The Sea/Land Breeze Hodographs Along the Northern Croatian Coast
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P1.3 THE SEA/LAND BREEZE HODOGRAPHS ALONG THE NORTHERN CROATIAN COAST Maja Telišman Prtenjak* and Branko Grisogono University of Zagreb, Zagreb, Croatia 1. INTRODUCTION summertime anticyclone is further analyzed by the same numerical model as in Prtenjak et al. Many studies analyzed the components of (2006). During the period examined, only a weak the sea/land breeze (SLB) system at different synoptic forcing is present over the northern spatial and temporal scales resulting in a Croatian coast, according to the surface and the considerable amount of SLB-related knowledge upper-level diagnostic charts for Europe. During (e.g. Miller et al, 2003). One of the specific SB such sunny and dry weather conditions, complex characteristics is the clockwise (CW) rotation of SLB development is inevitable there. To assess a theoretical hodograph in time, on the northern the effects of topographic forcing on the hemisphere, due to Coriolis force veering mesoscale wind field, besides the CR (Haurwitz, 1947). Still, the deviations from the simulation, the terrain sensitivity studies (two to standard hodographs in the anti-clockwise be presented) are also performed. From the (ACW) direction were reported at many stations initial topography, the island surface is replaced around the world (e.g. Simpson, 1996). Along by the sea surface making T1 test. The T2 test is the very complex northern Croatian coast, the formed with the initial orography being investigation of the measurements for two substituted with the idealized one where the stations (Malinska and Senj), also revealed the maximum height of the land surface is 10 m. The ACW rotation (e.g., Orlić et al., 1988; Prtenjak simulations start from 00 UTC on 18 June, last and Grisogono, 2007) thus indicating distorted three successive days, and the first ~12 hours hodographs but without a further detailed that are affected by the model initialization are analysis. Therefore we analyze the simulated omitted from the analysis. surface wind field that is obtained by a three- 240 dimensional (3D) nonhydrostatic numerical model for one particular, although typical, SLB case (18-20 June 2000, as in Prtenjak et al., 200 2006). In order to study the cause of the rotation in more detail an analysis on the diurnal base of 160 modeled wind hodographs at several selected < stations is performed. UCKA Op Ri V Y 120 . K RB A P E L 2. DATA AND METHODS ISTRIA Ma VC A 80 Pu-A KRK CRES Se V The description of the 3D nonhydrostatic KB E L E B mesoscale meteorological model MEMO6 may I T be found in e.g. Kunz and Moussiopoulos 40 (1995). It is widely utilized for simulations of 0 coastal flows and it showed a reasonable ability 0 40 80 120 160 200 240 to reproduce the mesoscale phenomena (e.g., X Klaić et al., 2002; Prtenjak et al., 2006) as do the Figure 1. Coarse and fine (rectangle) model other state-of-the-art models used in similar domains, Istria and Kvarner Bay (KB), showing the studies (e.g. Mangia et al., 2004). The model measuring sites (Pu-A = Pula-airport; Op = Opatija, Ri has two horizontal grids; the coarse one (240 x = Rijeka, Se = Senj, Ma = Malinska). Topography 240 km2) where horizontal resolution is ∆x = ∆y contours are given every 100 m between at 0 and = 2 km and the fine one (100 x 100 km2) with ∆x 1700 m. Učka is a mountain situated at the eastern = ∆y = 1 km (Fig. 1). The model top is at 8000 coast of Istria in the Rijeka Bay (RB), and between Krk island and mainland Velebit Channel (VC) is m. found. Here, the well-studied period (the control run, CR) covering the 18-20 June 2000 during a Meteorological stations along the northern Croatian coast (Fig. 1) that have surface hourly ___________________________________________ measurements of wind are Pula-airport, Opatija, Rijeka, Senj and Malinska representing a variety * Corresponding author address: Maja Telišman of geographical details. Prtenjak, University of Zagreb, Faculty of Science, Dept. of Geophysics, Zagreb, Croatia, email: [email protected]. 1 3. RESULTS exists between the CR and T2 test with pronounced CW rotation of the hodograph (Figs. A fine diurnal SLB analysis can only be 3a and 3b). made if the 24-hours wind regimes are In Rijeka, the simulated CR wind hodograph examined. Hence, a particular attention is paid has the CW rotation (Fig. 3c). The hodograph for to the comparison among hodographs and T1 test displays significant differences compared model results for one day, i.e., 19 June 2000. to the CR (Figs. 3c and 3d). In the CR, the The aim is to explain the basic local effects daytime mesoscale eddy with the CW rotation in influencing the wind dynamics at the considered the surface wind field forms inside the Rijeka stations during the particular day. Bay (Prtenjak et al., 2006). A superposition The wind field above Istria forms the daytime between the eddy and the daytime onshore flow convergence zone. At Pula-airport (Fig. 2a), the creates a more pronounced CW rotation in the diurnal wind vectors rotate in the CW direction CR wind than in T1 test. As for Opatija, the since the hodograph shape is under the onshore flow in T1 test has a larger morning influence of convergence zone mentioned wind speed (by 25 %) than in the CR due to the above. Comparing the CR with T1 test, only small roughness length of the sea surface. small changes can be noticed (Fig. 2b). Above During the afternoon, the stronger advection of the station in T1 test, the wind is stronger around the marine air is caused by the higher wind the noon and weaker in the afternoon as speeds. Consequently, the sea-land temperature compared to the CR. The largest difference difference is smaller, as is the daytime wind appears between the CR and T2 test. In the speed, than in the CR. Removing the latter (Fig. 2b), the southwesterly winds blow topography in T2 test, the southwesterly SB is almost for 24 hours over Pula-airport because enhanced by the background wind without the convergence zone develops near the nighttime offshore flow (Figs. 3c and 3d). eastern part of Istria, far away from the station At Senj, the modeled wind hodograph for the (Prtenjak et al., 2006). day examined mimics the shape and the ACW rotation of the climatological hodograph Pula-airport satisfactory (Prtenjak and Grisogono, 2007). In (a) N (b) N 3 3 the CR, the wind in the Velebit channel blows 2 along the mainland coast in front of Senj 2 1 4 1 22 1 4 (Prtenjak et al., 2006). In T1 test, the channeled 7 W 0 W 0 E E 19 flow is not found, and the ACW rotation is still ) 16 4 1 -4 -3 -2 -1 0 1 2 3 4 -4 -3 -2 -1 1 0 1 2 3 4 ) - 7 1 s -1 - 19 -1 22 10 1 16 19 s present in the wind hodograph (Figs. 3e and 3f). m 10 22 ( 16 m ( -2 v -2 v 13 10 7 While the morning SB is stronger, the afternoon -3 -3 13 13 SB is weaker in T1 test and more perpendicular -4 -4 u (m s-1) u (m s-1) to the coastline when compared to the CR. Such S S CR T1 T2 diurnal wind speed arrangement is connected with the lower sea-land temperature difference due to the stronger marine air advection before Figure 2. Surface wind hodographs for Pula-airport noon (as in the case of Opatija and Rijeka). The on 19 June 2000 for (a) the control run (CR) and (b) steep topography with the mountain pass near for the T1 test (without islands) and T2 test (idealized Senj secures favorable conditions for ACW topography lower than 10 m everywhere). The wind veering in the daily wind. After sunrise vectors are directed toward the origin of the (approximately during 8-13 h), upslope coordinate system. The numbers represent local southeasterly wind develops and twists the standard time. southwesterly SB in the ACW sense (Figs. 3e and 3f). During the afternoon (13-19 h) the In Opatija, comparing the morning wind diminishing slope wind is replaced by the valley speed in the CR and T1 test, it is seen that the wind. The SB and valley winds coincide, and absence of islands increases the wind speeds therefore, there is no significant modification in (Figs. 3a and 3b). The larger speeds cause the afternoon wind directions. During the stronger advection of the cold marine air that is evening, downslope NW wind begins and followed by the lower surface air temperature together with the easterly land breeze forms the during the day. Due to the smaller land-sea offshore flow. The daily wind cycle is completed temperature difference, the wind speed by the superposition of the fully formed mountain decreased by ~50% in the afternoon. An wind, land breeze and downslope northeasterly additional reason for the overall low wind speed winds. The T2 test once again differs is the absence of both the channeling of the air significantly from the typical wind hodograph flow and the mesoscale eddies near Opatija (Figs. 3e and 3f). Orlić et al. (1988) argued that inside the Rijeka Bay. The largest difference the mountain/valley and slope winds presumably 2 appear around Senj and their associated pressure gradient would be closely parallel to Malinska (a) N (b) N the coast. The results of numerical experiments 4 4 16 3 3 are in agreement with this hypothesis, ) 1 13 - 2 s ) 1 2 - m s reproducing the anomalous wind regime around 22 ( 1 7 v m 4 ( 1 13 16 v 0 Senj.