The same takes place in the case of onshore winds except for the southward shift of radiance maxima ( Figure 3, (d)–(f)). The radiances of moderate intensity extend tens of kilometres further westwards in the case of the offshore wind as compared to the onshore one. This difference peaks at latitudes corresponding to Y ∼ 150–200 km ( Figure 3). The differences dLoff–onwnav (λ) = Loffwnav (λ) − Lonwnav (λ), where Loffwnav (λ) and Lonwnav (λ) are binned radiances at offshore and onshore winds, are mapped in Figure 4. The maximum dLoff–onwnav (λ) are comparable to the Loffwnav (λ) in magnitude, are located between the 10 and 15 m isobaths and extend from 90 to 180

km in the y-axis and from 140 to 200 km in the x-axis. In Figure 5, the zonal profiles of the Nutlin-3a in vitro bottom relief are compared to the profiles of radiance differences dLwnav at 443, 555 and 670 nm. It is evident that (1)dLwnav distributions west of the shallow are flat and exhibit minor between-profile distinctions; find more (2) profile segments at depths Z < 30 m indicate substantial enhancement of Loffav (λ) against Lonav (λ) at sites with moderate steepness of the sea floor (profiles (d)–(g)) and a virtually zero radiance difference at greater bottom steepness (profiles (a) and (b)); (3) profiles of dLav (443) and dLav (555) have the highest magnitude

and resemble each other in position and shape, but a number of dLav (670) profiles appear to be shifted eastwards and differ in shape from the corresponding radiance profiles at shorter wavelengths (d)–(f). The profiles of Loffav and Lonav in Figure 6 demonstrate the following trend: the onshore radiance slightly exceeds the offshore radiance

in the deep-water part of the middle and northern testing area; an inverse relation between them occurs at the western boundary of the shallow; further east, Loffav grows faster than oxyclozanide Lonav but the latter overtakes the former in the vicinity of the coastline. As a result, the summary radiance progression in the presence of easterly and westerly winds looks like a closed loop, whose lower and upper branches correspond to the onshore and offshore events. The eastern intersections of the branches occur at sites of less than a few metres of water, where the insufficient accuracy of the bottom topography model prevents a stricter association of intersections with bottom features. The higher-sensitivity profiles in Figure 6 (dashed) indicate that western intersections occurred at Z > 30 m if r < = 160 km but occurred at sites with 14–30 m of water in profiles at r > 160 km distinguished by roughness of bottom relief in the west of the shallow. In some cases the depth and radiance profiles show conformity in their shape: the two-step structures of the offshore branch of the radiance loop and of the bottom profile in Figure 6f appear to be a manifestation of such conformity. However, the more intricate relationships of these profiles outnumber the situations of straightforward interpretability.