similar sub-inertial f-peaks have also been observed at high latitudes [van Haren, 2006].
 As the non-sharp harmonic f-peak is reflected in D3 in the present data, D3 is a non-linear interaction reaction [not SR] result between f and D2, rather than a tidal constituent. It unlikely represents Doppler shifting, because the tidal currents are not the moving source of f/D1, as in the model of [Xing and Davies, 2002] and just like D4 from D2 + D2, confirming the negligible spectral difference between Eulerian and isotherm-following shear observations [van Haren, 2000]. The observed polarization rejects “Doppler shifting” as a dominant explanation for D3 here. This is also suggested from D3(z,t), being in between the pancake appearance of f-motions and the vertically aligned D2. Future investigations should address why S(D3) is not found at the same z-levels as S(f) and the reason for the 180°-phase difference or maximum shear across layers of large N, as thin as they may be. Possibly, sub-inertial motions, trapped poleward from their generation latitude in weak-N layers, adjust their shear across large-N layers in which turbulent exchange is [initially] weak.
 In the deep open ocean interior of the Canary Basin 1.5 years of ADCP-data demonstrate that dominant D2-energy is not associated with large vertical current shear at the same frequency: the shear spectrum only shows peaks at f(≈D1) and 3f(≈D3) thereby, more than the Ek-spectrum, resembling the GM-spectrum outside the interaction frequencies. In the vertical, f-scales are at least 10 times smaller than D2-scales, causing f-shear variance 100 times larger than D2-shear. Similar observations were made in shorter ADCP-records above Great Meteor Seamount (GMS), also at ϕ = 30°N, except that D2-tidal amplitudes were twice those presented here. Whilst Ek(f) is 2–10 times larger than observed elsewhere, Δz(D2)2 [shear variance] is 10 times larger [smaller] than elsewhere.
 In z,t, f-shear is organized in flat pancake structures of O(10 m) thickness and 3–6 days duration that are frayed by D3-modulations. The observed z,t,σ separation of S(f) and S(D3) questions (non-)separability in the vertical wavenumber (m-) domain.
 Although Ek(f) and S(f) are much broader than deterministic tidal harmonics, Ek(f) ‘peaks’ at 1.02f and S(f) ‘peaks’ at 0.97f. The latter frequency equals the lower short-wave limit of the IGW-band considering minimum stratification N = 6f (Δz = 10 m), and equals M1. This suggests that Ek(f) is generated locally within 100 km in latitudinal direction by a mechanism that is several times more powerful (or less dissipative) than at other latitudes. It may be SR, in addition to local geostrophic adjustment, provided the resonant frequencies spread energy into the neighbouring bands swiftly, whilst free waves propagate poleward to become trapped at the lower IGW-limit.
 I thank the crew of the R/V Pelagia for deploying the mooring to within 100 m from the intended latitude. Theo Hillebrand and NIOZ-MTM prepared the instrumentation and designed the mooring. The funding of instrumentation by N.W.O. large investment program Long-term Ocean Current Observations (LOCO) is gratefully acknowledged.