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Influence of the cloud shell on tracer budget measurements of LES cloud entrainment. Dawe, Jordan T. 2012

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The Influence of the Cloud Shell on Tracer Budget Measurements of LES Cloud Entrainment JORDAN T. DAWE AND PHILIP H. AUSTIN Department of Earth and Ocean Sciences, University of British Columbia, Vancouver, British Columbia, Canada (Manuscript received 30 August 2010, in final form 20 July 2011) ABSTRACT Direct measurements of rates of entrainment into and detrainment from cumulus cloud cores obtained from LESmodel cloud fields produce values twice as large as those produced from tracer budget calculations. This difference can be explained by two effects: the presence of a shell of air around the cloud cores that is moister than the mean environment and air at the edge of the cloud core that is drier than the mean core, and the tendency for the mean tracer values of the entrained fluid to be greater than the mean tracer values of the cloud shell. Preferential entrainment of shell air that is moving upward faster than the mean shell creates strong vertical momentum fluxes into the cumulus cloud core, thereby making the assumption that cumulus cloud cores entrain fluid with zero vertical momentum incorrect. Variability in the properties of the moist cloud shell has strong impacts on entrainment values inferred from tracer budget calculations. These results indicate that the dynamics of the cloud shell should be included in parameterization of cumulus clouds used in general circulation models. 1. Introduction The rate at which air is entrained into and detrained from cumulus clouds affects cloud properties, cloud-top height, and vertical transports of heat andmoisture. Proper simulation of cumulus subgrid-scale fluxes in general cir- culation models (GCMs) depends on the accurate param- eterization of entrainment of environmental properties into the clouds and detrainment of cloud properties into the environment (Bechtold et al. 2008; de Rooy and Siebesma 2010). Entrainment and detrainment may be defined math- ematically as E52 1 A þ n̂(u2u i ),0 rn̂  (u 2 ui) dl, (1a) D5 1 A þ n̂(u2u i ).0 rn̂  (u 2 ui) dl, (1b) where E and D are the entrainment and detrainment rates (kg m23 s21), r is the density of air (kg m23 s21), u is the velocity of the air (m s21), ui is the velocity of the cloud surface (m s21), A is the area of the cloud (m2), n̂ is a unit vector directed out the cloud surface, and the path integral is taken around the cloud surface at a con- stant vertical level (Siebesma 1998). Entrainment and detrainment are thus caused by differences between the motion of the cloud surface and the motion of the air. This includes not just mixing processes, but also adia- batic processes such as condensation of water vapor at cloud base.Many parameterizations use the cloud core as the region over which to consider entrainment and de- trainment, defined as regions having condensed liquid water, positive buoyancy, and upward vertical velocity. In this case, the motion of the cloud core surface is simply substituted for themotion of the cloud surface inEqs. (1). Entrainment and detrainment rates impact GCM pa- rameterizations in several ways. First, profiles of cloud vertical mass flux are usually calculated from parame- terized entrainment values using the continuity equation for a simple entraining plume to represent an ensemble of cumulus clouds: r ›a ›t 1 ›Mcore ›z 5 E 2 D. (2) Here a is the fractional cloud core area and Mcore is vertical cloud core mass flux (kg m22 s21). The level Corresponding author address: Jordan T. Dawe, Department of Earth and Ocean Sciences, University of British Columbia, 6339 Stores Road, Vancouver, BC V6T 1Z4, Canada. E-mail: jdawe@eos.ubc.ca DECEMBER 2011 DAWE AND AUST IN 2909 DOI: 10.1175/2011JAS3658.1  2011 American Meteorological Society where the mass flux profile goes to zero then defines the location of the cloud ensemble top. Thismass flux profile is combined with the entrainment rate of environmental air into the cloud and the detrainment rate of cloud air into the environment to generate vertical profiles of cloud water vapor, condensate, and temperature, and these profiles are then used to calculate the moistening of the environment by detrainment of cloud fluid (Tiedtke 1989; Kain and Fritsch 1990). Precipitation rates are also generated from the mass flux and tracer profiles produced from the entrainment and detrainment pro- files. This wide variety of effects make entrainment rate one of the strongest controls on the climate sen- sitivity of GCMs (Stainforth et al. 2005; Rougier et al. 2009). Large-eddy simulation (LES) is the primary tool used to study cloud entrainment. LES mass entrainment and detrainment rates are typically obtained using budgets of conserved tracer variables to infer the amount of fluid exchange between the cloud ensemble and the sur- rounding air. Siebesma and Cuijpers (1995) derive the following equations for entrainment and detrainment of mass from the ensemble of cloud core plumes: Ef(fcore 2 fenv) 5 2Mcore ›fcore ›z 2 ›raw9f9 core ›z 2 ra ›fcore ›t 1 ar ›f ›t   forcing (3a) and Df(fcore 2 fenv) 5 2Mcore ›fenv ›z 1 ›r(1 2 a)w9f9 env ›z 1 r(1 2 a) ›fenv ›t 2 r(1 2 a) ›f ›t   forcing , (3b) wheref (units denoted by [f]) represents any conserved tracer, such as the total specific humidity qt (kilograms of water per kilogram of moist air) or the liquid-water moist static energy h (J kg21);w is vertical velocity (m s21); the sub- and superscripts ‘‘env’’ and ‘‘core’’ denote horizon- tally averaged values conditionally sampled in the cloud environment and core, respectively; ‘‘forcing’’ refers to tracer sources and sinks, such as radiation or large-scale subsidence, not included in the other terms; primed values represent anomalies relative to the horizontal mean; overbars represent horizontal averaging; and Ef(z) and Df(z) are the total mass entrainment rate into and de- trainment rate from the cloud core inferred from the tracer budget (kg s21 m23). Under this budget formula- tion, Ef(z) and Df(z) consist of all horizontal mass ex- changes between clouds and their environment, including advective processes, diffusive processes, and thermody- namic phase changes. We shall refer to values calculated by this method as ‘‘tracer budget’’ entrainment and detrainment. For convenience, the various tracer and entrainment/detrainment rate subscripts used below are summarized in the appendix. Alternatively, entrainment and detrainment of mass can be calculated directly from the LES velocity and tracer fields. Romps (2010) recently presented a technique to measure local (grid scale) mass entrainment rate e(x, y, z) and detrainment rate d(x, y, z). His Eq. (2) is e 2 d 5 › ›t (Ar) 1 $  (ruA). (4) Here A is the ‘‘activity’’ of the fluid, where A is 1 at cloud core points and 0 otherwise. The values of e 2 d are averaged over the time that a grid cell ex- periences mass fluxes between an active and an inactive point; positive e2 d values are considered to be purely e and negative values, d. Summing these point mea- surements horizontally gives Ed(z) andDd(z), the total mass entrained into and detrained from the cloud core field (kg s21 m23), where the subscript d indicates that these quantities were calculated directly from the model velocity and tracer fields. We shall refer to en- trainment and detrainment values calculated by this method as ‘‘direct’’ entrainment and detrainment. Romps found that such direct calculation of the en- trainment and detrainment mass fluxes produced values roughly twice as large as tracer budget calculations.Romps attributed this difference to the tracer budget calcula- tion assumption that fluid exchanged between clouds and environment has the mean properties of the cloud ensemble or environment at that level, respectively. Stud- ies of the dense, descending shell of moist air that forms around trade wind cumulus clouds (Jonas 1990; Rodts et al. 2003; Heus and Jonker 2008; Jonker et al. 2008; Heus et al. 2009; Wang and Geerts 2010) suggest that the cloud shell properties are quite different than the core or environment properties, bolstering Romps’ hy- pothesis. Since fluid exchanges between clouds and en- vironment must pass through this shell, it is likely that it plays an important role in entrainment and detrainment dynamics. Below we examine the sources of the discrepancy in entrainment and detrainment values calculated via tracer budgets and directly using Eq. (4). We show that the dis- crepancy is explained by two effects: the presence of the shell of moist air around the cloud cores and drier air at 2910 JOURNAL OF THE ATMOSPHER IC SC IENCES VOLUME 68 the edge of the cloud core, and preferential entrainment of shell air with higher average humidity and upward ve- locity than the mean shell properties, which enhances tracer fluxes between the clouds and the environment. We derive a relation to transform the direct mass entrain- ment and detrainment rates into tracer budget values suitable for use in one-dimensional simple entraining plume cloud parameterizations, and then use these transformed fluxes to evaluate the impact of the shell on tracer budget entrainment and detrainment rates of specific humidity and vertical velocity. Finally, we ex- amine the dynamics that drives the preferential entrain- ment of air with higher than average specific humidity and vertical velocity. 2. Model description All LES calculations in this paper were made using the System forAtmosphericModeling (SAM;Khairoutdinov and Randall 2003). Two model runs were performed, configured as standard Global Energy and Water Cycle Experiment (GEWEX) Cloud System Studies (GCSS; Randall et al. 2003) experiments: a Barbados Ocean- ographic and Meteorological Experiment (BOMEX; Siebesma et al. 2003) run and an Atmospheric Radia- tion Measurement Study (ARM; Brown et al. 2002) run. The BOMEX run was performed on a 6.4 km 3 6.4 km horizontal3 3.2 km vertical domain with 25-m grid size in all directions for 6 h, and the first 3 h of simulation were discarded. The ARM run was performed on a 7.68 km 3 7.68 km 3 4.5 km domain with 30-m grid size. Precip- itation was disabled in both runs. We have implemented the direct entrainment calcu- lation scheme of Romps (2010) in SAM, allowing us to calculate the mass of air entrained into and detrained from cloud core directly frommodel r, u, andA. Romps [2010, his Eq. (4)] also presents a method for calculating local entrainment and detrainment rates for any model variable in the same framework as ourEq. (4) but neglects forcing terms. These terms are significant for quantities such as vertical momentum, so we modify Romps’ equation to include their effects: ef 2 df 5 › ›t (fAr) 1 $  (fruA) 2 rASf, (5) where Sf is any nonadvective and nondiffusive source or sink term for f, such as precipitation for qt or pressure gradient for w (units of [f] s21). Diffusion is excluded from Sf as it is part of the entrainment/detrainment process and so is included in the ef 2 df term of the equation. The inclusion of these source/sink terms al- lows us to expand the definition of f to include non- conserved fluid properties. As with Eq. (4), the local (ef)(x, y, z) and (df)(x, y, z) must be horizontally summed to give the total entrain- ment into or detrainment out of the cloud ensemble for any fluid property, but since f can be negative for properties such as vertical velocity, it is possible for en- trainment to reduce and for detrainment to increase the various properties of the cloud core. To accommodate this effect, if the average value of f is positive over the time that a grid cell experiences mass fluxes between an active and an inactive grid cell, then positive ef 2 df values are considered to be purely ef and negative values, df. However, if the average off is negative, then positive ef 2 df values are considered to be purely (df)(x, y, z) and negative values, (ef)(x, y, z). The obvious way to calculate the average value of f is to perform a flux-weighted calculation, so that f 5 (ef2 df)/(e2 d).However, doing so for positive definite quantities, such as qt, sometimes results in negative f. To see the reason for this, consider a situation in which e2 d integrated over the period that a grid cell is active is found to be slightly bigger than zero for a grid cell. The Romps algorithm would assign e to a small value and d to be zero, but this is only one of many equally valid choices; as long as e ’ d, the net flux measured by the algorithm would be satisfied. At the same time, (eq)d2 (dq)d f[(ef)d2 (df)d] usingqt forfg is found to be negative, presumably due to e and d having similar mag- nitudes while the detraining air has higher humidity than the entraining air. In this case, [(eq)d 2 (dq)d]/(e 2 d) will be negative, even though qt is always positive. To avoid this problem, we calculate f as a simple time average for the purpose of determining if ef 2 df is assigned to ef or to df. Horizontal summation of (ef) and (df) then gives (Ef)d(z) and (Df)d(z), the total entrainment and detrainment of a property for the cloud ensemble (units of [f] kg s21 m23) calculated directly from the model velocity and property fields. 3. Relationship between direct and tracer budget entrainment Romps (2010) established that the direct estimate of mass entrainment and detrainment yields values roughly twice the size of those calculated via conserved tracer budgets. Furthermore, examination of the ratios of the mass entrainment and detrainment calculated via a total specific water budget (Eq, Dq) to the directly calculated values (Ed, Dd) over the diurnal cycle of an ARM LES reveals significant changes over the course of the day (Fig. 1). Thus, the direct and tracer budget measure- ments of E andD are not only significantly different but also have differing dynamics, which may need to be accounted for in large-scale parameterizations of cloud DECEMBER 2011 DAWE AND AUST IN 2911 entrainment and detrainment. In this section we exam- ine the sources of disagreement between direct and tracer budget estimates of mass entrainment into and detrainment from the cloud core. a. E and D cloud shell correction Romps attributed the differences between (Ef, Df) and (Ed, Dd) to the assumption made by Siebesma and Cuijpers (1995) that fluid being entrainedor detrained has the properties of the mean environment or cloud core, respectively. If we examine the horizontal mean specific humidity of the fluid at the ‘‘cloud core edge’’ (cloud core model grid cells that are nearest-neighbor adjacent to noncore cells), which presumably is the fluid being de- trained, we see that it is indeed drier than the mean core (Fig. 2a). Similarly, the fluid available for entrainment in the ‘‘cloud core shell’’ (noncore model grid cells that are nearest-neighbor adjacent to core cells) is moister than the mean environment. Budget equations that explicitly distinguish between the mean cloud core and environment properties and the properties of the entraining and detraining fluid al- low us to transform (Ed, Dd) values into corresponding tracer budget values, and back again. We start our derivation with the observation that both the tracer budget and direct values of E and D are consistent with the continuity equation [Eqs. (2) and (4)]. This implies that Ef 2 Df 5 Ed 2 Dd. (6) Similarly, the entrainment and detrainment rates of fluid properties must be consistent with the total property budget, giving us Effenv 2 Dffcore 5 EdfE 2 DdfD, (7) where fE and fD represent the f of the fluid being en- trained or detrained, respectively. Combining these equations and solving for Ef and Df in turn results in Ef,T 5 Ed 2 Ed fE 2 fenv fcore 2 fenv 1Dd fcore 2 fD fcore 2 fenv   , (8a) Df,T 5 Dd 2 Ed fE 2 fenv fcore 2 fenv 1Dd fcore 2 fD fcore 2 fenv   . (8b) Here the subscript T indicates that these Ef and Df tracer budget values have been calculated by trans- formation of direct values, not via Eqs. (3). Ideally these transformed values should be identical to the tracer budget values, but numerical errors may result in dif- ferences between the two calculationmethods and so we use the subscript T to make clear the method used to calculate each entrainment and detrainment value. The bracketed terms represent the bias introduced by as- suming that entrained/detrained air has the properties of the mean environment and core. Thus, to convert from (Ed, Dd) to (Ef,T, Df,T), both Ed and Dd must be re- duced by EdA 1 DdB, where A 5 (fE 2 fenv)/(fcore 2 fenv) and B 5 (fcore 2 fD)/(fcore 2 fenv). Note that rearrangement ofA givesfE5Afcore1 (12 A)fenv, meaning that A can be thought of as the fraction of mean core air in a mixture of mean core and mean environment air needed to produce the properties of the entrained fluid. Similarly,fD5Bfenv1 (12B)fcore and B can be thought of as the fraction of mean envi- ronment air in a mixture of mean core and mean envi- ronment air needed to produce the properties of the detrained fluid. FIG. 1. Ratio of the total specific water tracer budget (a) en- trainment and (b) detrainment values to the directly calculated values over the duration of the ARM model run. 2912 JOURNAL OF THE ATMOSPHER IC SC IENCES VOLUME 68 Alternatively, we can solve for Ed and Dd, arriving at Ed,T 5 Ef 1 Ef fE 2 fenv fD 2 fE 1 Df fcore 2 fD fD 2 fE   . (9a) Dd,T 5 Df 1 Ef fE 2 fenv fD 2 fE 1 Df fcore 2 fD fD 2 fE   . (9b) Again, the T subscript indicates these Ed and Dd values have been calculated by transformation of Ef and Df, not via Eq. (4). In this case, to convert from (Ef,Df) to (Ed,T,Dd,T), bothEf andDfmust be increased byEfa1 Dfb, where a5 (fE2 fenv)/(fD2 fE) and b5 (fcore2 fD)/(fD 2 fE). We now have relationships allowing us to transform the unbiased Ed andDd values into biased tracer budget Ef and Df values, which are better suited for simple entraining plume parameterization of cloud fields. Com- parison of Eq and Dq (Ef and Df inferred using total specific moisture qt as the tracer) with Ed and Dd shows that the direct entrainment and detrainment magnitudes are significantly larger than the tracer budget values (Figs. 2b,c, gray and dotted lines). Using Eq. (8) to cal- culate Eq,T and Dq,T with qE 5 qedge, the horizontal mean humidity in the cloud edge, and qD 5 qshell, the horizontal mean humidity in the cloud shell, results in values quite close to the tracer budget values above the middle of the cloud layer. The transformation also du- plicates the negative detrainment values near cloud base that are typically produced by tracer calculations. b. Preferential entrainment of moist ascending air Relative to the tracer budget values, theEq,T andDq,T values calculated using qE5 qedge and qD5 qshell are still too large near cloud base.We can explain this difference as being the result of the mean fluid property values of the entrained and detrained air being different than the mean values of the shell and edge air, respectively. Using the mean shell and edge values of properties to trans- form the direct entrainment and detrainment assumes that any fluid parcel in the shell or edge is equally likely to be entrained or detrained. In reality,mixing relatively dry air into the cloud core is more likely to cause evaporation, which will drive detrainment, while mixing relatively moist air into the cloud core is more likely to produce a saturated fluid mixture, resulting in entrainment. This suggests that the moistest shell parcels are more likely to undergo entrainment than the average shell parcel, and the driest edge parcels are more likely to detrain than the average edge parcel. We can directly calculate the effective fluid property values at which entrainment occurs by taking the total fluid property entrainment (Ef)d [calculated via Eq. (5)] and dividing it by the total mass entrainment Ed so that fentrain 5 (Ef)d/Ed. Similarly, the effective property values of the detraining air can be found from FIG. 2. Result of transforming direct entrainment values into equivalent tracer budget values using mean cloud core shell and edge properties from the BOMEX simulation. (a) Mean profiles of the total specific humidity in the cloud core (thick black line), cloud core edge (thin black line), cloud core shell (thin gray line), and cloud core environment (thick gray line). These qt values are used to transform directly calculated values of (b) entrainment and (c) detrainment (gray line) into equivalent tracer budget values (black line). The tracer budget entrainment and detrainment are shown for comparison (dotted lines). DECEMBER 2011 DAWE AND AUST IN 2913 fdetrain 5 (Df)d/Dd. Examination of these values from the BOMEX simulation using qt for f shows that qentrain is moister than qshell (Fig. 3a), indicating that entrainment occurs preferentially at the moistest parts of the shell. Conversely, there is little difference between qdetrain and qedge, indicating that the detrained parcels tend to have the mean moisture of the cloud core edge. Using qentrain and qdetrain to transform Ed and Dd reduces the large entrainment and detrainment values near cloud base found using the mean shell and edge properties (solid black line, Figs. 3b,c), bringing Eq,T and Dq,T into agree- ment with Eq and Dq. 4. Eq, Eh, and Ew differences Equation (8a) or (8b) implies that the tracer budget method will measure different entrainment and detrain- ment values for fluid properties with differing values of A 5 (fE 2 fenv)/(fcore 2 fenv) and B 5 (fcore 2 fD)/ (fcore 2 fenv), respectively. Supporting this, Romps (2010, his Fig. 2) showed that changing the sources and sinks applied to an artificial numerical tracer re- sulted in large changes in measured tracer budget en- trainment rates. With this in mind we compare Ef,T and Df,T values produced by h and w with those produced using qt. Liquid water moist static energy shows a similar relative distribution of core, edge, shell, environment, entrained, and detrained properties when compared to qt, indicating a tight coupling between these variables in the cloud dynamics. Because these properties are so tightly cou- pled,Eh,T andDh,T values are nearly identical to theEq,T and Dq,T (not shown). Vertical velocity shows very different relative profiles compared to qt or h (cf. Figs. 4a and 3a). There is a much wider spread in the w values, with the shell having nearly zero vertical velocity and the edge being halfway between the core and the environment. The value of wdetrain is slightly larger than the value ofw in the cloud core edge, while wentrain is much larger than w in the shell, be- coming roughly the same value as wedge. Since wentrain and wdetrain are both larger than wshell and wedge, this implies that rapidly rising air is both preferentially en- trained and detrained over slowly rising air. These ef- fective entrainment and detrainment w values produce Ew,T and Dw,T values (solid black line, Figs. 4b, 4c) that are quite different than the entrainment and detrainment produced by qt and h (dotted line, Figs. 4b,c); Ew,T is negative near cloud base while Eq,T is positive, and both Ew,T and Dw,T are half the magnitude of Dq,T over much of the cloud layer. Finally, we examine the temporal variability of A 5 (fE2 fenv)/(fcore2 fenv) andB5 (fcore2 fD)/(fcore2 fenv) from the transformation Eqs. (8a) and (8b) in the ARMmodel run. SinceA represents the fraction of core air in a mixture of core and environmental air that has the properties of fE, and B represents the fraction of environmental air in amixture of core and environmental FIG. 3. Result of transforming direct entrainment values into equivalent tracer budget values using effective entrainment and de- trainment properties from the BOMEX simulation. (a) Mean profiles of qentrain (black line), and qdetrain (dotted line), overlaid on the mean total specific water values of the core, edge, shell, and environment. These qt values are used to transform directly calculated values of (b) entrainment and (c) detrainment (gray line) into equivalent tracer budget values (black line). The Siebesma tracer budget en- trainment and detrainment are shown for comparison (dotted lines). 2914 JOURNAL OF THE ATMOSPHER IC SC IENCES VOLUME 68 air that has the properties of fD, A and B provide information about the reentrainment of previously detrained core fluid and detrainment of previously entrained environmental fluid occurring at different model heights. However, A and B cannot be consid- ered exact mixing fractions, as the source heights of entrained or detrained air mixtures may be different than the height at which they entrain or detrain, and not all mixtures of core and environment properties are equally likely to undergo entrainment. The values ofA andB calculated for qt both show strong changes over the ARM diurnal cycle (Figs. 5a,b). Near cloud base, A is nearly 1 while B is nearly 0, implying that both the entrained and detrained air have the properties of the cloud core air. This is due to the main entrainment process at cloud base being condensation of rising thermals instead of mixing; buoyant updrafts simply condense without modification of their proper- ties. Similarly, the air that detrains from the clouds at cloud base is almost undiluted becausemost entrainment at this level comes from the well-mixed subcloud layer below and so has properties nearly identical to the cloud core. At cloud top, A is also nearly 1 while B is nearly 0, implying that both the entrained and detrained air have the properties of the cloud core air. This is due to cloud core detrainment in the inversion being driven by the cloud becoming negatively buoyant as it enters the steep inversion temperature gradient (Wu et al. 2009). This process is adiabatic, and so the air detraining from the core is undiluted by the environment. Conversely, much of the air surrounding the remaining cloud core that is available for entrainment was previously detrained from the corewithoutmixing, and so has the properties of the core air. As the clouds detrain into the inversion over the course of the day, they cause the inversion to rise. This means that points in themidcloud layer are less influenced by the adiabatic entrainment and detrainment processes oc- curring at cloud base and cloud top, and so the effects of mixing become more prominent. By the end of the day, A within the cloud layer has values near 0.6, suggesting that a significant amount of reentrainment of air previously detrained from the core still occurs.Also,Bhas values near 0.2, indicating that air detraining from the core is rela- tively undiluted by environmental air; this makes sense, since relatively little dilution by environmental air is re- quired to cause the core air to become neutrally buoyant and detrain. When calculated for w, A reaches a value around 0.4 and B goes to 0.6 near the middle of the cloud layer by the end of the day. The differences between these values and the values ofA and B calculated for qt are the result of buoyancy and pressure gradient forces on themixtures, and the stronger tendency for upward-moving shell par- cels to be entrained relative to the tendency to entrain moister shell parcels. In other words, a relatively dry, rapidly ascending shell parcel is more likely to be en- trained than a relatively moist, slowly ascending shell parcel. This is especially apparent near cloud base where the values ofA are larger than 1, due to themean entrained FIG. 4. Result of transforming direct entrainment values from the BOMEX simulation into equivalent w budget values. (a) Mean profiles of the effectivew values being entrained (black line), and detrained (dotted line), overlaid on the meanw values of the core, edge, shell, and environment. The entrained and detrained w values are used to transform directly calculated values of (b) entrainment and (c) detrainment (gray line) into equivalent tracer budget values (black line). The entrainment and detrainment values transformed using qt are shown for comparison (dotted lines). DECEMBER 2011 DAWE AND AUST IN 2915 parcels having a larger upward velocity than the mean core parcels. Performing these calculations with fixed values of (fcore 2 fenv), to remove changes due to movement of the mean environment and core profiles, shows similar results. Changes in the properties of the entraining and detraining fluid due to the dynamics of mixing and en- trainment in the shell clearly are active in determining the rates at which properties entrain and detrain. 5. Causes of preferential entrainment of moist ascending air The reason that shell air that is moister and ascending faster than the mean shell is more likely to be entrained can be seen by comparing instantaneous snapshots of the model values of local mass entrainment e, moisture en- trainment eqt, and vertical velocity entrainment ew. Since theRomps (2010) method of calculating e and d requires taking time averages, it is unsuitable for calculating in- stantaneous entrainment fields. Instead, we use an alter- native method we have devised that substitutes spatial interpolation for time averaging (DaweandAustin 2011). This alternative method results in slightly smaller values of e and d than those produced by Romps’ method, but the two calculations show good agreement in variability. The eqt and ew fields are calculated simply bymultiplying the value of e by the values of qt and w, respectively. Comparing the e, eqt, and ew fields shows that e and eqt have a very similar spatial pattern, but ew is concentrated in regions where strong updrafts enter the cloud core (Fig. 6). The reason for this can been seen by examining the buoyancy, condensed liquid water, and vertical ve- locity fields that define the cloud core. Of these three fields, buoyancy is the strongest constraint determining if air is part of the core. However, regions exist far above cloud base where air has become negatively buoyant but maintains upward velocity and condensed liquid water. As this air continues to rise, more condensation occurs, which heats the updraft, makes it positively buoyant, and thus entrains it into the core. In this way, entrain- ment is positively correlated with both qt and w. This process occurs fairly often in our model cloud field, as evidenced both by our manual examination of the FIG. 5. Variation in (a) the fraction of core air in a mixture of core and environmental air needed to produce the mean humidity entrained by the clouds, (b) the fraction of environmental air in a mixture of core and environmental air needed to produce the mean humidity detrained by the clouds, (c) the fraction of core air in a mixture of core and environmental air needed to produce the mean vertical velocity entrained by the clouds, and (d) the fraction of environmental air in a mixture of core and environmental air needed to produce the mean vertical velocity detrained by the clouds, over the duration of the ARM model run. 2916 JOURNAL OF THE ATMOSPHER IC SC IENCES VOLUME 68 output fields and by the size of the difference between wshell and wentrain in the mean profiles. While the tendency for rapidly ascending shell air to be entrained more often than the slower parts of the shell was found for cloud core entrainment, we would like to emphasize that this process is not an artifact of the cloud core sampling; similar results appear when we perform entrainment calculations for simple cloudy re- gions (areas of condensed liquid water). In this case, vertical advection of air can drive condensation, con- verting environment air into cloud air and thus driving entrainment of air into the cloud. 6. Discussion Considering all these results, we now turn to the most important question of all: which entrainment value is the right one? The unsatisfying answer is that it depends on the purpose for which the entrainment is to be used. Consider a cumulus cloud plume model based on a simplified form of the continuity equation that assumes the cloud fraction is constant, ›Mcore ›z 5 E 2 D, (10) a cloud budget equation for a conserved variable f that assumes mean vertical advection is balanced by en- trainment of mean environmental properties, Mcore ›fcore ›z 5 E(fenv 2 fcore), (11) and a simple detrainment forcing equation, r ›fenv ›t 5 D(fcore 2 fenv). (12) The term fenv is input to the parameterization from the GCM. If we assume we have a perfect parameterization ofMcore and fcore at cloud base with which to construct mean core mass flux and tracer profiles, we wish the E andD values to produce a profile of ›fenv/›t to force the GCM that agrees with LES results for a similar mean environmental profile. The E and D we desire then are FIG. 6. Instantaneous vertical cross section of (a) directly calculated cloud coremass entrainment, (b) humidity entrainment, (c) vertical velocity entrainment, (d) buoyancy, (e) condensed liquid water, and (f) vertical velocity of a single BOMEX simulation cloud, illustrating the tendency to entrain shell air that is rising faster than the mean shell. Black lines indicate the edge of the cloud core in each figure. DECEMBER 2011 DAWE AND AUST IN 2917 closer to Ef and Df than to Ed and Dd but nevertheless are not identical to Ef andDf because of neglect of the time tendency and Reynolds flux budget terms in Eqs. (11) and (12). This also implies that we should have different Ef andDf values for properties with different distribution patterns around the clouds. Using values near Ed and Dd instead would require modifying Eq. (11) to Mcore ›fcore ›z 5 E(fcore 2 fE) 2 D(fcore 2 fD) (13) and Eq. (12) to r ›fenv ›t 5 D(fD 2 fenv) 2 E(fE 2 fenv). (14) Now, instead of calculating different E andD values for each tracer we wish to model, we must instead calculate fE and fD values for each property that is entrained or detrained. While it is possible this would produce a bet- ter parameterization, it seems simpler to fold the effects of fE and fD into the E and D values and keep the equations in their less complex forms. On the other hand, the true values of the mass entrainment and de- trainment are important for comparison of LES results with field studies using Doppler radar to estimate en- trainment and detrainment velocities, or possibly for cal- culations of aerosol reactions whose chemical properties are dependent on the concentration of liquid water in the air (Hoppel et al. 1994). They are also vital for di- agnosing mass exchanges of individual clouds in an LES ensemble, for which a simple ‘‘environment’’ and ‘‘cloud core’’ mean tracer budget may be difficult to define. The large positive values of wentrain are clearly in- consistent with the often-made assumption that fluid entrained into the cloud has negligible vertical mo- mentum (Siebesma et al. 2003). This is reflected in the smaller values of the transformed Ew,T and Dw,T shown in Fig. 4. The negative values of Ew, Eq, and Dw pro- duced near cloud base emphasize the artificial nature of the tracer budget entrainment and detrainment. Rather, Ef and Df should be interpreted simply as mathemati- cal quantities that satisfy both the continuity Eq. (2) and the tracer budget of the cloud core under the assumption that the core entrains mean environment fluid and de- trains mean cloud core fluid. As both BOMEX and ARM model simulations involved nonprecipitating shallow cumulus, we have ignored the effects of precipitation. Precipitation is generally not considered part of the turbulent mixing processes associated with entrainment and detrainment in parameterization, instead being represented by a sink term in the liquid water budget (Tiedtke 1989; Kain and Fritsch 1990). Nevertheless, incorporating precipitation into the tracer budget and direct entrainment calcula- tions would be relatively simple. The precipitation flux divergence would be a new sink/source forcing term in Siebesma’s Eq. (3), andwould be part of the forcing term rASf in Romps’ Eq. (5), resulting in precipitation flux divergence not being counted as part of the detrainment. Specifying the advection terms would be somewhat trickier since, depending on the complexity of the mi- crophysics scheme, moisture might be advected as a sin- gle qt field or advected as separate hydrometeor classes. However, this would simply mean adding extra advec- tion terms for each hydrometeor class. Once these ef- fects were properly incorporated into the calculations, the transformations between (Ed, Dd) and (Eq, Dq) would be unchanged. 7. Conclusions We have explained the differences between values of cloud core entrainment and detrainment of mass cal- culated via tracer budget and direct calculations as the result of the presence of a shell of moist air around the cloud cores and drier air at the edge of the cloud core, and the tendency for themean tracer value of the entrained fluid to be greater than themean tracer value of the cloud shell. Relaxing the assumption made by Siebesma and Cuijpers (1995) that entrained and detrained fluid has the properties of the environment and core, respectively, allows us to transform direct entrainment/detrainment values into corresponding tracer budget values suitable for use in simple entraining plume parameterizations of cumulus convection. The moistest, fastest-rising regions of the shell are entrained more often than drier, slower-rising regions. This tendency results from thermodynamic phase changes in rising air parcels. Condensation in upward-moving, saturated, but negatively buoyant air parcels causes la- tent heating, increasing the air’s buoyancy and causing it to entrain into the core. This effect suggests that the dynamics of the moist cloud shell have a role in medi- ating fluxes between the clouds and the environment. Transforming directly calculated values of entrainment and detrainment into tracer budget values results in different entrainment and detrainment values for total specificwater qt and liquid-watermoist static energy h than for vertical velocity w. Furthermore, the tracer budget values of entrainment and detrainment compatible with qt, h, and w exhibit different patterns of variability over the course of a diurnal cycle in a GCSS ARM LES. This suggests that cumulus cloud parameterizations based on bulk models should use different E and D values for qt and h than forw, and it raises the possibility that different 2918 JOURNAL OF THE ATMOSPHER IC SC IENCES VOLUME 68 entrainment and detrainment rates apply to other cloud properties, such as aerosol concentrations. Direct entrainment and detrainment calculations are powerful tools that should be used to help improve our understanding of the dynamics ofmass exchanges between clouds and their environment, with an eye to folding these effects into the simplest parameterizations possible. Doing so has the potential to improve GCM parameterization of the magnitude and variability of mass and tracer ex- changes between clouds and their environment. Acknowledgments. Support for this workwas provided by the Canadian Foundation for Climate and Atmo- spheric Science through theCloudAerosol Feedback and Climate network. We thank Marat Khairoutdinov for making SAM available to the cloud modeling com- munity. We would also like to thank David Romps and two anonymous reviewers whose comments significantly improved the quality of this paper. All figures were gen- erated using the matplotlib library in the Python pro- gramming language. APPENDIX Table of Notation Table A1 shows the variables, along with their defi- nitions and units, used in this study. REFERENCES Bechtold, P., M. Köhler, T. Jung, F. Doblas-Reyes, M. Leutbecher, M. J. Rodwell, F. Vitart, and G. Balsamo, 2008: Advances in simulating atmospheric variability with the ECMWF model: From synoptic to decadal time-scales. Quart. J. Roy. Meteor. Soc., 134, 1337–1351, doi:10.1002/qj.289. Brown, A. R., and Coauthors, 2002: Large-eddy simulation of the diurnal cycle of shallow cumulus convection over land.Quart. J. Roy. Meteor. Soc., 128, 1075–1093. Dawe, J. T., and P. H. Austin, 2011: Interpolation of LES cloud surfaces for use in direct calculations of entrainment and de- trainment.Mon. Wea. Rev., 139, 444–456. de Rooy, W. C., and A. P. Siebesma, 2010: Analytical expressions for entrainment and detrainment in cumulus convection.Quart. J. Roy. Meteor. Soc., 136, 1216–1227, doi:10.1002/qj.640. Heus, T., and H. J. J. Jonker, 2008: Subsiding shells around shallow cumulus clouds. J. Atmos. Sci., 65, 1003–1018. ——, C. F. J. Pols, H. J. J. Jonker, H. E. A. Van den Akker, and D. H. Lenschow, 2009: Observational validation of the com- pensating mass flux through the shell around cumulus clouds. Quart. J. Roy. Meteor. Soc., 135, 101–112. Hoppel, W. A., G. M. Frick, J. Fitzgerald, and R. E. Larson, 1994: Marine boundary-layer measurements of new particle for- mation and the effects nonprecipitating clouds have on aerosol size distribution. J. Geophys. Res., 99, 14 443–14 459. Jonas, P. R., 1990: Observations of cumulus cloud entrainment. Atmos. Res., 25, 105–127. Jonker, H. J. J., T. Heus, and P. P. Sullivan, 2008: A refined view of vertical mass transport by cumulus convection.Geophys. Res. Lett., 35, L07810, doi:10.1029/2007GL032606. Kain, J. S., and J. M. Fritsch, 1990: A one-dimensional entraining/ detraining plume model and its application in convective pa- rameterization. J. Atmos. Sci., 47, 2784–2802. TABLE A1. List of symbols. Symbol Unit Definition First occurrence E(z), D(z) kg m23 s21 Cloud core mass entrainment, detrainment rate Eq. (2) Ef(z), Df(z) kg m 23 s21 Mass entrainment, detrainment rate calculated using the Siebesma tracer budget Eqs. (3a), (3b) e(x, y, z), d(x, y, z) kg m23 s21 Local mass entrainment, detrainment rate calculated directly from model velocity and tracer fields Eq. (4) Ed(z), Dd(z) kg m 23 s21 Cloud core mass, detrainment rate calculated from the horizontal sum of e(x, y, z) or d(x, y, z) Section 1 (ef)(x, y, z), (df)(x, y, z) [f] kg m23 s21 Local cloud core f entrainment, detrainment rate calculated directly from model velocity and tracer fields Eq. (5) (Ef)d(z), (Df)d(z) [f] kg m 23 s21 Cloud core f entrainment, detrainment rate calculated from the horizontal sum of (ef)(x, y, z) or (df)(x, y, z) Section 2 Ef,T(z), Df,T(z) kg m 23 s21 Mass entrainment, detrainment rate calculated by transforming direct values into budget values Eqs. (8a), (8b) Ed,T(z), Dd,T(z) kg m 23 s21 Cloud core mass entrainment, detrainment rate calculated by transforming tracer budget values into direct values Section 1 f(x, y, z) [f] Any fluid property, such as qt (kg kg 21), h (J kg21), or w (m s21) Section 1 fcore(z) [f] Mean cloud core f Section 3a fedge(z) [f] Mean cloud edge f Section 3a fshell(z) [f] Mean cloud shell f Section 3a fenv(z) [f] Mean environment f Section 3a fentrain(z) [f] Effective value of f being entrained calculated from (Ef)d/Ed Section 3b fdetrain(z) [f] Effective value of f being detrained calculated from (Df)d/Dd Section 3b fE(z) [f] Placeholder for the value of f assumed to be entraining Eq. (8a) fD(z) [f] Placeholder for the value of f assumed to be detraining Eq. (8b) DECEMBER 2011 DAWE AND AUST IN 2919 Khairoutdinov, M. F., and D. A. Randall, 2003: Cloud resolving modeling of the ARM summer 1997 IOP: Model formulation, results, uncertainties, and sensitivities. J.Atmos. Sci., 60, 607–625. 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