The response of the velocity profile (on the left panel) NSC 683864 solubility dmso to the down-estuary wind in the middle Bay shows that, for most of the time, it was landward with a vertical shear (an indication of a wind-straining regime), whereas in the lower and upper portions of the Bay, the velocity profile oscillates between seaward and landward directions without much of a vertical shear (an indication of the presence of a well-mixed regime). With the above analysis, it is natural to ask if one can describe the interaction between the straining and mixing to form a parameter to represent the wind-induced variations in stratification.

CS has defined the modified horizontal Richardson number, which is combined with the Wedderburn number (W), as: equation(9)

(Rix,CS)2=(H4Nx4/48KM)(1-W)Rf(u∗S3/khS+u∗B3/khB)where Nx   (≈gβΓ  ) is the horizontal buoyancy frequency, KM   is the effective vertical eddy viscosity ( Dyer, 1997), and u∗Su∗S and u∗Bu∗B are the root-mean-square values of friction velocities on the surface and bottom layers, respectively. The surface and bottom boundary layer thickness (hS   and hB  ) are estimated by an entrainment model ( Trowbridge, 1992 and Chant et al., 2007): equation(10) hS=2γRiC1/2u∗S2N∞Δt,hB=2γRiC1/2u∗B2N∞Δtwhere γ   is a constant (=1.22), Ric   is the critical gradient Richardson number (=0.25), Δt   is Fasudil a characteristic time scale chosen as 3 h, and N  ∞ represents background stratification. Following Ralston et al. (2008), KM   is assumed to scale as a  0CdUtℓ  , where a0 = 0.028 and ℓ   is a vertical mixing length scale. When the surface and bottom boundary layers merge (hS+hB⩾HhS+hB⩾H), ℓ scales with H. Otherwise, the average of hS and hB is used for ℓ (CS, 2009). For values of Rix,CS greater than a threshold value (of order 1), the water column should stratify, and for sub-critical values the water column should remain unstratified ( Stacey et al., 2001).

The modified horizontal Ri in Eq. (9) was calculated at selected stations Fenbendazole along the channel of the Bay during both hurricanes. The temporal variation of Rix,CS for three experiments is plotted in Fig. 20a. Without wind forcing, although Rix,CS showed the tidal variability, the minimum values of Rix,CS at the three locations were approximately 0.2, 1.0, and 0.3, respectively ( Fig. 20a). This indicates that tidally induced mixing dominates in the upper and lower Bay, whereas stratification is relatively significant in the mid Bay. In the case of Hurricane Floyd ( Fig. 20a(d)–(f)), Rix,CS decreased at all three locations. The value of Rix,CS dropped below 0.1 in the upper and lower Bay, and reached a value of 0.25 in the mid-Bay. Interestingly, the value of Rix,CS increased rapidly to greater than 1 in the upper and middle Bay regions. In the lower Bay, the value of Rix,CS persisted below 0.1 for one day and then increased until the end of the Floyd wind period.