ureal parameters ol me Sea Breeze and lis vertical structure in the Boston Basin
|
|
- Rosemary Chandler
- 5 years ago
- Views:
Transcription
1 ureal parameters ol me Sea Breeze and lis vertical structure in the Boston Basin James P. Barbato Geography Department Fitchburg State College Fitchburg, Mass Abstract The sea breeze is a mesoscale wind whose frequency of occurrence is times annually in the Boston Basin. Boston's sea breeze is among the best developed of all midlatitude sites studied. The complexity of site conditions and an urban concentration alter the characteristics of the sea breeze with inland penetration. Vertical temperature and dew point data have provided the first detailed look at the changes effected in Boston's atmosphere by this local wind. The data have also revealed that Boston's sea breeze is not always a moist flow of marine air but that the moisture content of the air is directly related to the regional wind speed and direction prior to onset of the sea breeze. Transformations of the vertical characteristics of the atmosphere suggest subtle but serious geographic and environmental variations in the spatial distribution of atmospheric contaminants. 1. Introduction The sea breeze is a mesoscale wind system whose frequency of occurrence is related to the establishment of strong temperature gradients induced by the differential heating of adjacent land-sea surfaces. The sea breeze affects the climatology of the Boston Basin some 40 or 50 times annually during the spring, summer, and fall months. Other factors that affect the sea breeze are 1) topography, 2) concavity of the coast, and 3) coastal water temperatures. Urban Boston is situated in a basin surrounded by a low upland rim of higher terrain. Relief in the hemispheric-shaped basin is subdued; the greater part of the lowland is <15 m above sea level. Terrain roughness is not an important factor within the basin, but it becomes a significant topographic constraint along the basin's margin. The most prominent escarpment is located along the west and northwest, where elevations rise abruptly m. The high elevations of the basin rim delay the inland progress of the sea breeze. Only 15 of the 40 sea breeze episodes observed in 1972 penetrated farther inland than the basin rim. The concavity of the coastline complicates the sea breeze penetration at Boston. Sea breezes along straight coastlines advance inland normal to the coast (Fig. 1); however, because of Boston's concave coastline, the flow is initiated normal to the coast and becomes divergent inland as penetration occurs. Additional variations in the flow appear with the passage of time and the effects of the Coriolis force. These will be discussed later in the paper / 78 / $ American Meteorological Society FIG. 1. Generalized sea breeze flow along straight, convex, and concave coastlines. Boston's compact, highly concentrated urban area, with some 2.5 million people, situated along a cold water margin generates two mesoscale breezes: a bay breeze and a sea breeze. The bay breeze is a response to a heated coastline, while the areas adjacent to the immediate coast remain cooler, and is restricted to a very narrow zone along the coast. It is superseded later in the day by the sea breeze. The cold water margin also exerts a strong influence in the seasonal distribution of sea breeze episodes at Boston. Most coastal mid-latitude locations experience their largest number of sea breezes during the spring months, when the temperature contrast between the land and ocean surfaces is normally the greatest (Defant, 1951). Although sea breezes have been recorded as early in the year as February, Boston records its greatest number of sea breeze episodes during th summer months because the temperature contrast between the land-sea surfaces is greatest in July and August at this site. The establishment of sea breezes along the Massachusetts coast may be very localized. Rexroad (1954) reported a vigorous sea breeze at Salem, Mass., but 20 km to the south at Boston, the sea breeze was not present. The combination of elements of the topographic situation, the concavity of the coast, and 1420 Vol. 59, No. 11, November 1978
2 Bulletin American Meteorological Society the large thermal gradients that can become seasonally established impart distinct characteristics to the sea breeze at Boston. Consequently, criteria found in much of the literature defining the sea breeze along relatively straight coastlines cannot be directly applied to the Boston Basin. 2. Criteria for distinguishing the Boston sea breeze Explicit criteria were required to identify a sea breeze episode at Boston. The general considerations of high solar azimuth, clear skies, and anticyclonic circulation were considered too broad since Boston, under certain synoptic conditions, often experiences these conditions accompanied by easterly winds. Six criteria were defined as essential to the identification of a sea breeze episode: 1) The barometer is recording high pressure and anticyclonic circulation prevails with the center of the anticyclone located west of and at a latitude south of Boston (42 N). 2) The amount of sunshine received that day must be ^50% of the amount possible. 3) Prior to onset of the sea breeze, the regional surface wind must be blowing offshore, i.e., westerly. 4) During the sea breeze, an afternoon wind maximum should be evident from the data collected by the National Weather Service (NWS) at Logan International Airport, East Boston, Mass. 5) The temperature trace at Logan Airport, which first experiences the sea breeze because of its location in Boston Harbor, should clearly indicate a change of air associated with a change in the circulation. Thus, the thermograph trace should record either a distinct temperature decrease accompanying onset of the sea breeze, or a retardation of the diurnal temperature curve, or both these factors. 6) The duration of the sea breeze must be ^5 h at Logan Airport. Criteria 1 and 2 are generally synonomous with each other. Defant (1951) indicated that the probability of a sea breeze event was 90% if these two conditions were met. At Boston, criterion 3 would be a westerly wind blowing from 190 to 350. Onset of the sea breeze causes the surface wind to veer or back to an easterly direction of between 15 and 145. These specific values delineate the concavity of the Boston coastline and are, therefore, unique to this site. The requirement that the regional wind be offshore prior to sea breeze onset represented a strict definition of the sea breeze in accordance with Munn (1966). Some early authors (Dolezel, 1945; Wexler, 1946) termed conditions at Boston in which an afternoon wind maximum was superimposed upon an onshore gradient wind a sea breeze. Although this afternoon wind maximum may be associated with 1421 a strengthening of the land-sea temperature gradient, it is not a true sea breeze. Criteria 4 and 5 are selfexplanatory. Criterion 6 was established after testing determined that sea breezes of shorter duration were restricted to the immediate coastline and subject to confusion with the bay breeze. Those whose duration was ^5 h penetrated inland with well defined characteristics. 3. Data base for the climatology of the Boston sea breeze Standard synoptic data from four Massachusetts sites were used: the NWS office at Logan Airport, the Massachusetts Institute of Technology (MIT) in Cambridge, the University of Massachusetts Suburban Experimental Station at Waltham, and Hanscom AFB, Bedford. The first three sites lie along an east-west inland traverse (Fig. 2). The fourth, Hanscom AFB, was included because of its proximity to the traverse and also because its extrabasin location on the nearby upland justified its inclusion as a data site. Radiosonde data were obtained from Environmental Meteorological Support Unit (EMSU) radiosondes launched twice daily from MIT. The EMSU project began in September 1971 and ended in May The radiosondes were released from a 30 m rooftop at 1000 GMT (0500 EST) and 1500 GMT (1000 EST). Data were gathered at 50 m intervals beginning at 30 m and terminating at 3000 m. On occasion, varied work schedules delayed the radiosondes until 1100 GMT (0600 EST) and 1600 GMT (1100 EST). Landsat-1 (launched as ERTS-1) provided the first satellite photograph of a sea breeze episode in the Boston Basin on 28 July This was used to compute inland penetration of the sea breeze front. 4. Various parameters of the Boston sea breeze The various parameters were determined from data for 40 Boston sea breeze episodes in a. Wind field Mean onset and retreat times of the sea breeze were computed to the nearest hour. Onset was defined as the time when the wind shifted from a westerly direction to an easterly wind between 15 and 145 on a day that fulfilled the six criteria previously discussed. Retreat was defined as the time when the mesoscale sea breeze was supplanted by the regional westerly wind. Mean onset of the Boston Basin sea breeze was 1500 GMT (1000 EST) with the mean wind from 100 at 4.7 ms. Maximum wind occurred at 1900 GMT (1400 EST) from 117 at 7.2 ms". Mean retreat took place at 2300 GMT (1800 EST) with the wind veering from 136 at 5.7 m s". These findings significantly differed from Dolezel's (1945) study; however, the differences are a result of the more accurate definition of what constitutes a sea breeze episode at Boston rather than any faulty technique on Dolezel's part
3 1422 Vol. 59, No. 11, November 1978 FIG. 2. Data network in the Boston Basin. The rotation of the wind shift at onset and retreat is presented in Table 1. At onset, the wind field veers from westerly to easterly in 67% of the cases. At retreat, the wind veers from easterly to westerly in 90% (36 of 40) of the episodes. Since the Coriolis force causes the sea breeze to veer throughout the day, the sea breeze TABLE 1. Rotation of the wind shift at onset and cessation of the sea breeze at Boston based on 40 episodes in Rotation Onset, days Cessation, days Through north Through south Total flow is usually from 130 to 140 by late afternoon. As the sea breeze weakens, the veering of the wind continues while the regional westerly wind reestablishes itself. The dominance of the right-hand turning of the sea breeze is quite evident from Table 1. Consequently, it would appear that although the regional synoptic wind affects the rotation of the wind at onset, the Coriolis effect strongly influences the wind rotation direction at cessation time. The combination of the sea breeze and the Coriolis veering of the sea breeze flow illustrates a significant mesoscale wind regime in the Boston Basin. More importantly, the diurnal rotation of the sea breeze wind field suggests more subtle geographic and environmental implications associated with the spatial distribution of
4 Bulletin American Meteorological Society T A B L E 2. Characteristics of the sea breeze at Boston (Logan Airport) based on 40 episodes in Characteristic Onset time, EST Cessation time, EST Duration, h Mean The duration of the sea breeze varied at each site. Tables 2 and 3 present data from the two extremes of the linear traverse. The mean duration of 8.1 h at Logan Airport represents a steady wind field, whereas at Hanscom AFB, near the inland limit of penetration, the 4.6 h mean duration is very misleading. On any given sea breeze day, the wind field may vary in a series of pulsations at Hanscom AFB. One hour the sea breeze may be present, the next hour, absent; however, this behavior was expected because the forcing function (i.e., the thermal gradient) weakens inland. This behavior also established that Hanscom AFB, 28 km inland from Logan Airport, is representative of the limit of inland penetration of the Boston sea breeze. An early study (Davis et al., 1890) reported sea breeze penetrations of km along the Massachusetts-New Hampshire coasts. The absence of a data site farther inland prevented the writer from determining if any of the 15 sea breezes observed at Hanscom AFB penetrated any farther inland. topography The basin's upland periphery was verified as a significant topographic obstacle. In 62.5% (25 of 40 cases), the sea breezes were restricted to the basin lowland, 20.1 km inland from Logan Airport. Where the vector resultant of the frictional component and the Coriolis force balance the pressure gradient driving force, the sea breeze stalls since the major component of the frictional force is generally opposite to the wind. The effect of the upland is to significantly increase the frictional component. d. Rate of advance and retreat Analysis of wind shifts, hence sea breeze arrival times at each site, demonstrated that the sea breeze front advanced at a mean rate of 8.8 km h. Between the coast and Kenmore Square (downtown Boston), inland penetration was rapid at 11.7 km h, while farther inland between Kenmore Square and the Waltham data site, the penetration rate slowed to 4.7 km hr. The sea breeze Characteristics of the sea breeze at Bedford, Mass. (Hanscom AFB), based on 15 episodes in Characteristic Mean Onset time, EST Cessation time, EST Duration, h Duration c. Effect of TABLE Range atmospheric contaminants. The transport wind and basin topography may combine to create mesoscale regions of higher pollutant concentrations along the inland limits of the wind field. These implications will be explored in a forthcoming paper. b Range stalled at the basin's margin in 62.5% (25 of 40) of the episodes studied. The speed of inland penetration at Boston is atypical of most sea breeze observations. Simpson et al. (1977) reported a tendency for an acceleration of the rate of sea breeze advance based on the observations of 76 sea breeze fronts that passed Lasham, England, over a 12-year period. Simpson et al. explained this observed acceleration of the front in terms of increased temperature contrast at the front due to the decrease of solar heating of the sea air. Simpson et al. concluded that their observations confirmed the conclusions of a numerical model developed by Neumann and Mahrer (1975) in which one of the most interesting developments of the model depicted the most rapid rates of inland penetration occurring a few tens of kilometers inland. Yet Simpson et al. (1977) acknowledge that sea breeze observations in more complex terrain (the California coast) by Fosberg and Schroeder (1966) have demonstrated contrary resulfs. Fosberg and Schroeder observed the marine air penetrating rapidly early in the day but slowing down later in the day. The Boston Basin is neither the California coast nor Lasham, but the concave coast, the basin rim, and the urban sprawl serve to categorize the area as different. It is possible that the increased temperature contrasts responsible for the rapid inland penetration occur between the coast and the concrete-asphalt landscape of Boston. As the sea breeze front accelerates across the city and reaches the basin margin (also the location of the more vegetated suburbs), the temperature contrasts may be less and the speed of inland penetration reduced. Certainly, the lack of universal agreement suggests that additional research on the relationship(s) between site conditions and the rate of ea breeze advance may be warranted. Retreat or cessation of the sea breeze within the entire basin occurred in ^1.0 h in 80% of the cases examined. Retreat rates ranged from a rapid 24.4 km h to a low of 7.4 km h". On 14 occasions, data from the inland sites at Waltham and Hanscom AFB demonstrated that the sea breeze was still in progress but data from the NWS at Logan Airport indicated that the sea breeze flow had terminated. Further examination of the data revealed that the sea breeze cell was bifurcating along the coast at cessation time. A similar bifurcation and increase in the landward component of the sea breeze in the very lowest layer along the Rhode Island and New York City coastlines at sunset was reported by Fisher (1961) and by Frizolla and Fisher (1963, p. 738), _1 1
5 1424 Vol. 59, No. 11, November 1978 who concluded... that such accelerations probably are a sensitive function of local conditions when small variations between the drivirlg force provided by the horizontal temperature gradients and friction become important. It is therefore likely that the bifurcations and accelerations of the sea breeze at Boston are similar to those observed by Frizolla and Fisher. e. Vertical limits The EMSU radiosonde data made it possible to determine for the first time the vertical extent of the Boston Basin sea breeze. Figure 3 was prepared using those da,y& in 1972 when the sea breeze was present in the 1000 EST (1500 GMT) EMSU sounding at MIT. The difference in wind direction between the 0500 EST (1000 GMT) and 1000 EST (1500 GMT) sounding is particularly evident at the 30 rri level (the height of the rooftop from which the radiosondes were launched at MIT). The actual depth of the sea breeze circulation was derived by determining that height in the radiosonde sounding where the wind veered or backed from the 15 to 145 compass heading. Those wind directions represent the dominant criterion of the sea breeze flow in the Boston Basin. Deviations from these compass headings in the vertical wind profile delineate the upper boundary, or vertical extent, of the inland flow of air into the Boston Basin. It should be noted that a return wind flow aloft (in the case of Boston a seaward flow) is an integral part of the solenoidal sea breeze cell. The orientation of the basin and its geographic location in the westerly wind belt are such that the sea breeze return flow is superimposed in the regional wind field that persists at altitudes above the surface inland component of the sea breeze. The vertical depth (height) of the sea breeze flow in the Boston Basin as determined from the EMSU 1972 data is given below. Date Depth of Inland Flow, m 25 April April April July July July August September 530 The mean depth of the Boston Basin sea breeze was 667 m and ranged from a maximum vertical extent of 1230 m to a minimum depth of 330 m. The shape of the FIG. 3. Vertical wind profiles for 8 sea breeze days in 1972 prepared from EMSU sounding data. The number after the feather indicates wind directions. If the wind shaft is between 0 and 90 and the number is a 1, it signifies a wind from 10. If the shaft is between 90 and 180, the 1 designates a wind from 110, etc. North is toward the top.
6 Bulletin American Meteorological Society 1425 basin appears to exert little or no effect upon the vertical development of the sea breeze since the vertical depth measurements are comparable with those reported for other mid-latitude sites by Sutcliffe (1937), Defant (1951), Fisher (1960), and Frizolla and Fisher (1963). In fact, the vertical development of one (2 August) of the Boston sea breezes was quite large. The probable explanation for this great vertical extent was the development of a particularly strong temperature gradient. The EMSU measurements have permitted the determination of the vertical extent of Boston sea breezes. However, it should be noted that most sea breezes at Boston penetrate the coast after midmorning. Consequently, the 1000 EST (1500 GMT) sounding is representative of very early sea breeze passages. It is therefore quite probable that as the sea breeze flow intensifies, a greater vertical extent may develop later in the day. /. Effect on surface temperature and dew point values The temperature and moisture parameters of sea breezes were among the first characteristics of sea breezes studied. Craig et al. (1945) constructed a series of sea breeze cross sections from temperature and psychometric measurements made by balloon and airplane ascents through sea breezes along a line from Marshfield (30 km southeast of Boston) eastward to Provincetown, Mass., on the terminus of Cape Cod. The results of their study demonstrated a marked temperature and moisture gradient across the sea breeze front. The effects of the Boston Basin sea breeze upon temperature and dew point values were consistent with those reported in the literature. Two marked variations in the diurnal temperature profile occurred, depending upon whether onset of the sea breeze was midmorning or delayed at Logan Airport (Fig. 4). On 2 October a 1500 GMT (1000 EST) onsfet produced a flattened temperature profile and retarded the daily maximum temperature. The 1700 GMT (1200 EST) delayed onset of 3 October demonstrated a sharp decline in the temperature profile as cooler air advanced inland. The control day (8 October), used for comparisons, was the closest day with anticyclonic circulation to the 2 sea breeze days except that a sea breeze did not develop. The temperature profile for the control day more closely approximated the expected bell-shaped temperature profile. In 70% (28 of 40) of the sea breeze days, a mean decrease of 3.3 C from the normal temperature was recorded. In 30% (12 of 40) a mean increase of 2.1 C from the normal was observed. Of these, 75% (9 of 12) were those days when onset was delayed (similar to 3 October) and hence the temperature profile rose correspondingly before rapidly declining after onset. Dew point temperatures demonstrated a double pattern. Days with an early, well-defined onset (2 October) depict a marked increase in the dew point temperature (Fig. 4). Late onset times produced a smaller and more poorly defined increase in the dew point temperatures FIG. 4. Temperature and dew point profiles for selected sea breeze days and a control day in (3 October). The data for 4Q sea breeze days in 1972 revealed that the increase in dew point values accompanying onset was between 1.1 C and 3.3 C. It was discovered that much of the variability in dew point values was associated with the wind direction and speed of the previous night. All sea breeze days that experienced significant increases in atmospheric moisture were those days on which the transport wind prior to onset of the sea breeze was ^2.6 m s~\ Air moved offshore had sufficient residence time over the water to be humidified before being entrained in the sea breeze flow and returned landward. Those days with transport wind speeds >2.6 m s -1 prior to onset produced dew point temperature increases ranging from C to 1.1 C.
7 1426 Vol. 59, No. 11, November 1978 g. Vertical temperature distribution Vertical temperature data from radiosonde ascents launched at MIT at 1000 and 1500 GMT provided an opportunity to examine the impact of the sea breeze on the vertical temperature distribution. Data were gathered every 50 m beginning at 30 m (the height of the rooftop from which the radiosondes were released). Examples of representative soundings for spring, summer, and fall sea breeze episodes are presented in Figs. 5, 6, and 7. Figure 5 depicts soundings that are similar to each other fbr 3 sea breeze days (25, 26, 27 April) along with the profile for the control day (1 May), which represents a typical temperature profile on the closest non-sea breeze day with anticyclonic circulation. The large temperature differentials at all levels between the sea breeze days and the control day represent the impact of the cold water adjacent to Boston's coastline in the spring. The significance of the sea breeze as a climatological phenomenon in advecting cooler air landward cannot be underestimated. Higher summer temperatures but similar differentials in temperature are evident in Fig. 6. Figure 7 is representative of a late summer-early fall episode. h. Vertical dew point temperature distribution Detailed radiosonde soundings have provided the first precise look at the vertical moisture distribution during a sea breeze episode. A representative profile (Fig. 8) FIG. 5. Vertical temperature profiles for selected days in 1972.
8 Bulletin American Meteorological Society 1427 for 27 April 1972 illustrates a large dew point temperature increase (8.7 C) that accompanied the 1600 GMT sea breeze inflow 530 m in height. The dew point temperature increase accompanying the 28 July 1972 onset was 2.5 C. Values in this range were more typical (Fig. 9). The most striking result of the analysis of the vertical dew point temperature profiles accompanying onset of a sea breeze was that many profiles did not reveal an increase in atmospheric moisture accompanying the sea breeze flow. Several conclusions were made regarding the sea breeze vertical moisture distribution. The vertical EMSU profiles demonstrated that both shallow (330 m) and deep (1230 m) sea breeze circulations were capable of advecting extremely moist air into the Boston Basin. It was also observed that several sea breezes produced soundings in which the expected increase in the vertical moisture profile was absent. The vertical moisture distribution was found to be entirely dependent upon the regional synoptic wind prior to onset. All sea breeze days that experienced increases in the vertical moisture profile were those on which the speed of the transport wind prior to onset was <2.6 m s _1. The air advected eastward over Boston Bay and the Atlantic Ocean was moving slowly enough to be humidified and returned landward as part of the sea breeze flow. Those days on which the speed of the regional westerly winds was >2.6 m s _1 demonstrated minimal effects on the FIG. 6. Vertical temperature profiles for selected days in 1972.
9 1428 Vol. 59, No. 11, November 1978 FIG. 7. Vertical temperature profiles for selected days in moisture profiles. The residence time of this fastermoving air over the water was so brief that it was not humidified before it was returned inland in the sea breeze. 5. Conclusions The spatial characteristics of the sea breeze in the Boston Basin have illustrated its role as a dynamic mesoscale wind system. The results from the transect line revealed that the rate of inland penetration varied from 4.7 to 11.7 km hr and that these values were within the range considered 1 as normal for a mid-latitude site. Inland penetration of the sea breeze varied. The majority of sea breezes stalled along the topographic boundary of the basin. Those sea breeze episodes that advanced farther inland reached their maximum limits of penetration km from the base data point at Logan Airport. The sea breeze was found to diverge inland along a hemispheric arc that delineated the sea breeze front as analogous to a miniature macroscale cold front. The effect of the Coriolis force was evident in the right-hand turning of the sea breeze wind as the day progressed. Vertical analysis of the sea breeze circulation resulted in several findings. The vertical extent of the sea breeze
10 Bulletin American Meteorological Society 1429 inflow was found to vary between 330 and 1230 m, which is also within the normal range for a sea breeze in the middle latitudes. The vertical temperature profiles were shifted to the left; i.e., lower temperatures were recorded at each successive pressure surface on sea breeze days. Dew point temperature data from 30 m illustrated that the increase accompanying the sea breeze ranged from +0.6 C to +8.7 C. The study of the temporal characteristics determined that 40 sea breezes annually was a normal level of occurrence for a mid-latitude site. However, the cold water margin of Boston skewed the frequency and season of occurrence from the normal spring maximum to a midsummer maximum (July and August). Two effects on the temperature regime were noted. A flattening of the diurnal temperature profile accompanied all sea breeze episodes, and the diurnal maximum temperature on sea breeze days was below the normal for those dates as cooler air was advected inland off the water. The results of the dew point analysis produced an unexpected finding. Historically, it was assumed that the sea breeze advected moist marine air inland. This analysis determined that the speed of the wind in the Boston Basin prior to onset of the sea breeze was instrumental in de- FIG. 8. Vertical dew point profiles for 27 April 1972.
11 1430 Vol. 59, No. 11, November 1978 FIG. 9. Vertical dew point profiles for 28 July termining whether moist air would be advected inland. If the speed of the evening and early morning wind was >2.6 m s _1, the air advected seaward would have had little time to become humidified. Hence, the sea breeze would advect the air, which had recently arrived over the water from a prior land trajectory, back inland. The rotation of the sea breeze wind by the Coriolis force during the afternoon hours emphasized that even mesoscale wind systems are subject to certain macroscale forces. Furthermore, it has also been shown that the sea breeze advects cooler, more stable marine air into the basin behind a frontal zone, exhibiting vigorous turbulent motion, similar to the passage of a macroscale cold front. The three later characteristics, i.e., the Coriolis effect, the frontal zone, and the transport of more stable air inland, provide an indication that, aside from its spatial and temporal characteristics, the sea breeze may also affect the urban atmosphere in a manner previously unrecognized. The turbulent motions at the sea breeze front and the potential "piling up" of atmospheric pollutants in advance of the front by the regional wind may be responsible for significant short-term increases of pollutants accompanying the onset of the sea breeze. Furthermore, the cooler, more stable marine air may restrict the ability of the urban atmosphere to diffuse and disperse gaseous contaminants. Consequently, it is
12 Bulletin American Meteorological Society 1431 a logical assumption that potential increases in contaminant levels may be recorded during a sea breeze episode in the Boston Basin. Similarly, the combination of the turning of the sfea breeze wind by the Coriolis force and the tendency of the frontal zone to stall along the basin's periphery may demonstrate that particular geographic locations within the Boston Basin, especially the northwest quadrant, may experience a serious decline in air quality, while sensors located closer to the coast are recording acceptable background contaminant levels. These hypothesized effects suggest that the validity of these statements concerning the transformation of the ventilation characteristics of the Boston urban atmosphere be examined since the magnitude and scope of the effect of the sea breeze in transforming the urban atmosphere may be particularly significant to air quality levels in the Boston Basin. The author plans to report on these effects in a paper currently in preparation. References Craig, R., I. Katz, and P. J. Harney, 1945: Sea-breeze cross sections from psychrometric measurements. Bull. Am. Meteorol. Soc., 26, Davis, W. M., L. G. Schultz, and R. DeC. Ward, 1890: An investigation of the sea breeze. Ann. Harvard College Observ., 21, Defant, F., 1951: Local winds. Compendium of Meteorology, edited by Thomas Malone, AMS, Boston, pp Dolezel, E. J., 1945: Ari analysis of the sea breeze in the Boston area. AAF Weather Station, MIT, Cambridge, Mass. (Unpublished manuscript.) Fisher, E. L., 1960: An observational study of the sea breeze. /. Atmos. Sci., 17, Fosberg, M., and M. Schroeder, 1966: Marine air penetration in central California. J. Appl. Meteorol., 5, Frizolla, J. A., and E. L. Fisher, 1963: A series of sea breeze observations in the New York City area. J. Appl. Meteorol 2, Munn, R. E 1966: Descriptive Micrometeorology. Academic, New York, 245 pp. Neumann, J., and Y. Mahrer, 1975: A theoretical study of the lake and land breezes of circular lakes. Mon. Wea. Rev., 103, Rexroad, F. H., 1954: Boston's east wind. Weatherwise, 7, 60-63, 67. Simpson, J. E., D. A. Mansfield, and J. R. Milford, 1977: Inland penetration of sea breeze fronts. Quart. J. Roy. Meteorol. Soc., 103, Sutcliffe, R. C., 1937: The sea breeze at Felixstowe: A statistical investigation of pilot-balloon ascents up to 5500 feet. Quart. J. Roy. Meteorol. Soc., 63, Wexler, R., 1946: Theory and observations of land and sea breezes. Bull. Am. Meteorol. Soc., 27, announcements continued from page 1419 Directory of upwelling researchers The Scientific Committee on Oceanic Research (SCOR) Working Group 56, Equatorial Upwelling Processes, is assembling a directory of scientists and engineers interested in physical arid biological processes of upwelling occurring within the Upper ocean in the region between 15 N and 15 S. Scientists and engineers primarily interested in the biological aspects of equatorial upwelling should send name, affiliation, and address to: Dr. Richard T. Barber, Chairman, SCOR WG 56 Biological Panel, Duke University, Marine Lab., Beaufort, N.C Those primarily interested in the physical aspects of equatorial upwelling should contact: Dr. David Halpern, Chairman, SCOR WG 56 Physical Panel, NOAA Pacific Marine Environmental Lab., th Ave. N.E., Seattle, Wash Climatological data summaries The National Climatic Center (NCC) has recently published Climatography of the U.S. No. 20 (Substation Summaries) and the revised and updated Climatography of the U.S. No. 60 (Climate of the States). Climatography of the U.S. No. 20 includes climate summaries for 1063 NWS cooperative climatological observing stations in all 50 states and Puerto Rico. The 4-page data summaries contain for each location a means and extremes table; sequential tables for monthly and annual mean maximum, mean minimum, and average temperature, total precipitation, and total snowfall; monthly normals ( ) of temperature, precipitation, and total heating and cooling degree days; probability statistics for monthly precipitation; and probability statistics for spring and fall freeze dates and the length of the growing season for five temperature thresholds. These summaries were prepared for stations with a complete record for and are based upon the period of record 1951 through the latest complete year of record available at the time of preparation. Climatography of the U.S. No. 60 has been revised and reprinted for each of the 50 states and for Puerto Rico and the U.S. Virgin Islands combined. It contains a narrative description of the general climate of the state (or area), the normals, means, and extremes table for each First Order Station in the state, and the means and extremes table for those substations in the state that are included in Climatography of the U.S. No. 20. Copies of these publications are available from NCC. The "Substation Summaries" are priced at $0.15 per station; "Climate of the States" is priced at $0.50 per state. Requests for copies should be addressed to: Director, National Climatic Center, Federal Bldg., Asheville, N.C (tel: , ext. 683). Continued on page 1473
Air Pressure and Wind
Air Pressure and Wind 19.1 Understanding Air Pressure Air Pressure Defined Air pressure is the pressure exerted by the weight of air. Air pressure is exerted in all directions down, up, and sideways. The
More information2. THE NEW ENGLAND AIR QUALITY STUDY
P2.4 NEW ENGLAND COASTAL AIR POLLUTION DISPERSION MODELING Michael Tjernström * and Mark Žagar Stockholm University, Stockholm, Sweden Wayne Angevine CIRES, University of Colorado, and NOAA Aeronomy Laboratory,
More informationChapter. Air Pressure and Wind
Chapter Air Pressure and Wind 19.1 Understanding Air Pressure Air Pressure Defined Air pressure is the pressure exerted by the weight of air. 19.1 Understanding Air Pressure Air Pressure Defined Air pressure
More informationASSESSMENT OF SEA BREEZE CHARACTERISTICS FROM SODAR ECHOGRAMS
ASSESSMENT OF SEA BREEZE CHARACTERISTICS FROM SODAR ECHOGRAMS SUNEETHA RANI. JUPUDI Prof. M. PURNACHANDRA RAO Department of Physics, Andhra University, Visakhapatnam, India. ABSTRACT The SODAR echograms
More informationMcKnight's Physical Geography 11e
Chapter 2 Lecture McKnight's Physical Geography 11e Lectures Chapter 5 Atmospheric Pressure and Wind Michael Commons Ohio Northern University Atmospheric Pressure and Wind The Nature of Atmospheric Pressure
More informationAugust 1990 H. Kondo 435. A Numerical Experiment on the Interaction between Sea Breeze and
August 1990 H. Kondo 435 A Numerical Experiment on the Interaction between Sea Breeze and Valley Wind to Generate the so-called "Extended Sea Breeze" By Hiroaki Kondo National Research Institute for Pollution
More information18.1 Understanding Air Pressure 18.1 Understanding Air Pressure Air Pressure Defined Measuring Air Pressure Air pressure barometer
18.1 Understanding Air Pressure 18.1 Understanding Air Pressure Air Pressure Defined Air pressure is the pressure exerted by the weight of air. Air pressure is exerted in all directions down, up, and sideways.
More informationWinds and Ocean Circulations
Winds and Ocean Circulations AT 351 Lab 5 February 20, 2008 Sea Surface Temperatures 1 Temperature Structure of the Ocean Ocean Currents 2 What causes ocean circulation? The direction of most ocean currents
More informationSection 1. Global Wind Patterns and Weather. What Do You See? Think About It. Investigate. Learning Outcomes
Chapter 5 Winds, Oceans, Weather, and Climate Section 1 Global Wind Patterns and Weather What Do You See? Learning Outcomes In this section, you will Determine the effects of Earth s rotation and the uneven
More informationChapter 6: Atmospheric Pressure, Wind, and Global Circulation
Discovering Physical Geography Third Edition by Alan Arbogast Chapter 6: Atmospheric Pressure, Wind, and Global Circulation Factors That Influence Air Pressure Air Pressure is the measured weight of air
More informationSea and Land Breezes METR 4433, Mesoscale Meteorology Spring 2006 (some of the material in this section came from ZMAG)
Sea and Land Breezes METR 4433, Mesoscale Meteorology Spring 2006 (some of the material in this section came from ZMAG) 1 Definitions: The sea breeze is a local, thermally direct circulation arising from
More informationThe ocean water is dynamic. Its physical
CHAPTER MOVEMENTS OF OCEAN WATER The ocean water is dynamic. Its physical characteristics like temperature, salinity, density and the external forces like of the sun, moon and the winds influence the movement
More informationOcean Circulation. Si Hui Lee and Frances Wen. You can access ME at
Ocean Circulation Si Hui Lee and Frances Wen You can access ME at http://tinyurl.com/oceancirculation Earth - the blue planet - 71% area covered by the oceans - 3/4 of ocean area between 3000-6000m deep
More informationMeteorology I Pre test for the Second Examination
Meteorology I Pre test for the Second Examination MULTIPLE CHOICE 1. A primary reason why land areas warm up more rapidly than water areas is that a) on land, all solar energy is absorbed in a shallow
More informationINTRODUCTION * Corresponding author address: Michael Tjernström, Stockholm University, Department of Meteorology, SE-
4.12 NEW ENGLAND COASTAL BOUNDARY LAYER MODELING Mark Žagar and Michael Tjernström * Stockholm University, Stockholm, Sweden Wayne Angevine CIRES, University of Colorado, and NOAA Aeronomy Laboratory,
More informationRead each slide, some slides have information to record on your organizer. Some slides have numbers that go with the question or red and underlined
Read each slide, some slides have information to record on your organizer. Some slides have numbers that go with the question or red and underlined to use for answering the questions. Essential Question:
More informationABSTRACT INTRODUCTION
Numerical investigation of the formation of elevated pollution layers over the Los Angeles air basin Rong Lu, R.P. Turco Department of Atmospheric Sciences, University of California, Los Angeles, 405 Hilgard
More informationLecture 22: Ageostrophic motion and Ekman layers
Lecture 22: Ageostrophic motion and Ekman layers November 5, 2003 1 Subgeostrophic flow: the Ekman layer Before returning to our discussion of the general circulation of the atmosphere in Chapter 8, we
More informationPGF. Pressure Gradient. Wind is horizontal movement of the air or other word air in motion. Forces affecting winds 2/14/2017
Winds Wind is horizontal movement of the air or other word air in motion. Forces affecting winds 1. Pressure gradient force a. High pressure flows to low pressure b. Pressure gradient = difference in pressure
More information2.4. Applications of Boundary Layer Meteorology
2.4. Applications of Boundary Layer Meteorology 2.4.1. Temporal Evolution & Prediction of the PBL Earlier, we saw the following figure showing the diurnal evolution of PBL. With a typical diurnal cycle,
More informationGoals for today: continuing Ch 8: Atmospheric Circulation and Pressure Distributions. 26 Oct., 2011
Goals for today: 26 Oct., 2011 continuing Ch 8: Atmospheric Circulation and Pressure Distributions Examples of synoptic scale and mesoscale circulation systems that are driven by geographic diversity in
More informationChapter 10 Lecture Outline. The Restless Oceans
Chapter 10 Lecture Outline The Restless Oceans Focus Question 10.1 How does the Coriolis effect influence ocean currents? The Ocean s Surface Circulation Ocean currents Masses of water that flow from one
More informationLecture 24. El Nino Southern Oscillation (ENSO) Part 1
Lecture 24 El Nino Southern Oscillation (ENSO) Part 1 The most dominant phenomenon in the interannual variation of the tropical oceanatmosphere system is the El Nino Southern Oscillation (ENSO) over the
More informationWind: Small-scale and Local Systems
Wind: Small-scale and Local Systems Scales of Atmospheric Motion Atmospheric motions/phenomena occur on many diverse spatial and temporal scales. Weather forecasters tend to focus on Mesoscale and synoptic
More informationSection 6. The Surface Circulation of the Ocean. What Do You See? Think About It. Investigate. Learning Outcomes
Chapter 5 Winds, Oceans, Weather, and Climate Section 6 The Surface Circulation of the Ocean What Do You See? Learning Outcomes In this section, you will Understand the general paths of surface ocean currents.
More informationThe influence of synoptic scale flow on sea breeze induced surface winds and calm zones
PUBLISHED BY THE INTERNATIONAL METEOROLOGICAL INSTITUTE IN STOCKHOLM SERIES A DYNAMIC METEOROLOGY AND OCEANOGRAPHY Tellus (2010), 62A, 209 217 Printed in Singapore. All rights reserved C 2009 The Authors
More information10.6 The Dynamics of Drainage Flows Developed on a Low Angle Slope in a Large Valley Sharon Zhong 1 and C. David Whiteman 2
10.6 The Dynamics of Drainage Flows Developed on a Low Angle Slope in a Large Valley Sharon Zhong 1 and C. David Whiteman 2 1Department of Geosciences, University of Houston, Houston, TX 2Pacific Northwest
More informationATOMOSPERIC PRESSURE, WIND & CIRCULATION
ATOMOSPERIC PRESSURE, WIND & CIRCULATION A. INTRODUCTION Important because: pressure patterns drive wind patterns which in turn drive oceanic circulation patterns o atmospheric & oceanic circulation: major
More informationCurrents measurements in the coast of Montevideo, Uruguay
Currents measurements in the coast of Montevideo, Uruguay M. Fossati, D. Bellón, E. Lorenzo & I. Piedra-Cueva Fluid Mechanics and Environmental Engineering Institute (IMFIA), School of Engineering, Research
More informationSURFACE CURRENTS AND TIDES
NAME SURFACE CURRENTS AND TIDES I. Origin of surface currents Surface currents arise due to the interaction of the prevailing wis a the ocean surface. Hence the surface wi pattern (Figure 1) plays a key
More informationAT350 EXAM #2 November 18, 2003
AT350 EXAM #2 November 18, 2003 Name and ID: Enter your name and student ID number on the answer sheet and on this exam. Record your answers to the 50 questions by using a No. 2 pencil to completely fill
More information8.4 COASTAL WIND ANOMALIES AND THEIR IMPACT ON SURFACE FLUXES AND PROCESSES OVER THE EASTERN PACIFIC DURING SUMMER
8.4 COASTAL WIND ANOMALIES AND THEIR IMPACT ON SURFACE FLUXES AND PROCESSES OVER THE EASTERN PACIFIC DURING SUMMER Ragoth Sundararajan * and Darko Koraĉin Desert Research Institute, Reno, NV, USA Michael
More informationCharacterization of Boundary-Layer Meteorology During DISCOVER-AQ
Characterization of Boundary-Layer Meteorology During DISCOVER-AQ Daniel M. Alrick and Clinton P. MacDonald Sonoma Technology, Inc. Gary A. Morris St. Edward s University for Texas Air Quality Research
More informationLecture Outlines PowerPoint. Chapter 18 Earth Science 11e Tarbuck/Lutgens
Lecture Outlines PowerPoint Chapter 18 Earth Science 11e Tarbuck/Lutgens 2006 Pearson Prentice Hall This work is protected by United States copyright laws and is provided solely for the use of instructors
More informationATMOSPHERIC CIRCULATION. WIND = The horizontal movement of air. Results from the differences in air pressure. Always moves from HIGH to LOW.
ATMOSPHERIC CIRCULATION WIND = The horizontal movement of air. Results from the differences in air pressure. Always moves from HIGH to LOW. Pressure differences result from variations in temperature. AIR
More informationLesson: Ocean Circulation
Lesson: Ocean Circulation By Keith Meldahl Corresponding to Chapter 9: Ocean Circulation As this figure shows, there is a connection between the prevailing easterly and westerly winds (discussed in Chapter
More informationLecture 14. Heat lows and the TCZ
Lecture 14 Heat lows and the TCZ ITCZ/TCZ and heat lows While the ITCZ/TCZ is associated with a trough at low levels, it must be noted that a low pressure at the surface and cyclonic vorticity at 850 hpa
More informationConditions for Offshore Wind Energy Use
Carl von Ossietzky Universität Oldenburg Institute of Physics Energy Meteorology Group Detlev Heinemann Conditions for Offshore Wind Energy Use Detlev Heinemann ForWind Carl von Ossietzky Universität Oldenburg
More informationMeteorology. Circle the letter that corresponds to the correct answer
Chapter 6 Worksheet 2 Meteorology Name: Circle the letter that corresponds to the correct answer 1) A steep pressure gradient: a. produces light winds. b. produces strong winds. c. is only possible in
More informationChapter 13 Lecture Outline. The Atmosphere in Motion
Chapter 13 Lecture Outline The Atmosphere in Motion Understanding Air Pressure Air pressure is the force exerted by weight of air above Weight of the air at sea level 14.7 psi or 1 kg/cm 2 Decreases with
More informationWednesday, September 27, 2017 Test Monday, about half-way through grading. No D2L Assessment this week, watch for one next week
Wednesday, September 27, 2017 Test Monday, about half-way through grading No D2L Assessment this week, watch for one next week Homework 3 Climate Variability (due Monday, October 9) Quick comment on Coriolis
More informationSmall- and large-scale circulation
The Earth System - Atmosphere II Small- and large-scale circulation Atmospheric Circulation 1. Global atmospheric circulation can be thought of as a series of deep rivers that encircle the planet. 2. Imbedded
More informationOcean Currents that Redistribute Heat Globally
Ocean Currents that Redistribute Heat Globally Ocean Circulation Ocean Currents Fig. CO7 OCEAN CURRENTS Surface ocean currents are similar to wind patterns: 1. Driven by Coriolis forces 2. Driven by winds
More informationReview for the second quarter. Mechanisms for cloud formation
Review for the second quarter Mechanisms for cloud formation 1 Rising air expands and cools; Sinking air compresses and warms. (18) (24) Dry adiabatic lapse rate (10 o C/km): the rate of temperature decrease
More information1.5 THE LAND BREEZE CHARACTERISTICS IN ISRAEL DURING THE SUMMER BY THE MM5 MODEL
1. THE LAND BREEZE CHARACTERISTICS IN ISRAEL DURING THE SUMMER BY THE MM MODEL S. Berkovic and Y. Feliks Department of Mathematics, Israel Institute for Biological Research P.O.B 19, Ness-Ziona, Israel
More information9/25/2014. Scales of Atmospheric Motion. Scales of Atmospheric Motion. Chapter 7: Circulation of the Atmosphere
Chapter 7: Circulation of the Atmosphere The Atmosphere: An Introduction to Meteorology, 12 th Lutgens Tarbuck Lectures by: Heather Gallacher, Cleveland State University Scales of Atmospheric Motion Small-
More informationChapter 10: Global Wind Systems
Chapter 10: Global Wind Systems Three-cell model of atmospheric circulation Intertropical Convergence Zone (ITCZ) Typical surface wind patterns Upper-level pressure and winds Climatological sea-level pressure
More informationTopic 4 Temperature, Atmospheric Circulation and Climate. Temperature Concepts and Measurement 10/2/2017. Thermometer and Instrument Shelter
Topic 4 Temperature, Atmospheric Circulation and Climate Temperature Controls Global Temp. Patterns Atmospheric Circulation Primary High and Low Pressure Areas Global Circulation Model Local Winds Ocean
More informationThe dryline is a mesoscale phenomena whose development and evaluation is strongly linked to the PBL.
2.2. Development and Evolution of Drylines The dryline is a mesoscale phenomena whose development and evaluation is strongly linked to the PBL. Text books containing sections on dryline: The Dry Line.
More informationSUPPLEMENTARY INFORMATION
doi: 1.138/nature877 Background The main sis of this paper is that topography produces a strong South Asian summer monsoon primarily by insulating warm and moist air over India from cold and dry extratropics.
More informationEEm F/6 4/2 FEB 82 8 MAKJANIC UNCLASSIF I OFT DIDRSTI6NIB NL
AD-Alll 953 FOREIGN TECHNOLOGY DIV WRIGHT-PATTERSON AFS OH THE ALTERNATING EFFECT OF SEA BREEZE AND BORA.Ctfl F/6 4/2 FEB 82 8 MAKJANIC UNCLASSIF I OFT DIDRSTI6NIB NL EEm , 1~IIi~~1 111., 11111L,25 ~ iiii.
More informationScales of Atmospheric Motion Scale Length Scale (m) Time Scale (sec) Systems/Importance Molecular (neglected)
Supplement Wind, Fetch and Waves Scales of Atmospheric Motion Scale Length Scale (m) Time Scale (sec) Systems/Importance Molecular 10-7 - 10-2 10-1 (neglected) Coriolis not important Turbulent 10-2 10
More informationSummary of Lecture 10, 04 March 2008 Introduce the Hadley circulation and examine global weather patterns. Discuss jet stream dynamics jet streams
Summary of Lecture 10, 04 March 2008 Introduce the Hadley circulation and examine global weather patterns. Discuss jet stream dynamics jet streams arise because the Coriolis force prevents Hadley-type
More informationClimatology of the 10-m wind along the west coast of South American from 30 years of high-resolution reanalysis
Climatology of the 10-m wind along the west coast of South American from 30 years of high-resolution reanalysis David A. Rahn and René D. Garreaud Departamento de Geofísica, Facultad de Ciencias Físicas
More informationFoundations of Earth Science, 6e Lutgens, Tarbuck, & Tasa
Foundations of Earth Science, 6e Lutgens, Tarbuck, & Tasa The Atmosphere in Motion Foundations, 6e - Chapter 13 Stan Hatfield Southwestern Illinois College Atmospheric pressure Force exerted by the weight
More informationAtmospheric Circulation
Atmospheric Circulation Why do we say Earth's temperature is moderate? It may not look like it, but various processes work to moderate Earth's temperature across the latitudes. Atmospheric circulation
More informationLocal Winds. Please read Ahrens Chapter 10
Local Winds Please read Ahrens Chapter 10 Scales of Motion Microscale: meters Turbulent eddies Formed by mechanical disturbance or convection Lifetimes of minutes Mesoscale: km s to 100 s of km s Local
More informationThe atmospheric circulation system
The atmospheric circulation system Key questions Why does the air move? Are the movements of the winds random across the surface of the Earth, or do they follow regular patterns? What implications do these
More informationAtmospheric & Ocean Circulation-
Atmospheric & Ocean Circulation- Overview: Atmosphere & Climate Atmospheric layers Heating at different latitudes Atmospheric convection cells (Hadley, Ferrel, Polar) Coriolis Force Generation of winds
More informationLecture Outlines PowerPoint. Chapter 15 Earth Science, 12e Tarbuck/Lutgens
Lecture Outlines PowerPoint Chapter 15 Earth Science, 12e Tarbuck/Lutgens 2009 Pearson Prentice Hall This work is protected by United States copyright laws and is provided solely for the use of instructors
More informationMETEOROLOGICAL POTENTIAL FOR AIR POLLUTANT DISPERSION IN URBAN AND RURAL AREAS ALONG THE EAST COAST OF TAMILNADU
Sankaran. S et al. / International ournal of Engineering Science and Technology (IEST) ETEOROLOGICL POTENTIL FOR IR POLLUTNT DISPERSION IN URBN ND RURL RES LONG THE EST COST OF TILNDU SNKRN. S, ssistant
More informationChapter 7 Weather and Climate
Chapter 7 Weather and Climate *Describe what weather is, what affects it, and where it occurs. *Explain the connection between air pressure and wind. * *Many factors affect a region s weather. * *atmosphere
More informationInfluence of Heat Transport by Sea Breezes on Inland Temperature in the Osaka Area
Academic Article Journal of Heat Island Institute International Vol. 9-2 (2) Influence of Heat Transport by Sea Breezes on Inland Temperature in the Osaka Area Atsumasa Yoshida* Junichi Yashiro* Xinbo
More informationImpact of Sea Breeze Fronts on Urban Heat Island & Air Quality in Texas
Impact of Sea Breeze Fronts on Urban Heat Island & Air Quality in Texas Xiao-Ming Hu Center for Analysis and Prediction of Storms, School of Meteorology University of Oklahoma July 14, 2015 at LanZhou
More informationATMOSPHERIC CIRCULATION
Name ATMOSPHERIC CIRCULATION (adapted from Dr. S. Postawko, U. of Ok.) INTRODUCTION Why does the wind blow? Why do weather systems in the mid-latitudes typically move from west to east? Now that we've
More information+ R. gr T. This equation is solved by the quadratic formula, the solution, as shown in the Holton text notes given as part of the class lecture notes:
Homework #4 Key: Physical explanations 1.The way water drains down a sink, counterclockwise or clockwise, is independent of which hemisphere you are in. A draining sink is an example of vortex in cyclostrophic
More informationWind is caused by differences in air pressure created by changes in temperature and water vapor content.
Topic 8: Weather Notes, Continued Workbook Chapter 8 Wind is caused by differences in air pressure created by changes in temperature and water vapor content. Wind blows from high pressure areas to low
More informationAbstract. 1 Introduction
On the atmospheric stability in the Athens Basin M. Petrakis,* P. Kassomenos,* S. Lykoudis,* V. Synodinou^ "National Observatory ofathens, Institute of Meteorology and Physics of the Atmospheric Environment,
More informationChapter 8 Air Masses
Chapter 8 Air Masses Air Masses - 1 1. An Air Mass is a large body of air usually about 1500 km across and several km thick, that has homogeneous physical properties. 2. The important physical properties
More informationTHE ATMOSPHERE. WEATHER and CLIMATE. The Atmosphere 10/12/2018 R E M I N D E R S. PART II: People and their. weather. climate?
R E M I N D E R S Two required essays are due by Oct. 30, 2018. (A third may be used for extra credit in place of a Think Geographically essay.) ESSAY TOPICS (choose any two): Contributions of a noted
More informationLaura Landry*, Duc Nguyen, and Michael Woodman Maryland Department of the Environment, Baltimore, MD
THE INFLUENCE OF THE CHESAPEAKE BAY BREEZE ON MARYLAND AIR QUALITY Laura Landry*, Duc Nguyen, and Michael Woodman Maryland Department of the Environment, Baltimore, MD 1. INTRODUCTION On March 1,, the
More informationThe student will be expected to demonstrate an understanding of the cause of winds and how winds affect climate.
The student will be expected to demonstrate an understanding of the cause of winds and how winds affect climate. In this lesson you will: 2.3.1 Define the term prevailing winds. (k) 2.3.3 State the impact
More informationSIO20 - Midterm Examination 2 v1 Winter Section A. Circle the letter corresponding to the best answer. (1 point each)
NAME: Section A. Circle the letter corresponding to the best answer. (1 point each) 1. Rainbows result from: a. refraction and reflection of sunlight by water droplets b. reflection of sunlight by oceans
More informationChapter 2. Turbulence and the Planetary Boundary Layer
Chapter 2. Turbulence and the Planetary Boundary Layer In the chapter we will first have a qualitative overview of the PBL then learn the concept of Reynolds averaging and derive the Reynolds averaged
More informationA Comparison of the UK Offshore Wind Resource from the Marine Data Exchange. P. Argyle, S. J. Watson CREST, Loughborough University, UK
A Comparison of the UK Offshore Wind Resource from the Marine Data Exchange P. Argyle, S. J. Watson CREST, Loughborough University, UK Introduction Offshore wind measurements are scarce and expensive,
More informationMET 200 Lecture 11 Local Winds. Last Lecture: Forces. Review of Forces. Balance of Forces
MET 200 Lecture 11 Local Winds Last Lecture: Forces Scales of Motion Eddies Sea Breeze Mountain-Valley Circulations Chinook - Snow Eater Drainage Wind - Katabatic Wind 1 2 Review of Forces 1. Pressure
More informationATMS 310 Tropical Dynamics
ATMS 310 Tropical Dynamics Introduction Throughout the semester we have focused on mid-latitude dynamics. This is not to say that the dynamics of other parts of the world, such as the tropics, are any
More informationName Date L.O: SWBAT explain what breezes, planetary winds, ocean currents & monsoons are.
Name Date L.O: SWBAT explain what breezes, planetary winds, ocean currents & monsoons are. 1. A cool breeze is blowing toward the land from the ocean on a warm, cloudless summer day. This condition is
More informationMesoscale Meteorology
Mesoscale Meteorology METR 4433 Spring 2015 3.4 Drylines The dryline is a mesoscale phenomena whose development and evaluation is strongly linked to the PBL. In this section, we will consider its general
More informationIdealized WRF model sensitivity simulations of sea breeze types and their effects on offshore windfields: Supplementary material
Idealized WRF model sensitivity simulations of sea breeze types and their effects on offshore windfields: Supplementary material Authors: C. J. Steele, S. R. Dorling, R. von Glasow and J. Bacon Synoptic
More informationAtmospheric & Ocean Circulation- I
Atmospheric & Ocean Circulation- I First: need to understand basic Earth s Energy Balance 1) Incoming radiation 2) Albedo (reflectivity) 3) Blackbody Radiation Atm/ Ocean movement ultimately derives from
More informationCHAPTER 8 WIND AND WEATHER MULTIPLE CHOICE QUESTIONS
CHAPTER 8 WIND AND WEATHER MULTIPLE CHOICE QUESTIONS 1. is the movement of air measured relative to the Earth's surface. a. Gravity b. The pressure gradient force c. The Coriolis Effect d. The centripetal
More informationAtmosphere & Weather. Earth Science
Atmosphere & Weather Earth Science Energy Transfer in the Atmosphere Earth s energy is provided by the SUN! Energy is important to us because it 1. Drives winds and ocean currents. 2. Allows plants to
More informationCHANGE OF THE BRIGHTNESS TEMPERATURE IN THE MICROWAVE REGION DUE TO THE RELATIVE WIND DIRECTION
JP4.12 CHANGE OF THE BRIGHTNESS TEMPERATURE IN THE MICROWAVE REGION DUE TO THE RELATIVE WIND DIRECTION Masanori Konda* Department of Geophysics, Graduate School of Science, Kyoto University, Japan Akira
More informationWind in the Atmosphere
Lesson 2 Wind in the Atmosphere ESSENTIAL QUESTION What is wind? By the end of this lesson, you should be able to explain how energy provided by the sun causes atmospheric movement, called wind. p 6.ESS2.2,
More informationAtmospheric Circulation (Ch. 8) Ocean & Atmosphere are intertwined Gases & waters freely exchanged Wind Weather Climate
Atmospheric Circulation (Ch. 8) Ocean & Atmosphere are intertwined Gases & waters freely exchanged Wind Weather Climate Atmospheric Structure Consists of Layers Separated by Temperature Stratosphere: Temperature
More informationSESSION THREE: FACTORS THAT INFLUENCE WEATHER IN SOUTH AFRICA
SESSION THREE: FACTORS THAT INFLUENCE WEATHER IN SOUTH AFRICA KEY CONCEPTS: In this section we will focus on the following aspects: Factors determining the weather of South Africa Influence of the oceans
More informationFrequency of lake breeze at Lake Taihu
耶鲁大学 - 南京信息工程大学大气环境中心 Yale-NUIST Center on Atmospheric Environment Frequency of lake breeze at Lake Taihu Reporter:Qin hairun 2013-7-12 1 uoutline Literature Reading Recent Work Discussion and suppose
More informationAtmospheric Waves James Cayer, Wesley Rondinelli, Kayla Schuster. Abstract
Atmospheric Waves James Cayer, Wesley Rondinelli, Kayla Schuster Abstract It is important for meteorologists to have an understanding of the synoptic scale waves that propagate thorough the atmosphere
More information3 Global Winds and Local Winds
CHAPTER 15 3 Global Winds and Local Winds SECTION The Atmosphere BEFORE YOU READ After you read this section, you should be able to answer these questions: What causes wind? What is the Coriolis effect?
More informationChapter 22, Section 1 - Ocean Currents. Section Objectives
Chapter 22, Section 1 - Ocean Currents Section Objectives Intro Surface Currents Factors Affecting Ocean Currents Global Wind Belts (you should draw and label a diagram of the global wind belts) The Coriolis
More informationShorelines Earth - Chapter 20 Stan Hatfield Southwestern Illinois College
Shorelines Earth - Chapter 20 Stan Hatfield Southwestern Illinois College The Shoreline A Dynamic Interface The shoreline is a dynamic interface (common boundary) among air, land, and the ocean. The shoreline
More informationSailing the Seas: Wind Driven Ocean Circulation Ocean Gyres
Sailing the Seas: Wind Driven Ocean Circulation Ocean Gyres Ocean Currents What Happens at the Coast? Readings: Ch 9: 9.2-9.6, 9.8-9.13 Graphic: America's Cup sailboat race off Newport, Rhode Island. J.
More informationVertical Motion and Atmospheric Stability
Lesson 4 Vertical Motion and Atmospheric Stability This lesson describes the vertical structure of the atmosphere, atmospheric stability and the corresponding vertical motion. Adiabatic diagrams are introduced
More informationA Theoretical Consideration For Sea Breeze Circulation In Peninsular India
A Theoretical Consideration For Sea Breeze Circulation In Peninsular India V.LakshmanaRao 1, P.Satish 2 Assistant Professor(c), Department of Meteorology & Oceanography, Andhra University, Visakhapatnam,
More informationMeteorology. Circle the letter that corresponds to the correct answer
Chapter 7 Worksheet 2 Meteorology Name: Circle the letter that corresponds to the correct answer 1) Which of the following factors contributes to the general subsidence in the latitude zone 20 degrees
More informationApplied Earth Science Climate Exam Practice Questions Page 1
Name: 1. Which combination of climate factors generally results in the coldest temperatures? A) low elevation and low latitude B) low elevation and high latitude C) high elevation and low latitude D) high
More information3/6/2001 Fig. 6-1, p.142
First GOES 11 image http://visible earth.nasa.g ov/view_rec. php?id=190 Air-born dust from the Sahara Desert, Feb. 2001 Fig. 6-CO, p.140 dust from China over Japan. 3/5/2001 FIGURE 6.1 A model of the atmosphere
More informationPrevailing Winds. The Coriolis Effect
Prevailing Winds 1. Wind: a movement of air in the atmosphere. Bill Nye wind (2 minutes) 2. Local or regional wind: occur in fairly small areas. 3. Prevailing winds: Major wind pattern that affect large
More informationUnderstanding Weather
Understanding Weather Images Graphic of the atmosphere. Enlarge Cirrus clouds. Enlarge Air masses Air masses are parcels of air that bring distinctive weather features to the country. An air mass is a
More information