Formulation of a tropical town energy budget (t-TEB) scheme

Karam, Hugo Abi; Filho, Augusto José Pereira; Masson, Valéry; Noilhan, J.; Filho, Edson Pereira Marques

doi:10.1007/s00704-009-0206-x

Cited by 26 publications

(20 citation statements)

References 55 publications

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“…This behavior is attributed to the sea-breeze intensification and thermal capability of vegetation in rural area. The numerical result obtained by [15] with urban and vegetation numerical SEB schemes has supported the observations of the UHI in the MARJ. Reference [23] also indicated that the UHI in the city of São Paulo has a predominant daytime character, with a maximu m intensity during afternoon.…”

Section: Introductionsupporting

confidence: 66%

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The Vertical Structure of Tropical Urban Heat Island with LES

Filho

Cassol²,

Karam³

et al. 2013

AJEE

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The Large-eddy simulation (LES) model is used to investigate the influence of the Tropical Urban Heat Island (UHI) in the vert ical structure of the Planetary Boundary Layer (PBL) under adiabatic and non-saturated conditions. An idealized UHI is represented by two-dimensional patches of heat fluxes at the surface defining variable Bowen rat io along the horizontal do main. The results indicated that the heterogeneities are able to induce the format ion of intense updraft over the center of warm patch. Th is buoyant thermal transports the mo isture fro m the lower to the upper part of the PBL and penetrate the entrainment zone. Consequently, the urban-breeze circulat ion can contribute to the clouds development at the top of the PBL over the UHI.

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Section: Introductionsupporting

confidence: 66%

“…Regard ing the modeling, urban SEB has received great attention [13][14][15][16]. The main difficu lty in coupling the SEB with mesoscale at mosph eric mo dels is th e fact that there are many parameters wh ich must be defined in order to optimize the nu merical simulations ( [17], [11]).…”

Section: Introductionmentioning

confidence: 99%

The Vertical Structure of Tropical Urban Heat Island with LES

Filho

Cassol²,

Karam³

et al. 2013

AJEE

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“…The main disadvantage of these expressions is that they can only be used on restricted situations (e.g., flat surfaces) and as demonstrated by Rotach (1993), Roth (2000), and Karam et al (2009) they are inappropriate to simulate the flow inside the urban canopy layer. Indeed, in urban areas, complex and heterogeneous obstacles (like buildings) exchange fluxes with all the atmosphere inside the canopy and not only with the ground level as specified in the boundary layer laws.…”

Section: Introductionmentioning

confidence: 99%

On the Coherence in the Boundary Layer: Development of a Canopy Interface Model

et al. 2017

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A 1D Canopy Interface Model (CIM) is developed to act as an interface between a meso-scale and a micro-scale atmospheric model and to better resolve the surface turbulent fluxes in the urban canopy layer. A new discretisation is proposed to solve the TKE equation finding solutions that remain fully concordant with the surface layer theories developed for neutral flows over flat surfaces. A correction is added in the buoyancy term of the TKE equation to improve consistency with the Monin-Obukhov surface layer theory. Obstacles of varying heights and dimensions are taken into account by introducing specific terms in the equations and by modifying the mixing length formulation in the canopy layer. The results produced by CIM are then compared with wind and TKE profiles simulated with a LES experiment and results obtained during the BUBBLE meteorological intensive observation campaign. It is shown that the CIM computations are in good agreement with the results simulated by the LES as well as the measurements from BUBBLE. The applicability of the correction term in an urban canopy layer and to further validate CIM in multiple stability conditions and various urban configurations is discussed.

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“…The main objective of this section is to find a simple method to estimate LW in clear-sky conditions in Sã o Paulo, which could be easily implemented in algorithms to evaluate the energy balance at the surface in urban areas (Arnfield and Grimmond 1998;Martilli et al 2002;Offerle et al 2003;Karam et al 2009). …”

Section: Estimating Lw For Clear-sky Conditions In Sã O Paulomentioning

confidence: 99%

Observational Characterization of the Downward Atmospheric Longwave Radiation at the Surface in the City of São Paulo

Barbaro

Oliveira

Soares

et al. 2010

Journal of Applied Meteorology and Climatology

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This work describes the seasonal and diurnal variations of downward longwave atmospheric irradiance (LW) at the surface in Sã o Paulo, Brazil, using 5-min-averaged values of LW, air temperature, relative humidity, and solar radiation observed continuously and simultaneously from 1997 to 2006 on a micrometeorological platform, located at the top of a 4-story building. An objective procedure, including 2-step filtering and dome emission effect correction, was used to evaluate the quality of the 9-yr-long LW dataset. The comparison between LW values observed and yielded by the Surface Radiation Budget project shows spatial and temporal agreement, indicating that monthly and annual average values of LW observed in one point of Sã o Paulo can be used as representative of the entire metropolitan region of Sã o Paulo. The maximum monthly averaged value of the LW is observed during summer (389 6 14 W m 22; January), and the minimum is observed during winter (332 6 12 W m 22 ; July). The effective emissivity follows the LW and shows a maximum in summer (0.907 6 0.032; January) and a minimum in winter (0.818 6 0.029; June). The mean cloud effect, identified objectively by comparing the monthly averaged values of the LW during clear-sky days and all-sky conditions, intensified the monthly average LW by about 32.0 6 3.5 W m 22 and the atmospheric effective emissivity by about 0.088 6 0.024. In August, the driest month of the year in Sã o Paulo, the diurnal evolution of the LW shows a minimum (325 6 11 W m 22 ) at 0900 LT and a maximum (345 6 12 W m 22 ) at 1800 LT, which lags behind (by 4 h) the maximum diurnal variation of the screen temperature. The diurnal evolution of effective emissivity shows a minimum (0.781 6 0.027) during daytime and a maximum (0.842 6 0.030) during nighttime. The diurnal evolution of all-sky condition and clear-sky day differences in the effective emissivity remain relatively constant (7% 6 1%), indicating that clouds do not change the emissivity diurnal pattern. The relationship between effective emissivity and screen air temperature and between effective emissivity and water vapor is complex. During the night, when the planetary boundary layer is shallower, the effective emissivity can be estimated by screen parameters. During the day, the relationship between effective emissivity and screen parameters varies from place to place and depends on the planetary boundary layer process. Because the empirical expressions do not contain enough information about the diurnal variation of the vertical stratification of air temperature and moisture in Sã o Paulo, they are likely to fail in reproducing the diurnal variation of the surface emissivity. The most accurate way to estimate the LW for clear-sky conditions in Sã o Paulo is to use an expression derived from a purely empirical approach.

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Formulation of a tropical town energy budget (t-TEB) scheme

Cited by 26 publications

References 55 publications

The Vertical Structure of Tropical Urban Heat Island with LES

The Vertical Structure of Tropical Urban Heat Island with LES

On the Coherence in the Boundary Layer: Development of a Canopy Interface Model

Observational Characterization of the Downward Atmospheric Longwave Radiation at the Surface in the City of São Paulo

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