Boundary-Layer Meteorol (2018) 169:151–161 https://doi.org/10.1007/s10546-018-0361-7 NOTES AND COMMENTS 1 1 2 David Melecio-Vázquez · Prathap Ramamurthy · Mark Arend · Jorge E. González-Cruz Received: 26 May 2017 / Accepted: 14 May 2018 / Published online: 31 May 2018 © The Author(s) 2018 Abstract We use various temperature proﬁlers located in and around New York City to observe the structure and evolution of the thermal boundary layer. The primary focus is to highlight the spatial variability of potential-temperature proﬁles due to heterogeneous surface forcing in an urban environment during different ﬂow conditions. Overall, the observations during the summer period reveal the presence of thermal internal boundary layers due to the interaction between the marine atmospheric boundary layer and the convective urban environment. The summer daytime potential-temperature proﬁles within the city indicate a superadiabatic layer is present near the surface beneath a mildly stable layer. Large spatial variability in the near-surface (0–300 m) potential temperature is detected, with the thermal proﬁle in the lower atmosphere uniquely determined by the underlying surface forcing and the distance from the coast. The summer and winter average night-time potential-temperature proﬁles show that the atmosphere is still convective near the surface. The seasonal averages of mixing ratio show large variability in the vertical direction. Keywords Coastal boundary layer · Microwave radiometer · Moisture boundary layer · Thermal boundary layer · Urban boundary layer 1 Introduction Key knowledge gaps exist in our understanding of boundary-layer processes over coastal cities where the population is projected to increase in the coming years (United Nations 2015). The climatology of coastal cities is simultaneously inﬂuenced by the additional convection resulting from anthropogenic activities and sea-breeze incursion, leading to an uncertain B David Melecio-Vázquez email@example.com Department of Mechanical Engineering and NOAA-CREST Center, City College of New York, New York, NY 10031, USA Department of Electrical Engineering and NOAA CREST Center, City College of NewYork, New York, NY 10031, USA 123 152 D. Melecio-Vázquez et al. thermal environment because of the high vulnerability to extreme temperatures. However, the lack of adequate observations at appropriate spatial and temporal scales inhibits our ability to produce accurate boundary-layer forecasts in urban environments, which is important for emergency-responses purposes (National Research Council 2012). Over the last 30 years, many observational and numerical experiments have been con- ducted with which to study the urban boundary layer. Problems related to air pollution (Molina and Molina 2004) and the threat of terrorism (Batchvarova and Gryning 2006)have led to many dispersion studies in Europe and the USA. The Joint Urban 2003 ﬁeld campaign in Oklahoma City and the BUBBLE (Basel Urban Boundary-Layer Experiment) campaign in Switzerland are examples of large-scale, urban-dispersion campaigns capturing the urban–ru- ral differences in boundary-layer structure (Rotach et al. 2005). The data from these studies have been helpful in improving the representation of urban-scale processes in numerical weather prediction (Salamanca and Martilli 2010) and air-pollution models (Batchvarova and Gryning 2006; Franzese and Huq 2011). However, their applicability in coastal–urban environments is questionable. While very few experiments have been conducted to inves- tigate coastal–urban interactions, Mestayer et al. (2005) have observed the variation of the boundary-layer height during sea-breeze events in Marseille during the ESCOMPTE cam- paign, noting that the sea breeze tends to weaken boundary-layer development (Lemonsu et al. 2006) despite the increasing insolation as the day progresses into the afternoon; a similar behaviour was also found by De Tomasi et al. (2011) in Lecce, Italy. We do not refer to these experiments to provide an exhaustive list of urban boundary-layer studies, but to emphasize the fact that very few observations exist on the thermal characteristics of the urban boundary layer (Barlow 2014). Further, most experiments focus on the urban surface layer, whereas we seek to investigate the structure of the urban boundary layer here by extending observations to the entrainment zone (typically 2–3 km above ground level). While relatively few surface parameters are required to estimate the vertical structure of the boundary layer over homogeneous terrain, the high degree of surface heterogeneity and the inﬂuence of the sea breeze in coastal–urban zones require knowledge of the ﬂow history (De Tomasi et al. 2011). In New York City, observations of urban heat islands and cool islands (Gafﬁn et al. 2008; Meir et al. 2013) cannot be solely explained using surface characteristics. Based on helicopter transects in the 1960s, Bornstein (1968) revealed that neighbourhoods closer to the coast experience rural-like surface inversions. Here, we inves- tigate the variability of the urban boundary layer in New York City using vertical proﬁles from three local airports, and proﬁles derived from a microwave radiometer within the urban centre to investigate the seasonal variabilities in the thermal and moisture boundary-layer structure. Microwave radiometers have the advantage of being robust instruments (Xu et al. 2015), with a recent, extensive study judging them to be very good at estimating temperature proﬁles, particularly in the lower boundary layer (Lundquist et al. 2017). While microwave- radiometer observations have been used to determine the mixed-layer height (Cimini et al. 2013), the vertical extent of the urban heat island (Khaikine et al. 2006), and for estimating stability conditions for wind-energy applications (Friedrich et al. 2012), our main objectives here are to analyze the spatial variability in the thermal structure of the boundary layer over the highly dense area of New York City, and to quantify the diurnal and seasonal variabilities of the urban thermal and moisture proﬁles. 123 Thermal Structure of a Coastal–Urban Boundary Layer 153 2 Measurements and Data Analysis A Radiometrics proﬁling radiometer, model MP-3000A (Radiometrics, Boulder, Colorado, USA), is located on the roof of the engineering building at the City College of New York (CCNY) (40.821519°N, 73.948184°W; 65 m above sea level), and is part of the New York City Meteorological Network (NYCMetNet) (National Research Council 2012, 54). This microwave radiometer is a passive instrument that records vertical proﬁles of temperature, relative humidity, water vapour and liquid water density. Proﬁles are produced from brightness temperatures measured in several bands centred at different frequencies, with temperature from the 60-GHz-centred feature, water vapour from the 22-GHz feature, and liquid–wa- ter proﬁles from a combination of scans in the 22- to 30-GHz and 51- to 59-GHz bands. The brightness temperatures are then converted to vertical proﬁles of the above-mentioned variables using a neural-network algorithm based on radiosonde-derived observations. The neural-network output contains 58 levels with varying vertical spacing: 0 to 500 m in 50-m steps, 600 to 2000 m in 100-m steps, and 2,250 m to 10,000 m in 250-m steps. At every level, the potential temperature is calculated using 0.286 θ T ( p / p) , (1) where T is the temperature measured by the microwave radiometer in K, p is the reference pressure of 1013 hPa, and p is the pressure derived from the heights of a standard atmosphere (Wallace and Hobbs 2006). The pressure information is then used to estimate the mixing ratio at each level using (Stull 1988) 17.27 (T − 273.16) e 0.611exp , (2) sat T − 35.86 sat r 0.622 , (3) sat P − e sat and RH r r , (4) v sat where e is the saturation water-vapour pressure in kPa, r is the saturation water-vapour sat sat mixing ratio, r is the water-vapour mixing ratio that is used as the absolute measure of moisture for the atmosphere, and is calculated from the relative humidity, RH, as measured by the microwave radiometer. The microwave-radiometer proﬁles are compared with the American Meteorological Data Reports (AMDAR), which have been aggregated from several airlines to form records of varying temporal and spatial resolution. The root-mean-square error was reported to be around 0.72 K for the 900–800 hPa levels in the boundary layer (Benjamin et al. 1999). The boundary-layer proﬁles are from the John F. Kennedy International Airport (JFK; 40.6413°N, 73.7781°W) located on the Atlantic Coast, LaGuardia Airport (LGA; 40.7769°N, 73.8740°W) located 23 km west of the Atlantic Coast, and Newark Liberty International Air- port (EWR; 40.6895°N, 74.1745°W). It is important to point out that the AMDAR altitude values are derived from a pressure altitude based on a standard atmosphere. To calculate the true height of the measurement, the method outlined in Rahn and Mitchell (2016)isemployed using publicly available observations from the Automatic Surface Observing Systems net- work for the surface conditions at each site. Figure 1 shows a map of the region being analyzed. According to Stewart and Oke (2012), the airport locations (LGA, JFK, and EWR sites) can be categorized as a Local Climate Zone 8, 123 154 D. Melecio-Vázquez et al. and the CCNY site as a Local Climate Zone 1, which is mostly high-rise residential buildings with an average height of 25–65 m. Additional information on the land-use categories for New York City can be found in Gutiérrez et al. (2015a), where high-resolution, land-cover information was used for mapping the urban morphology (e.g., the building height and land- use category according to Fry et al. 2011). The land-use characteristics around each airport are as follows: around the JFK site are low-rise residential units, around the LGA site are high-rise residential and commercial units, while the EWR site is surrounded by a commercial district, with average building heights adjacent to each airport of 8.5–10, 15–25, and 8–10 m, respectively. The spatial variability of the urban boundary layer is investigated for selected dates during the month of July 2016 using observations from the microwave radiometer and AMDAR records. As the timestamps for the microwave radiometer and AMDAR records are not concurrent, these data were matched within ± 14 min and 59 s (to avoid duplicate records) between 0000 LST (local standard time) on 1 July 2016 to 2330 LST on 31 July 2016, in 30-min intervals. This process resulted in approximately 300 dates on which the microwave radiometer and AMDAR records occurred within a 30-min window. The dates were further narrowed to select cloudless days over all four locations, which resulted in the selection of different dates for each time-of-day, since no data were available spanning an entire day from all four sites. The timestamps in Fig. 1 do not correspond to the exact time of the observation, but represent the closest matched time. The dates chosen are during the extreme-heat episodes investigated in more detail in Ramamurthy et al. (2017a). Additionally, the potential-temperature (θ) gradient at each location was calculated by performing a linear regression on the θ data available in each layer. The slope of the linear regression equation was then recorded as the potential-temperature gradient, dθ/dz. Wind-speed proﬁles are available only for the AMDAR locations, since no wind-speed data are available at the CCNY location. For the averaged proﬁle analysis, only data from the microwave radiometer were used. Clear-sky observations from June to August 2015 were used to compute summer averages, with clear-sky observations from December 2014 to February 2015 used to calculate winter averages. The data were separated into bins for different time periods, and then again for every microwave-radiometer measurement height; the daytime and night-time hours for each season correspond to 1000–1600 LST (1400–2000 UTC) and 2200–0400 LST (0200–0800 UTC), respectively. 3 Results and Discussion 3.1 Spatial Variability Figure 1 shows the spatial variability of the boundary layer over New York City by compar- ing the temperature (microwave radiometer and AMDAR) and wind-speed (AMDAR only) proﬁles, including the ground track of the ﬂights used. As mentioned earlier, the altitudes were corrected to enable the direct comparison: AMDAR records were corrected with data obtained from surface stations and the hypsometric equation, while microwave-radiometer data were adjusted to account for the height of the instrument above sea level. Figure 1acom- pares the microwave-radiometer observations with AMDAR proﬁles, while Fig. 1b, c shows the wind-speed and wind-direction proﬁles, respectively, from the AMDAR locations only. Each column of Fig. 1 shows a typical transition of the boundary layer over the coastal–urban environment in New York City, and highlights the spatial variability within such a densely 123 Thermal Structure of a Coastal–Urban Boundary Layer 155 Fig. 1 Proﬁles of a potential temperature, b wind speed and c wind direction from different locations across New York City. Each column corresponds to a different hour of the day. The 0530 LST timestamp corresponds to near-sunrise proﬁles (sunrise is at 0538 LST) on 16 July 2016. The 1430 LST data represent the early afternoon on 16 July 2016. The 1800 LST data represent the late afternoon on 24 July 2016, with sunset at 2019 LST. The maps show the ground track of the ﬂights used. The following wind-speed proﬁles in b and c have a missing value at the ﬁrst level: the JFK and EWR sites at 0530, the JFK site at 1430, and the JFK and EWR sites at 1800 populated coastal–urban environment. Each location has a different footprint that affects the development of the boundary-layer proﬁles. The proﬁles at the JFK site (coastal site, Fig. 1a) are usually inﬂuenced by onshore ﬂow advecting cooler (with the exception of Fig. 1a—0530 LST showing the ﬂow from the east), saturated airmasses over the city during the warm sea- son (Gedzelman et al. 2003; Bailey and Freedman 2008). The EWR site is located inland, with potential-temperature proﬁles resembling those over homogeneous terrain, especially during the convective period around 1430 LST as shown in Fig. 1a. Potential-temperature 123 156 D. Melecio-Vázquez et al. gradients for these proﬁles were calculated for the levels 0–300 m to contrast the stability at each location. In the early morning hours before sunrise, the atmosphere is stable over all airport loca- tions, and weakly stable over the CCNY site. The wind direction during this period is from −1 the north (from land), and wind speeds < 5 m s are visible in the near-surface region. The θ gradient values below the 300-m level show very stable to weakly-stable layers for each location. The EWR and LGA locations are upstream of the change in surface roughness and, −1 thus, show a more stable layer with values of 11. and 11.4 K km , respectively for the gradient. Downstream, less stable layers can be seen at the CCNY and JFK locations, with −1 gradients of 6.6 and 3.5 K km , respectively, since roughness elements may be generating turbulence, resulting in a near-adiabatic layer (as noted in Godowitch et al. 1985, 1987,and Day et al. 2010) extending from the surface up to 200 m at the CCNY site, and up to 375 m at the JFK site. Anthropogenic heat sources may also play a role in maintaining the weakly stable layers found at these locations. The transition to the daytime convective period (see Fig. 1—1430 LST column) reveals the spatial variation within the city. The thermal boundary layer (Fig. 1a) over the EWR site is well-mixed and with a typical structure of a convective boundary layer over land, while the wind speeds are low and from the east (from water). The θ proﬁle at the JFK site is consistent with a daytime marine boundary layer, since the ﬂow is from the south (from water). At the JFK location, the air temperature close to the surface is lower, with a θ gradient −1 −1 of 10.7 K km ; at the LGA site, the superadiabatic layer with a θ gradient of − 9.4 K km reaches up to 650–700 m. The boundary layer over the CCNY site has an interesting and unique structure. The −1 near-surface θ gradient is − 15.4 K km , which may have been additionally affected by the anthropogenic heat released from the dense urban environment. The superadiabatic region ends at around 250 m where an elevated mixed layer can be seen, which is consistent with the proﬁle at the JFK site. Although a more detailed analysis is required, the marine boundary layer may have generated a capping stable layer starting at around 375 m. Above 1000 m, the CCNY proﬁle is comparable to the LGA proﬁle, and both exhibit a well-mixed region. The stable region between 375 m and 1000 m may inhibit efﬁcient mixing within the boundary layer, which has implications for air-pollution applications, since most convective schemes over the city ignore the formation and development of thermal internal boundary layers independent of the near-surface ﬂuxes. While the coastal JFK site is inﬂuenced by the sea breeze during the afternoon periods, as seen by the southerly winds in Fig. 1b, the sea breeze is unable to penetrate inland to the LGA and CCNY sites, which are inﬂuenced by the northerly land breezes. The low wind speeds at the EWR site and the nearly-adiabatic temperature proﬁle show that the penetration of the sea breeze is insufﬁcient to perturb the thermal proﬁle from mean adiabatic conditions. Moving into the evening hours, (see Fig. 1, 1800 LST column), surface cooling resulted in a stable boundary layer at all locations, except at the CCNY site. At the JFK site, wind −1 speeds from the south ≈8ms (the highest near-surface wind speeds across all locations), −1 and the θ gradient is 26.9 K km . At the CCNY location, the stable layer from 250 to −1 −1 500 m undergoes a transition from 3.2 K km at 1430 LST to a larger 10.6 K km at 1800 LST. However, in the lower 250 m, a superadiabatic layer is visible with a θ gradient −1 of − 1.0 K km . All proﬁles begin to collapse into a similar thermal regime starting at around 750 m. The strong stable conditions present across most of the region on the edges of the urban environment suggest the persistence of temperatures resulting from anthropogenic heating within the urban environment throughout most of the night. 123 Thermal Structure of a Coastal–Urban Boundary Layer 157 Fig. 2 Transition of potential temperature at different hours on 6 July 2016. Sunrise was at 0530 LST, and sunset was at 2030 LST. Location: brown ﬁlled circle: CCNY, pink ﬁlled circle: LGA In summary, different mechanisms inﬂuence the development of the boundary layer in New York City. Internal boundary layers form downstream of discontinuities in surface characteristics (Garratt 1990), such as the geometry, temperature, humidity, and/or surface ﬂuxes. In the proﬁles from the CCNY site, there is evidence of internal boundary layers forming due to the surface roughness, as can be seen by the persistent proﬁles in the boundary layer, where a superadiabatic layer forms near the surface, which slowly undergoes transition into a sub-adiabatic region below the elevated mixed layer. During the convective conditions from midday into the evening, the EWR proﬁle shows increased temperatures compared with the coastal proﬁles at the JFK site, and is more com- parable to the proﬁles that occur inland. These differences are most apparent during the afternoon hours when the sea breeze plays a dominant role, as seen by the ﬂow from the south over the JFK site. Figure 2 shows the transition of the thermal boundary layer at the CCNY and LGA sites, with similar stability features in the early morning just after sunrise detected at both locations. As the day progresses, a superadiabatic layer persists throughout the day over the CCNY location, whereas the LGA proﬁles illustrate a transition from stable to convective, and back to stable conditions. The proﬁles at both locations indicate stable conditions at a height ≈ 750 m throughout the day. The superadiabatic region over the city may be the result of a combination of anthropogenic heating from below and the capping produced by the sea breeze above preventing the exchange of the higher temperature air with layers aloft. 3.2 Average Boundary-Layer Proﬁles The average nocturnal and diurnal θ proﬁles are presented here for both the winter and summer seasons based only on data from the microwave radiometer collected at the CCNY location, and divided into summer-day and summer-night, and winter-day and winter-night, categories averaged over 11,968, 11,009, 15,522, and 13,566 proﬁles, respectively. Figure 3 shows the average vertical proﬁle of daytime/night-time pairs of the potential temperature 123 158 D. Melecio-Vázquez et al. Fig. 3 Summer and winter proﬁles, a potential temperature, and b mixing ratio. Diurnal- and nocturnal- averaged proﬁles for each respective season are shown for clear-sky conditions only. Grey areas indicate the extent of one standard deviation and the mixing ratio for the summer and winter periods. The grey areas represent one standard deviation from the mean value of each averaged proﬁle. The mean difference between the summer and winter daytime proﬁles at each level amounts to 25.4 K for the potential temper- −1 ature and 7.8 g kg for the mixing ratio. The standard deviation of the daytime summer and winter potential temperature averaged for the entire column is 2.7 and 6.0 K, respectively, −1 with corresponding standard deviations of 1.6 and 1.2 g kg for the summer and winter daytime mixing ratios, respectively. Strong organized thermals during the summer daytime convective period may lead to a reduced overall randomness in the proﬁle, which can be seen by the lower range of the values for the summer daytime average relative to the winter daytime average in Fig. 3a. The winter θ proﬁles in Fig. 3a show a superadiabatic layer starting at the instrument level and extending upwards to about 125 and 250 m for the daytime and night-time proﬁles, −1 respectively. The θ gradients for the layer from 0 to 300 m are − 18.7 and − 22.8 K km for the summer and winter daytime proﬁles, respectively, with night-time gradients of 0.3 −1 and − 6.1 K km , respectively. In the layer 150–200 m, an elevated stable layer can be identiﬁed. While a stable layer at the surface is usually expected over urban areas, this layer is elevated due to anthropogenic heating and/or mechanical turbulence generated by the urban roughness elements. The daytime and night-time boundary-layer heights are around 350 and 900 m based on the parcel method (Seidel et al. 2010). Other cities in the USA have been reported to have a superadiabatic layer close to the surface at night in urban areas; in St. Louis, a mean inversion base height for the nocturnal boundary layer is estimated as 150 m above a nearly adiabatic region (Godowitch et al. 1985); and in Houston, Texas, a mean inversion base height of 203 m has been observed (Day et al. 2010). The presence of the superadiabatic layer may be explained by the larger heat-storage capacity of the urban environment, and through radiative cooling of the surface at night. Hence, elevated stable layers over urban areas are often seen during convective periods (Bornstein 1968; Godowitch et al. 1985). The summer proﬁles show convective and stable boundary layers for the day and night- time, respectively. The average daytime mixed-layer depth is estimated to be 2.75 km, with an average superadiabatic layer extending from the instrument level to a height of 350 m. The elevated stable layer results in θ ≈ 5 K based on the bottom of the stable layer near 400 m to the top of the stable layer near 1250 m. Just above this layer is a level of statically neutral air of 600-m thickness. The night-time proﬁle shows a stable layer from the instrument level until about 400 m where the θ proﬁle shows higher temperatures than the daytime proﬁle. 123 Thermal Structure of a Coastal–Urban Boundary Layer 159 To the authors’ knowledge, few observational studies have focused on the vertical structure of humidity, except as a proxy for inferring the boundary-layer height (Haman et al. 2012), or the structure has been estimated using high-resolution model data (Lemonsu et al. 2006; Huang et al. 2016). The observed daytime mixing-ratio proﬁle shown in Fig. 3bhas two maxima. Here, the land- and/or sea-breeze interactions may play a role: during a sea breeze, the advected moisture is located near the surface, but aloft during a land breeze. It is interesting to note that the stable layer in the daytime proﬁles coincides with an increase in the mixing ratio at the same level. The presence of moisture may inﬂuence the thermal environment by reducing the convective efﬁciency of plumes rising from the surface. The large variability during the winter periods can be attributed to the decoupling of the surface layer from the layers aloft (Markowski and Richardson 2010). The stable layer above may either be affected by a low-level jet, with increased shear above and below a wind-speed maximum, or to the inability of the stable boundary layer to reach a steady-state due to wake turbulence generated from the urban roughness (Stull 1988). 4 Conclusions Coastal boundary layers form as a direct response to the surface forcing and ﬂow history, with the effects of the former well established in the literature relative to the effects of the latter on boundary-layer development over urban areas. Here we investigate the structure of boundary-layer proﬁles of temperature and humidity over New York City. While local forcing overwhelmingly dominates the structure of the boundary layer during the daytime, a similar proﬁle structure can be seen at all locations during the night-time, especially above 400 m. One of the unique features evident in our results is the interaction between the highly convective urban surface layer and the marine boundary layer, leading to the development of an internal boundary layer. Unlike a traditional boundary layer observed over non-coastal and non-urban surfaces, we do not see a uniformly mixed layer, but rather a stable layer during clear, daytime conditions. While we present the mean thermal characteristics of the coastal–urban environment here, additional work is necessary to study the turbulent transport of heat, momentum and moisture within the coastal–urban boundary layer. Current numerical weather prediction models used in the study of the urban boundary layer (e.g., Leroyer et al. 2014; Gutiérrez et al. 2015b; Ortiz et al. 2016; Ramamurthy et al. 2017b) lack a realistic representation of urban–coastal inter- actions, since boundary-layer parametrizations are unable to reproduce the thermal internal boundary layers observed. More effort and sustained observations are necessary to improve the predictability of the thermal conditions in the coastal–urban environment. Acknowledgements This work was supported by the National Oceanic and Atmospheric Administration, Ofﬁce of Education Partnership Program award NA16SEC4810008, Department of Defense Army Research Ofﬁce, W911NF-15-1-0443 and by the U.S. Department of Education—Earth Science and Environmental Sustainability (ESES) Graduate Initiative, award P031M105066. Access to AMDAR data and Automatic Surface Observing Systems data was provided via the NOAA (National Oceanic and Atmospheric Admin- istration) Meteorological Assimilation Data Ingest System and has been authorized according to agreements made between the CCNY NOAA Center for Earth System Sciences & Remote Sensing Technologies, NOAA and NOAA’s partners in accordance with the Memorandum of Understandings that NOAA has made with its partners. The authors wish to thank the Brookhaven National Laboratory for their support in preparing this manuscript. The Brookhaven National Laboratory is supported by the U.S. Department of Energy Ofﬁce of Science. The opinions and conclusions herein are solely those of the authors and do not represent the 123 160 D. Melecio-Vázquez et al. views of the Department of Education, Department of Commerce, the National Oceanic and Atmospheric Administration, the Department of Energy, and the Brookhaven National Laboratory. 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Boundary-Layer Meteorology – Springer Journals
Published: May 31, 2018
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